it feast ed eI Fk Baie Rats eet x ACH Al Oe Sete ‘t te 5 Gui PY a wheal 7 frie sie iba Tbre 6.45 wh it His r tN ralesms eek dite Ne May ees Haney we ven ihe rt cee VR ENS es pce Ries: mainly Catena of we rar iit sat eee in ag i it ANS STEN Att cat PISO, ie! Die amy yagi ene hst. tenets te Tatty ha its, aaa Caen} yesh) ta TET TR | Pai ae r a a iH se 3 PROCEEDINGS Ole Walle LINNEAN SOCIETY F NEW SOUTH WALES VOLUME 104 (Nos 457-460; for 1979-80) Sydney The Linnean Society of New South Wales 1980 © Linnean Society of New South Wales Contents of Proceedings Volume 104 PART 1 (No. 457) (Issued 21st July, 1980) PEOU, S. Some Carboniferous articulate brachiopods from eastern News Ouchi Wialesr sive rspcccnc sae cis apenas ee ee ur raw) oe aanieVn alse LARSON, H. K., and HOESE, D. F. The species of the Indo-West Paciic genus, Galumza) (Pisces: Eleotridae) <3: 5...55.-2..45-- HARRIS, M. MCD., KING, R.J., and ELLIS, J. The eelgrass Zostera capricornz in Illawarra Lake, New South Wales ......... HUTCHINGS, P., and RAINER, S. A key to estuarine polychaetes in INEWESOUCIVialeS Wee seis h eo retort acts euepvias Mee os 6 oe ei ehabe BUCHANAN, R. A., and HUMPHREYS, G. S. The vegetation on two podzols on the Hornsby Plateau, Sydney ................. BUCHANAN, R. A. The Lambert Peninsula, Ku-ring-gai Chase National Park. Physiography and the distribution of podzols, shrublands and swamps, with details of the swamp vegetation ANGLES FITMENT Sy rs ctter sc citer ka Las tele aur seta )os ctio) Suisicovle Pe gessteeoeuetlau'e ceria) emistin te PART 2 (No. 458) (Issued 21st July, 1980) FACER, R. A., HUTTON, A. C., and Frost, D. J. Heat generation by siliceous igneous rocks of the basement and its possible influence on coal rank in the Sydney Basin, New South Wales ............ CARR, P. F., JONES, B. G., and WRIGHT, A. J. Dating of rocks from the Bungonia district, New South Wales .................... TIMMS, B. V. The benthos of the Kosciusko glacial lakes ............ McNAMARA, K. J., and PHILIP, G. M. Living Australian schizasterid SCHIMOLASMER nace Sree e tee Paces has at occ wc erctns sgh neon Mle ay as ANDERSON, D. T. Cirral activity and feeding in the lepadomorph barnacle Lepas pectinata Spengler (Cirripedia) ............... Annexure to Parts 1 and 2. The Linnean Society of New South Wales. Record of the Annual General Meeting 1979. Reports amMGep aliameeys Mets: se reer cee ral tse ol ee otiee ove smelt @) a 6 eels oc NUMBER* 3 (No. 459) (Issued 16th January, 1981) SHAW, D. E., and CARTLEDGE, E. G. Sporobolomycetaceae from Indooroopilly (Australia) and from Port Moresby (Papua New Guimea) tei ia ie er a oaiey leat nna e Wa Mani pn arebeen 161 SKILBECK, C. G. A preliminary report on the late Cainozoic geology and fossil fauna of Bow, New South Wales ....................0- level DOMROW, R. The genus Razllzetza Trouessart in Australia (Acari: Dermanyssid ae). jn S es oe as eer i ce licen ea ey tice ona 183 POWELL, C. MCA., FERGUSSON, C. L., and WILLIAMS, A. J. Structural relationships across the Lambian Unconformity in the Hervey Range-Parkes:area IN :SoW) ic, Lace epee Cee tee 195 WRIGHT, A. J., and FLorY, R. A. A new Early Devonian tabulate coral from the Mount Frome Limestone, near Mudgee, New South Wales 211 NUMBER 4 (No. 460) (Issued 16th January, 1981) DOMROW, R. A new species of the ulysses group, genus Haemolaelaps Berlese(Acam: Dermanyssidae)) 2) goin a ae ee eee 22h CARR, P. F., JONES, B. G., KANSTLER, A. J., MOORE, P.S., and Cook, A. C. The geology of the Bungonia district, New South Weales ceo Ce SORk OS ie SGN Ah Vago aeae TERR ne Ga enn Ra 229 SKINNER, S. New records of Zygnemaphyceae and Oedogoniophyceae (Chlorophyta) from northern New South Wales .............. 245 DuGAN, K. G. Darwin and Diprotodon: The Wellington Caves fossilsiand the law, of succession’ elias) ee ee eee 265 LEITCH, E. C. Rock units, structure and metamorphism of the Port Macquarie Block, eastern New England Fold Belt ............. 273 LINNEAN SOCIETY OF NEW SOUTH WALES. Presidential addresses prntedanitheiProceedmnes NOZ0719 i She eee ae eee 293 TINE 2). Ps, SU Sel ea nS TS lene nn GE ae 299 *The change from Part to Number is required by the latest guidelines governing eligibility for the Book Bounty. Issue of the record of Society business as an Annexure to Parts 1 & 2 follows the same advice. — Ed. PROCEEDINGS of the | LINNEAN - SOCIETY NEW SOUTH WALES VOLUME 104 PARTS 1&2 © NATURAL HISTORY IN ALLITS BRANCHES THE LINNEAN SOCIETY OF NEW SOUTH WALES Founded 1874. Incorporated 1884. The Society exists to promote ‘the Cultivation and Study of the Science of Natural History in all its Branches’. It holds meetings and field excursions, offers annually a Linnean Macleay Fellowship for research, contributes to the stipend of the Linnean Macleay Lecturer in Microbiology at the University of Sydney, and publishes the Proceedings. Meetings include that for the Sir William Macleay Memorial Lecture, delivered biennially by a person eminent in some branch of Natural Science. The Society’s extensive library is housed at the Science Centre in Sydney. Membership enquiries should be addressed in the first instance to the Secretary. Candidates for election to the Society must be recommended by two members. The present annual subscription is $17.50. The current rate of subscription to the Proceedings for non-members is set at $30.00 per volume. Back issues of all but a few volumes and parts of the Proceedings are available for purchase. A price list will be supplied on application to the Secretary. OFFICERS AND COUNCIL 1979-80 President: A. RITCHIE Vice-Presidents: LYNETTE A. MOFFAT, T. G. VALLANCE, J. T. WATER- HOUSE, B.D. WEBBY . Honorary Treasurer: D. A. ADAMSON Secretary: BARBARA STODDARD Council: D. A. ADAMSON, M. ARCHER’, L. W. C. FILEWOOD?’, A. E. GREER, L. A. S. JOHNSON, HELENE A. MARTIN, P. M. MARTIN?, LYNETTE A. MOFFAT, P. MYERSCOUGH, A. RITCHIE, A. N. RODD, F. W. E. ROWE, E. J. SELBY*, C. N. SMITHERS, P. J. STANBURY, N. G. STEPHENSON’, T. G. VALLANCE, JOYCE W. VICKERY’®, J. T. WATERHOUSE, B. D. WEBBY, A.J. T. WRIGHT Honorary Editor: T. G. VALLANCE — Department of Geology & Geophysics, University of Sydney, Australia, 2006. Librarian: PAULINE G. MILLS Linnean Macleay Fellow: BARBARA D. PORTER Linnean Macleay Lecturer in Microbiology: K.-Y. CHO Auditors: W. SINCLAIR & Co. The office of the Society is in the Science Centre, 35-43 Clarence Street, Sydney, N.S.W., Australia, 2000. Telephone (02) 290 1612. ©Linnean Society of New South Wales * appointed 23 May 1979 ? appointed 19 December 1979 3 appointed 21 November 1979 * resigned 23 May 1979 ° resigned 24 October 1979 ° deceased 29 May 1979 Cover motif: Fossarus sydneyenszs Hedley Balmoral Beach, Sydney (Proc. Linn. Soc. N.S.W. 35, 1900: 89) PROCEEDINGS of the LINNEAN SOCIETY NEW SOUTH WALES VOLUME 104 PANT JI Some Carboniferous Articulate Brachiopods from Eastern New South Wales S. PEOU pe ee ee PEou, S. Some Carboniferous articulate brachiopods from eastern New South Wales. Proc. Linn. Soc. N.S.W. 104 (1), (1979) 1980:1-15. Nine fossil localities in the Carboniferous Berrico Creek Formation at Berrico- Rawdon Vale and an unnamed formation at Brownmore in eastern New South Wales, have yielded a number of new brachiopod taxa belonging to the Rhipidomella forttmuscula Zone. Among these taxa are Quadratza engeli sp. nov., Q. boonzenszs sp. nov., Productoid gen. et sp. nov., ‘Camarotoechia’ subtrigonalis sp. nov., Schizophoria subelliptica sp. nov., Podtsheremia fasciculata sp. nov., and Brachythyris cobarkensts sp. nov. They are short-ranging species and hence are suitable as zonal index fossils. S. Peou, Department of Geology, University of Newcastle, Australia 2308; manuscript received 28 September 1978, accepted in revised form 21 February 1979. INTRODUCTION The Rhip:domella fortemuscula Zone is one of nine major brachiopod zones in the Carboniferous of eastern Australia (Campbell and McKellar, 1969; Campbell and Roberts, 1969; Jones et al., 1973; Roberts, 1975; Roberts et al., 1976). The fauna of this zone was first studied by Cvancara (1958) and then by Campbell and McKelvey (1972) from the Barrington District, New South Wales. McKellar (1967) and Driscoll (1960) recognized this fauna from the Yarrol Trough, Queensland. Over the past twenty years, a large number of brachiopod genera and species have been described from the Rhzpzdomella fortimuscula Zone, many of them are short-ranging forms and clearly indicative of a late Visean age (Roberts, 1975, 1976). Recent work on rocks of this age in the Berrico Creek Formation at Berrico-Rawdon Vale (Whitford, 1971; Peou, 1977) and an unnamed formation at Brownmore (McDonald, 1972; Roberts, 1975) (Fig.1), has resulted in discrimination of several new taxa. Good stratigraphical control and short ranges suggest that these taxa may per BERRICO-RAWDON VALE BROWNMORE BRACHIOPOD ZONES/SUBZONES CUT HILL BOORAL FORMATION FORMATION FAULKLAND FORMATION 7A 7 UNNAMED SANDSTONE BERRICO CREEK 6 FORMATION 6 CARSONVILLE FORMATION 5 WOOTTON BEDS lL inoproductus (Balakhonia)/rawdonvalensis Marginirugus barringtonensis UNNAMED 6 FORMATION Rhipidomella fortimuscula 6? pinea FLAGSTAFF CARBONIFEROUS aspinosa SANDSTONE Fig. 1. Correlation of Carboniferous formations of the Berrico-Rawdon Vale and Brownmore districts, N.S.W. The brachiopod zones/subzones are indicated by numbers on the right hand side of columns (Modified from Roberts, 1975; Peou, 1977; and Peou and Engel, 1979). Proc. Linn. Soc. N.S.W., 104 (1), (1979) 1980 2 CARBONIFEROUS ARTICULATE BRACHIOPODS be useful for zonal identification. They include two species of Quadratza, one species each of ‘Camarotoechia’, Schizophoria, Podtsheremia and Brachythyris; one productoid described on the basis of only three specimens has been temporarily designated as a new genus and species. The descriptions of these brachiopods are based on collections housed in the Department of Geology, University of Newcastle, New South Wales. The fossils have been obtained from nine localities in the Berrico-Rawdon Vale-Brownmore region, N.S.W. (Fig.2). Details of these localities (locality number, grid references and name of the topographic sheets) are given at the end of the paper. SYSTEMATIC DESCRIPTION Superfamily PRODUCTACEA Family PRODUCTELLIDAE Schuchert & LeVene 1929 Subfamily CHONOPECTINAE Muir-Wood & Cooper 1960 Genus QUADRATIA Muir-Wood & Cooper 1960 Type species: Productus hirsutiformis Walcott 1884. Remarks: The specimens described below differ from those of Quadratza from the Mississippian rocks of Oklahoma and Nevada, in having a weak ventral sulcus and dorsal fold, better developed prostrate spines on the ventral visceral disc, faintly dendritic adductor scars, broader and flat lateral ridges in the brachial valve, and a pronounced adductor platform in the same valve. In addition, the present specimens are characterized by their bilobed cardinal process whose lobes are incised and Gloucester, Newcastle ryYGLOUCESTER WARDS RIVER OUPPER CHICHESTER SALISBURY L5450 -OBROWNMORE Fug. 2. Fossil locality map of the Berrico-Rawdon Vale and Brownmore districts, N.S.W. Proc. Linn. Soc. N.S.W., 104 (1), (1979) 1980 So JAKOG) 3 separated by a distinct median depression, instead of a knoblike process observed in Quadratia, but described by Muir-Wood and Cooper (1960, p.161) as probably incomplete. Most of these differences could be of generic significance, however it would be better to await further knowledge of the type species of Quadratza, before separate generic status is given to the present material. Quadratza engeli sp. nov. Fig. 3, 1-7 Material: NUF 4049-4057, 4355; holotype NUF 4053, paratypes NUF 4049, 4054- 4057, all from NUL 640 (the type locality) in the Berrico Creek Formation at Rawdon Vale. Derivation of name: In honour of Associate Professor B.A. Engel, Department of Geology, University of Newcastle, N.S.W. Diagnosis: A species of Quadratza characterized by having a distinct sulcus and fold, prostrate spines on ventral visceral disc and suberect to erect spines scattered on trail, a diamond-shaped dorsal adductor platform, a conspicuous breviseptum, and a moderate cardinal process with a median depression. Description: Exterior. Shell medium-sized, transverse, widest at straight hinge; interareas bearing fine striations; ears broad and flattened. Pedicle valve with a convex visceral disc and a short trail; umbo small, overhanging hinge; valve surface bearing faint concentric growth lines and weak rugae; prostrate spines rare, suberect to erect spines not arranged in rows on trail. Brachial valve with a concave visceral disc and a steep trail; interarea narrower than that of the pedicle valve; concentric growth lines and rugae well developed. Interior. Pedicle valve having an elliptical cavity of visceral disc well demarcated from impressions of external ears; anterior adductor scars either pear-shaped or elongate, elevated, placed between shallowly depressed posterior adductor scars; a shallow furrow separating adductor scars, and bearing a median ridge; diductor scars tear- drop-shaped in outline, ridged anteriorly and smooth posteriorly, enclosing adductor scars; a large shell thickening situated posterior to muscle field; two ridges borne near elongate hinge teeth, diverging at 16° from hinge. Brachial valve with an elevated adductor platform having a median depression; adductor scars weakly dendritic, spreading from the depression to lateral slopes of platform, bounded posterolaterally by two heavy ridges supporting cardinal process and diverging at 38°-40° from hinge ; anterior adductor scars broad, embracing small triangular posterior adductor scars; breviseptum non-sulcate, arrow-headed, dividing adductor scars; cardinal process with two high lobes shallowly incised ; a weak median ridge defined in deep depression separating the two lobes, detached from breviseptum by a small alveolus; sockets deep, bounded anteriorly by short socket ridges; narrow furrows separating these ridges from lobes of cardinal process; lateral ridges broad and flat, attached to socket ridges, following hinge margin, and dying out before reaching cardinal extremities. Measurements: Length of shell: 18.5mm-25.5mm; width of shell: 36mm-44mm. Remarks: Quadratza egregia Carter (1967) from the Mississippian Chapel Limestone of central Texas, U.S.A., is similar to the present species in the presence of ventral sulcus and dorsal fold. However, Carter’s species has smaller ears, overlapping growth lamellae and small spine bases in concentric rows on the pedicle valve, small closely set flattened teeth, and a lower bifid cardinal process supported by a narrow median septum. The Mississippian species Q. hirsutiformzs (Walcott) redescribed by Muir- Wood and Cooper (1960) from Oklahoma and Nevada, differs from Q. engelz in having stronger concentric growth lines and rugae, a more transverse cavity of the ventral visceral disc, thicker but shorter ridges arising near hinge teeth, a thinner breviseptum being not arrow-headed and originating from a low smooth platform, Proc. Linn. Soc. N.S.W., 104 (1), (1979) 1980 4 CARBONIFEROUS ARTICULATE BRACHIOPODS Proc. Linn. Soc. N.S.W., 104 (1), (1979) 1980. S. PEOU 5 and weaker ridges bounding the dorsal adductor scars postero-laterally. Q. rangariensis (Campbell, 1963) from the Tournaisian rocks of the Werrie and Belvue Synclines, N.S.W., has more numerous spines on the pedicle valve, broader but shorter adductor scars and smaller diductor scars in the same valve. The brachial valve of Q. rangariensis has a non-arrow-headed breviseptum developed from a flat to rounded posterior platform, and has undivided smooth adductor scars bordered postero-laterally by two short ridges arising from the central platform. Quadratia booniensis sp. nov. Fig.3, 8-18 Materzal: NUF 4037-4048; holotype NUF 4044, paratypes NUF 4045 and 4047, all from NUL 640 (the type locality) in the Berrico Creek Formation at Rawdon Vale. Derivation of name: After Boonie Doon farmhouse at Rawdon Vale. Diagnosis: A species of Quadratia having very distinct prostrate spines, suberect to erect spines in rows on ventral trail, a low dorsal platform, a thin breviseptum, and a small cardinal process with a shallow median depression. Description: Exterior. Shell medium-sized, transverse, with a maximum width at straight hinge; interareas flat, horizontally striated; ears subtriangular, flattened. Pedicle valve with a gently convex visceral disc and a short trail; umbo small, incurved over hinge; valve smooth on trail, bearing poorly developed concentric growth lines and rugae elsewhere; 7-8 spines on one row on trail, 2-3 spines defined on hinge margin. Brachial valve with a weakly concave visceral disc and a steep trail; interarea narrower than that of the pedicle valve; valve surface bearing prominent growth lines and rugae. Interior. Pedicle valve having an elliptical cavity of visceral disc well separated from impressions of external ears; adductor muscle field heart-shaped in outline; anterior adductor scars slightly elevated, faintly dendritic, inserted between smooth posterior adductor scars; a furrow dividing adductor scars; a weak ridge extending on floor of the furrow near posterior end of muscle field or from a shell thickening in one specimen to a short distance from anterior ends of adductor scars; diductor scars tear- drop-shaped, either smooth or faintly ridged; two distinct ridges arising in front of small and sharp hinge teeth, diverging at 14°-15° from hinge, being curved and obsolete along inner edges of ears. Brachial valve with a gently elevated adductor platform having a shallow median depression with a sharp breviseptum being obscure between adductors scars not clearly separated; a faint median ridge sitting in shallow depression between two incised lobes of cardinal process; two short but robust ridges supporting the process, diverging at 32°-34° from hinge; alveolus ill-defined; sockets deep, elongate; socket ridges developed from lobes of cardinal process by narrow furrows, lateral ridges broad and flat, running along hinge margin, fusing on ears. Fig. 3. 1-7. Quadratia engeli sp. nov. 1. Latex cast of a pedicle valve exterior; NUF 4049, paratype, x1. 2. Latex cast of an incomplete pedicle valve exterior showing a sulcus; NUF 4051, x1.5. 3. External mold of a brachial valve; NUF 4052, x1.1. 4-5. Internal mold of two pedicle valves; NUF 4055 and 4053, both paratypes, x1.1 and x1.5 respectively. 6. Latex cast of an incomplete brachial valve interior; NUF 4047, holotype, x1.3. 7. Enlargement of NUF 4047 showing a bilobate cardinal process whose incised lobes are separated by a median depression bearing a distinct ridge, x3. All from NUL 640, Rawdon Vale. 8-18. Quadratia booniensis sp. nov. 8-9. Latex cast of two pedicle valve exteriors; NUF 4038 and 4037, both x1. 10. External mold of an incomplete brachial valve; NUF 4041, x1. 11. Latex cast of NUF 4041, x1. 12. Internal mold of a pedicle valve; NUF 4045, paratype, x1.1. 13. Latex cast of NUF 4045, x1. 14. Internal mold of a pedicle valve; NUF 4044, paratype, xl. 15. Latex cast of NUF 4044, x1. 16. Latex cast of an incomplete brachial valve interior; NUF 4057, holotype, x1.5. 17. Enlargement of NUF 4057 showing a bilobate cardinal process with incised lobes separated by a median depression, x4.2. 18. Latex cast of an incomplete brachial valve interior; NUF 4355, x1.5. All from NUL 640, Rawdon Vale. Proc. Linn. Soc. N.S.W., 104 (1), (1979) 1980 6 CARBONIFEROUS ARTICULATE BRACHIOPODS Measurements: Length of shell: 18.5mm-25.5mm; width of shell: 31mm-44mm. Remarks: Quadratza booniensts is similar to Q. engelz mainly in the size and the shape of the shell, straight hinge, striated interareas, flattened ears, tear-drop outlines of ventral diductor scars, broad lateral ridges and incised lobes of the cardinal process. However, Q. engeli differs in having distinct sulcus and fold, less developed prostrate spines on the visceral disc and scattered suberect to erect spines not arranged in rows on the trail of the pedicle valve, elongate ventral adductor scars, a better developed dorsal adductor platform, a thicker and arrow-headed breviseptum, a stronger cardinal process supported on two heavier ridges, and a deeper median depression separating the two lobes of the process. Q. hzrsutzformzs (Walcott) redescribed by Muir-Wood and Cooper (1960) possesses a more pronounced concentric ornament, a more transverse cavity of ventral visceral disc, deeply impressed ventral adductor scars, a better developed alveolus, a shorter breviseptum springing from a smooth platform, and weaker ridges supporting the cardinal process. Q. egregza Carter (1967) is characterized by having distinct sulcus and fold, developed overlapping growth lamellae, several small spine bases on each side of ventral umbo close to posterior margin, closely set flattened teeth, and a narrow median septum supporting the cardinal process. The only other comparable species, Q. rangariensts (Campbell, 1963), has strongly developed spines on the pedicle valve, suboval to subtriangular ventral adductor scars being slightly embraced by the small diductor scars, a broad posterior dorsal platform from which arises a more distinct breviseptum, and weaker and shorter ridges bounding dorsal adductor scars. Family DICTYOCLOSTIDAE Stehli 1954 Subfamily DICTYOCLOSTINAE Stehli 1954 PRODUCTOID gen. et sp. nov. Fig. 4, 1-6 Materzal: NUF 4021-4023, all from NUL 545 in the unnamed formation at Brownmore. Description: Exterior. Shell large, concavo-convex; hinge line short; interareas concave; ornament of costae forming a reticulation with weak concentric ridges on umbonal region, broad concentric lamellae (on brachial valve only) , growth lines and spines. Pedicle valve with a small umbo, a shallow sulcus, a broad visceral disc and a long trail; costae subrounded to flat, branching, curved posteriorly on steep lateral slopes, and wrapping high knoblike structures on small ears; spines suberect to erect, big and long. Brachial valve with a short umbo, a low fold, and small ears bearing deep depressions for the reception of knoblike structures on ventral ears; costae Fig. 4. 1-6. Productoid gen. et sp. nov. 1. Latex cast of a pedicle valve exterior; note the distinct knoblike structure on one ear; NUF 4021, figured specimen, x0.8. 2. Latex cast of an incomplete pedicle valve exterior; NUF 4023, x1.6. 3. Latex cast of a cardinal area and umbonal regions of pedicle valve and brachial valve exteriors; NUF 4023, x2. 4-5. External mold of a brachial valve showing the broad visceral disc (4) and trail (5) ; NUF 4023, x0.9 and x0.8 respectively. 6. External mold of a brachial valve; note the distinct reticulate and lamellose ornament; NUF 4022, figured specimen, x0.9. All from NUL 545, Brownmore. 7-17. ‘Camarotoechia’ subtrigonalis sp.nov. 7. Latex cast of a pedicle valve exterior; NUF 4059, x3. 8.Latex cast of a brachial valve exterior; NUF 4058, x2.6. 9-10. Internal mold of two pedicle valves; NUF 4062 and 4061, both paratypes, x2.8 and x3.5 respectively. 11. Latex cast of NUF 4061, x4. 12. Internal mold of a brachial valve; NUF 4066, holotype, x4.5. 13. Latex cast of NUF 4066, x3.5. 14-15. Internal mold of a brachial vaive and latex cast of same; NUF 4065, paratype, x4.5 and x4.9 respectively. 16-17. Internal mold of two brachial valves; NUF 4067, paratype and NUF 4068, x4.2 and x5 respectively. All from NUL 723, except NUF 4059 and 4062 from NUL 882, Rawdon Vale. Proc. Linn. Soc. N.S.W., 104 (1), (1979) 1980 S. PEOU (1979) 1980 Proc. Linn. Soc. N.S.W., 104 (1) 8 CARBONIFEROUS ARTICULATE BRACHIOPODS rounded, increasing by intercalation; big spines rare, faint spines on long trail. Internal structures of both valves unknown. Measurements: Length of shell: 43mm-51mm; width of shell: 52mm-56mm. Remarks: Only three specimens are at present available for the description. The brachial valve exhibits three different ornamental zones: (a) a reticulate zone occupying the umbonal region and being produced by the intersection between concentric ridges and radial costae; (b) a lamellose zone situated between the other two, covering over 80% of valve surface, and bearing concentric lamellae with growth lines interrupting the radial costae, and rare spines; and (c) a narrow spinose zone on trail, bearing fine spines. Determination of the generic affinities of the species described above is difficult, due to the lack of specimens detailing the internal structures. This form is referred to the subfamily Dictyoclostinae only on the basis of its reticulate umbonal region and costate trail. A precise assignment must await detailed study of further material. The external ornamentation of the brachial valve, especially the broadly developed concentric lamellae traversing the radial costae, and the knoblike structures on the ears of the pedicle valve are the most distinctive features which could separate the present genus from all other productid genera. Superfamily RHYNCHONELLACEA Family CAMAROTOECHIIDAE Schuchert & LeVene 1929 Subfamily CAMAROTOECHIINAE Schuchert & LeVene 1929 Genus CAMAROTOECHIA Hall & Clarke 1893 Type species: Atrypa congregata Conrad 1841. Remarks: Numerous workers have recorded species of Camarotoechia from the Devonian and Carboniferous of Australia. The genus has yet to be unequivocally recorded from the southern hemisphere, or for that matter from Carboniferous rocks, so the following species, a more strongly-ribbed form than the type species C. congregata (Conrad, 1841), is referred to the genus as a procedural gambit until such time as the systematics of Australian Devonian and Carboniferous rhynchonellaceans are better known. ‘Camarotoechia’ subtrigonalis sp. nov. Fig. 4, 7-17 Material: NUF 4058-4070; holotype NUF 4066, paratypes NUF 4061, 4062, 4065 and 4067, from NUL 723 (the type locality) and 882 in the Berrico Creek Formation at Rawdon Vale. Derivation of name: subtrigonalis refers to the not completely trigonal shell outline. Diagnosis: A species of ‘Camarotoechia’ with a small and plicate shell being subtrigonal in outline, a feebly uniplicate anterior commissure, a V-shaped dorsal septalium supported by a short median septum, and an unsplit to split hinge plate bearing two short crura. Description: Exterior. Shell unequally biconvex, generally wider than long, ornamented with coarse rounded costae. Pedicle valve moderately convex; umbo slightly incurved; sulcus distinct, shallow, commencing in front of umbo, having 3 to 5 plicae; lateral slopes not steep, 4-6 plicae on each slope; concentric growth lines poorly developed. Brachial valve more convex than pedicle valve; umbo strongly incurved ; fold low, having 4 plicae; lateral slopes steep, each slope bearing 5-6 plicae. Interior. Pedicle valve with ill-defined adductor scars, smooth elongate diductor scars Proc. Linn. Soc. N.S.W., 104 (1), (1979) 1980 S. PEOU 9 tapering posteriorly and sitting between two short and sharp dental lamellae; diverging angle of the lamellae 28°-34°; teeth strong, supported on dental lamellae. In brachial valve, adductor scars smooth, separated by a sharp median septum extending about one-half total length of valve; septalium shallow; sockets deep and elongate, bounded posteriorly by outer edges of hinge plate. Measurements: Length of shell: 6mm-12.5mm; width of shell: 7mm-15mm. Remarks: ‘Camarotoechia’ subtrigonalis is similar to C. sp. Campbell (1957) and C. sp. A. Roberts (1963) respectively from Babbinboon and Lewinsbrook, N.S.W., particularly in the shape and size of the shell, and the number of plicae in the ventral sulcus. C. sp. differs from the described species in the possession of longer dental lamellae and developed rays on crura. C. sp. A. has a more transverse shell, fewer plicae on dorsal lateral slopes, a shorter median septum and narrower sockets in the brachial valve. C. sp. B_ Roberts (1965) from Trevallyn, N.S.W.., is characterized by a larger, subequally biconvex shell ornamented with angular plicae on the lateral slopes, a globular to rounded brachial valve, and a shorter dorsal median septum. In addition, C. amnica and C. septima Veevers (1959) respectively from the Carnarvon and Bonaparte Gulf Basins, Western Australia, have a pentagonal shell, a deeper ventral sulcus with fewer plicae, and a weaker dorsal median septum. Superfamily ENTELETACEA Family ENTELETIDAE Waagen 1884 Subfamily SCHIZOPHORIINAE Schuchert & LeVene 1929 Genus SCHIZOPHORIA King 1850 Type species: Conchylzolithus (Anomites) resupinatus Martin 1809. Schizophoria subelliptica sp. nov. Fig.5, 1-7 Material: NUF 3825-3847; holotype NUF 3839, paratypes NUF 3829-3831, 3840- 3842, all from NUL 514 (the type locality) in the Berrico Creek Formation at Rawdon Vale. Derivation of name: subelliptica refers to the not completely elliptical shell outline. Diagnosis: A species of Schizophorza with a subelliptical shell outline, ventral adductor scars on a high elevation and deeply depressed diductor scars, strong pallial markings, and two subparallel main pallial trunks arising at anterior ends of ventral adductor scars. Description: Exterior. Shell transverse, widest at about midlength; cardinal extremities well rounded; hinge about two-thirds to four-fifths maximum width of shell; capillae rounded, increasing by both intercalation and bifurcation, numbering 40 per 10mm on anterior median portion of shell; growth lines developed, spine bases not observed. Pedicle valve convex on umbonal region, concave anteriorly; beak small and short; lateral slopes steep; sulcus shallow, not reaching umbo; interarea broad; delthyrium open, triangular, as wide as high. Brachial valve strongly convex; lateral slopes very steep; fold indistinct; cardinal extremities gently concave; interarea narrow, bearing faint horizontal striations; notothyrium slightly wider than high. Interior. Pedicle valve with robust dental plates bordering muscle field laterally and diverging at 58°-64°; teeth strong; diductor scars tapering posteriorly, either smooth or weakly striated, adductor scars smooth, narrowly elongate, sitting on flanks of a heavy longitudinal elevation; a shallow furrow defined on the elevation in some specimens, dividing adductor scars; vascula genitalia on anterior and lateral sides of Proc. Linn. Soc. N.S.W., 104 (1), (1979) 1980 10 CARBONIFEROUS ARTICULATE BRACHIOPODS muscle field. In brachial valve, brachiophores projecting from either side of notothyrial cavity, diverging at 62°-76°; sockets elongate, with a subrounded floor bearing transverse grooves which extend to distinct fulcral plates; cardinal process consisting of a high median lobe and two lateral lobes separated by deep furrows; lamellose myophores developed in the process; anterior adductor scars shallowly depressed, separated from small posterior adductor scars by two low broad ridges; adductor scars finely striated; a large swelling concave posteriorly, located between adductor scars, bearing a rounded median ridge; postero-lateral sides of muscle field pustulose; two main parallel trunks branching anteriorly, arising either from anterior ends of posterior adductor scars or from the broad ridges separating the anterior and posterior adductor scars; another two subparallel trunks borne at anterior ends of anterior adductor scars; secondary pallial markings prominent in both valves. Measurements: Length of shell: 19.5mm-27.5mm; width of shell: 26.5mm-33mm. Remarks: Schizophoria subelliptica resembles S. verulamenszs Cvancara (1958) from Barrington, N.S.W., in the shape of the shell, and subparallel pallial trunks defined in the pedicle valve. It is distinguished from Cvancara’s species by its more numerous capillae, smaller diverging angles of dental plates and brachiophores, narrower ventral adductor scars, better developed secondary pallial markings, sockets and fulcral plates bearing transverse grooves, and trilobate cardinal process containing lamellose myophores. S. sp. cf. S. resupinata (Martin) described by Roberts (1971) from Bonaparte Gulf Basin, northwestern Australia, differs from the present species in having a shorter hinge, a broader ventral muscle field, a larger dorsal median swelling, a larger diverging angle of the brachiophores, and a single to multi-lobed cardinal process. S. resupznata (Martin) described by Sarycheva et al. (1963) and S. altaica Besnossova (1968) respectively from Kuznetsk Basin and eastern Kazakhstan, U.S.S.R., have a longer hinge and a less convex brachial valve. In addition, S. resupinata has fewer radial ribs, a weak dorsal median furrow, broader ventral muscle scars and stronger dorsal brachiophores; S. altazca is larger and has a rounded shell, an almost flat pedicle valve and no developed ventral sulcus and dorsal fold. Two species, S. antzqua Solle and S. striatula (Schlotheim), described by Pocock (1966) from the Devonian rocks of Germany, are characterized by having an elliptical to quadrate shell with a better developed radial ornament, an angular dorsal median septum, and fewer main pallial trunks in the brachial valve. Also, S. antzqua is smaller and possesses broader ventral muscle scars and oval dental sockets; S. strzatula exhibits stronger ventral sulcus and dorsal fold, and better developed myophores. Fig. 5. 1-7. Schizophoria subelliptica sp.nov. 1. Latex cast of a pedicle exterior; NUF 3825, x1.6. 2. Latex cast of a brachial valve exterior; NUF 3827, x2.2. 3. Internal mold of a pedicle valve; NUF 3832, x1.2. 4. Latex cast of NUF 3832, x1.3. 5. Internal mold of a pedicle valve; NUF 3831, paratype, x1. 6. Internal mold of a brachial valve; NUF 3839, holotype, x1.1. 7. Latex cast of NUF 3839, x1.2. All from NUL 514, Rawdon Vale. 8-14. Podtsheremia fasciculata sp. nov. 8. Latex cast of a pedicle valve exterior; NUF 4152, paratype, x2. 9. Latex cast of a brachial valve exterior with an apical portion of pedicle valve exterior; NUF 4151, paratype, x1.7. 10. Latex cast of a brachial valve exterior; NUF 4155, x2. 11. Internal mold of a pedicle valve; NUF 4157, x1.7. 12. Latex cast of NUF 4157, x1.9. 13. Internal mold of a brachial valve and a posterior portion of pedicle valve; NUF 4341, holotype, x1.5. 14. Latex cast of NUF 4341, x1.6. All from NUL 628, Rawdon Vale, except NUF 4155 from NUL 861, Berrico. 15-21. Brachythyres cobarkensis sp. nov. 15. Latex cast of a pedicle valve exterior; NUF 4225, x2.1. 16. Latex cast of a brachial valve exterior; NUF 4226, x1.7. 17-19. Internal mold of three pedicle valves; NUF 4231, paratype, x1; NUF 4234, holotype, x1; and NUF 4233A, x1.1. 20. Internal mold of a brachial valve ; NUF 4243, paratype, x1.1. 21. Internal mold of a brachial valve with a posterior portion of pedicle valve ; NUF 4232B, paratype, x1. All from NUL 517, except NUF 4226, 4243 and 4232 B from NUL 515, Rawdon Vale. Proc. LINN. Soc. N.S.W., 104 (1), (1979) 1980 11 S. PEOU Proc. Linn. Soc. N.S.W., 104 (1), (1979) 1980 12 CARBONIFEROUS ARTICULATE BRACHIOPODS Superfamily SPIRIFERACEA Family SPIRIFERIDAE King 1846 Genus PODTSHEREMIA Kalashnikov 1966 Type species: Podtsheremza prima Kalashnikov 1966 Podtsheremza fasciculata sp. nov. Fig.5, 8-14 Material: NUF 4341, 4151-4152, 4155, 4157; holotype NUF 4341, paratypes NUF 4151, 4152, from NUL 628 (the type locality) in the Berrico Creek Formation at Rawdon Vale, and NUL 861 in the same formation at Berrico. Derivation of name: fasciculata refers to the fasciculate costae on shell. Diagnosis: A species of Podtsheremza characterized by its biconvex shell with rounded costae frequently branching and forming fascicles on lateral slopes, ventral sinus with a simple median costae and branching costae, dorsal fold bearing a median furrow, and rows of denticles along hinge. Description: Exterior. Shell triangular in outline, transverse, mucronate, widest at hinge; mucros flat to slightly concave, well developed in small specimens; radial costae, fine lirae and concentric growth lines forming shell ornament; 20 to 23 fasciculate costae on each steep lateral slope, 6 to 7 simple costae on postero-lateral extremities, fascicles of 3 to 4 ribs on either side of ventral sinus and dorsal fold. Pedicle valve with a moderate and incurved umbo, a flat to weakly concave apsacline interarea ornamented with faint horizontal and vertical striations: delthyrium open, with an angle of 68°; sinus shallow, reaching umbo;,sinal angle about 19°. Brachial valve with a short umbo overhanging a narrow interarea; fold costate, conspicuous. Intertor. Pedicle valve with high and sharp dental lamellae, supporting elongate teeth; denticles arranged in rows on either side of base of a shallow delthyrial cavity, oriented perpendicular to hinge; adminicula short and sharp, diverging at 10°-12°; adductor scars narrowly elongate, finely striated, and divided by a weak myophragm; diductor scars also elongate, smooth but faintly striated posteriorly; two ridges ill- defined between the two muscle scars; vascula genitalia observed on lateral sides of muscle field. Brachial valve with shallow sockets, distinct inner socket ridges diverging at 82° and terminating short crura; cardinal process supported on these ridges, containing up to 18 tiny vertical plates; adductor scars of two pairs: lateral pairs subtriangular; median pairs quadrangular, well impressed, divided by a fine median ridge; the two pairs being smooth, separated by two ridges corresponding to furrows which border external fold. Measurements: Length of shell: 12mm-17mm; width of shell: 17mm-27mm. Remarks: When compared with the type species, Podtsheremia prima Kalashnikov (1966) from northern Urals, U.S.S.R., P. fasciculata has a more transverse shell with a hinge reaching its maximum width and mucronate cardinal extremities. P.? humilicostata and P.? thomast Roberts (1971) from the Bonaparte Gulf Basin, northwestern Australia, are distinguished from the present species by their fewer costae on lateral slopes and larger angle of adminicula. In addition, P.? humilzcostata has a smaller delthyrial angle, but a larger sinal angle; P. ? thomasz has a larger angle of inner socket ridges and more numerous vertical plates in the cardinal process. Family BRACHYTHYRIDIDAE Fredericks 1919 (1924) Genus BRACHYTHYRIS McCoy 1844 Type species: Spirifera ovalis Phillips 1836. Proc. Linn. Soc. N.S.W., 104 (1), (1979) 1980 S. PEOU 13 Brachythyris cobarkensis sp. nov. Fig.5, 15-21 Material: NUF 4225-4243; holotype NUF 4234, paratypes NUF 4231, 4232 and 4243, from NUL 517 (the type locality) and 515 in the Berrico Creek Formation at Rawdon Vale. Derivation of name; After Cobark River in Rawdon Vale. Diagnosis: A species of Brachythyris with a parasulcate anterior commissure, broad ventral muscle field from which radiate strongly developed pallial markings, robust dental ridges supporting heavy teeth, large socket plates attached to subtriangular cardinal process. Description: Exterior. Shell unequally biconvex, with 10-12 broad and flat plicae on each lateral slope and developed concentric growth lines; plicae bifurcating, simple on cardinal extremities. Pedicle valve strongly convex on umbonal region; umbo erect, small, sharply pointed; cardinal areas broad and concave; delthyrium open, triangular, wider than high; delthyrial angle 63°; sinus shallow, reaching umbo, costae in sinus not observed, sinal angle about 9°. Brachial valve with a small and short umbo, a distinct fold bearing a weak median furrow. Interior. Pedicle valve thickened on umbonal region; muscle scars well impressed, variable in outline, occupying about one-third valve surface; adductor scars narrowly elongate, ridged, divided posteriorly by a distinct myophragm; diductor scars broad, fusiform, having a deep posterior median furrow. In brachial valve, socket plates enclosing elongate sockets, adductor scars finely striated and divided by a weak median ridge; cardinal process having up to 32 branching, bifurcating and simple thin vertical plates; pallial markings weakly developed. Measurements: Length of shell: 24mm-29mm; width of shell: 23mm-28mm. Remarks: Brachythyris solida Campbell (1963) from the Belvue Syncline, N.S.W.., is similar to B. cobarkensis in the width/length ratio of shell, and the strong convexity of pedicle valve towards the umbo. However, it differs in having more numerous but narrower costae on the lateral slopes, and a subtriangular cardinal process containing fewer vertical plates. B. pseudovalis Campbell (1957) and B. elliptica Roberts (1963) respectively from Babbinboon and Lewinsbrook, N.S.W., are larger and have better developed costae on the lateral slopes, weaker sinus and fold, a larger sinal angle, and more numerous vertical plates in the cardinal process. B. planulata Roberts (1971) from the Bonaparte Gulf Basin, northwestern Australia, is characterized by its more transverse shell, uniplicate commissure, smaller delthyrial angle, larger sinal angle, and fewer vertical plates in the cardinal process. The species described by Carter (1967) as B. chouteauensts (Weller) and B. gzrty: (Branson) from the Mississippian Chapel Limestone of central Texas, exhibit better developed costae being usually simple, and lack a ventral myophragm. In addition, B. chouteauensis has a uniplicate anterior commissure, costate ventral sulcus and dorsal fold, smaller teeth and no developed dental ridges; B. gzrtyz has a subequally biconvex shell, narrower dental ridges and no developed dorsal median ridge. B. peculzar’s (Shumard) described by Weller (1914) from the Mississippian Chouteau Limestone at Mississippi Valley Basin, is smaller and possesses narrower cardinal areas, a rounded ridge dividing the lateral slopes into two regions, and fewer plicae being only simple and rounded. LOCALITIES OF FIGURED SPECIMENS Locality number Grid references NUL 514 738 453 Cobark 1:31680 Sheet Proc. Linn. Soc. N.S.W., 104 (1), (1979) 1980 14 CARBONIFEROUS ARTICULATE BRACHIOPODS NUL 515 740 455 Cobark 1:31680 Sheet NUL 517 736 490 Cobark 1: 31680 Sheet NUL 545 625 077 Dungog 1: 63360 Sheet NUL 628 732 499 Cobark 1:31680 Sheet NUL 640 708 462 Cobark 1: 31680 Sheet NUL 723 737 553 Cobark 1:31680 Sheet NUL 861 851 303 Gloucester 1 :63360 Sheet NUL 882 707 463 Cobark 1:31680 Sheet NU = University of Newcastle ACKNOWLEDGEMENTS I am indebted to Professor B. Nashar for her continuing support, and to Associate Professor B. A. Engel for his helpful advice and critical reading of the manuscript. Facilities provided by the Department of Geology of the University of Newcastle, N.S.W., are also acknowledged. References BrsnossovA, G. A., 1968 — Schizophoriidae. In Sarycheva, T. G., (ed.), Brakhiopody verkhnego Paleozoya vostochnogo Kazakhstana [Brachiopods from the Upper Palaeozoic of eastern Kazakhstan]. Trudy paleont. Inst. 121:53-54 (Russian). CAMPBELL, K. S. W., 1957. — A lower Carboniferous brachiopod-coral fauna from New South Wales. J. Paleont. 36 (1) :34-98. ———, and ENGEL, B. A., 1963. — The fauna of the Tournaisian Tulcumba Sandstone and its members in the Werrie and Belvue Synclines, N.S.W.J. geol. Soc. Aust: 10(1) :55-122. ——, and McKE iar, R. G., 1969. — Eastern Australian Carboniferous invertebrates: sequence and affinities. Pp.77-119 zn Campbell, K. S. W., (ed.), Stratigraphy and Palaeontology. Canberra: Aust. Nat. Univ. Press. ———, and McKeELvey, B. C., 1972. — The geology of the Barrington district, N.S.W. Pacific Geol. 5: 7- 43, ———, and RopsertTs, J., 1969. — Faunal sequence and overseas correlation (Carboniferous). In Packham, G.H., (ed.), The geology of New South Wales. J. geol. Soc. Aust. 16 (1) :261-264. CARTER, J. L., 1967. — Mississippian brachiopods from the Chapel Limestone of Central Texas. Bull. Amer. Paleont. 23 (238) : 253-449. ConrabD, T. A., 1841. — On the paleontology of the State of New York. N.Y. State Geol. Surv. 5th Ann. Rept: 25-27. Cvancara, A. M., 1958. — Invertebrate fossils from the lower Carboniferous of New South Wales. /. Paleont. 32(5) : 846-888. ; DRIscott, E. G., 1960. — Geology of the Mundubbera district. Pap. Dep. Geol. Univ. Qd 5(5) : 27p. Jones, P. J., et al., 1973. — Correlation chart for the Carboniferous System of Australia. Bull. Bur. Miner. Resour. Geol. Geophys. Aust. 156A: v+ 40p. KALASHNIKOV, N. V., 1966. — Brakhiopody Nizhnego Karbona Verkhnei Pechory na Severnom Urale — Stratigrafia i Paleontologii severo-vostoka evropeiskoi chasti SSSR [Lower Carboniferous brachiopods of the upper Pechora in the northern Urals. Jn Stratigraphy and paleontology of the northeast European regions of the U.S.S.R.]. Akad. Nauk. SSSR, Komi Filial, Inst. Geol. 28-61 (Russian) . McDona_p, L. K., 1972. — The geology of the Brownmore district, New South Wales. Kensington: University of New South Wales, B.Sc. thesis, unpubl. , McKELLAR, R. G., 1967. — The geology of the Cannindah Creek area, Monto district, Queensland. Publs. geol. Surv. Qd 331: 38p. Muir-Woop, H., and Cooper, G. A., 1960. — Morphology, classification and life habits of the Productoidea (Brachiopoda). Mem. geol. Soc. Amer. 81: 447p. Peou, S., 1977. — Stratigraphy, palaeoecology and taxonomy of the Rhzpzdomella fortemuscula and Balakhonia rawdonvalensis faunas in the region north of Newcastle, New South Wales. Newcastle: University of Newcastle, Ph.D. thesis, unpubl. ——, and EncEL, B. A., 1979. — A Carboniferous fauna from Rawdon Vale, New South Wales. Alcheringa 3 (2) : 141-157. Proc. Linn. Soc. N.S.W., 104 (1), (1979) 1980 Sp. OL) 15 Pocock, Y. P., 1966. — Devonian schizophoriid brachiopods from western Europe. Palaeont. 9 (3) :381- 412. RoseErTs, J., 1963. — A lower Carboniferous fauna from Lewinsbrook, New South Wales. J. Proc. R. Soc. N.S.W. 97: 1-31. ——, 1965. — A lower Carboniferous fauna from Trevallyn, New South Wales. Palaeont. 8(1) : 54-81. ——, 1971. — Devonian and Carboniferous brachiopods from the Bonaparte Gulf Basin, northwestern Australia. Bull. Bur. Mener. Resour. Geol. Geophys. Aust. 122: ix + 319p. ——, 1975. — Early Carboniferous brachiopod zones of eastern Australia. J. geol. Soc. Aust. 22(1) : 1-31. ——, 1976. — Carboniferous chonetacean and productacean brachiopods from eastern Australia. Palaeont. 19(1) : 17-77. , et al., 1976. — Late Carboniferous marine invertebrate zones of eastern Australia. Alcheringa 1 (2) : 197-225. SARYCHEVA, T. G., et al., 1963. — Brakhiopody i paleogeografia Karbona Kuznetskoi kotloviny [ Carboniferous brachiopods and palaeogeography of the Kuznetsk Basin]. Trudy paleont. Inst. 95: 3-406 (Russian) . VEEVERS, J., 1959. — Devonian and Carboniferous brachiopods from northwestern Australia. Bull. Bur. Miner. Resour. Geol. Geophys. Aust. 45: 220p. WELLER, S., 1914. — The Mississippian Brachiopoda of the Mississippi Valley Basin. Monogr. geol. Surv. Ill. 1: 1-508. WHITFORD, D. J., 1971. — The geology of the Stratford-Berrico district, New South Wales. Newcastle: University of Newcastle, B.Sc. thesis, unpubl. Proc. Linn. Soc. N.S.W., 104 (1), (1979) 1980 The Species of the Indo-West Pacific Genus Calumza (Pisces: Eleotridae) H. K. LARSON and D. F. HOESE (Communicated by J. R. PAXTON) Larson, H. K., & Hoess, D. F. The species of the Indo-west Pacific genus Calumia (Pisces: Eleotridae) . Proc. Linn. Soc. N.S.W. 104 (1), (1979) 1980:17-22. A brief diagnosis of the marine fish genus Calumza is given. Eleotrzs godeffroy: Ginther is placed in Calumza as a senior synonym of the type species C. bzocellata Smith. Calumia profunda is described as a new species from the Solomon Islands and the New Hebrides. The species of Calumza are among the smallest-sized eleotrids known, and Calumia is one of the few eleotrid genera found on coral reefs. It is suggested that the genus Allomicrodesmus be transferred to the family Eleotridae. H. K. Larson and D. F. Hoese, Department of Ichthyology, The Australian Museum, P.O. Box A285, Sydney South, Australia 2000; manuscript received 15 June 1978, accepted in revised form 21 February 1979. INTRODUCTION The family Eleotridae contains about forty genera of which only four, Allomicrodesmus, Xenisthmus, Calumia and an undescribed genus related to Xenisthmus, are confined to coral reefs of the Indo-west Pacific. The remaining genera are inhabitants of fresh or brackish water. Allomzcrodesmus has been included in the family Microdesmidae (Schultz 1966), but it is apparent that the genus belongs elsewhere (Dawson, pers. comm.). Re-examination of the type and an additional specimen of Allomizcrodesmus dorotheae from the Great Barrier Reef shows that the species has six branchiostegal rays characteristic of eleotrids; provisionally therefore we place Allomicrodesmus in the family Eleotridae. The undescribed genus and Allomicrodesmus are both monotypic and Xenzsthmus contains about 10 species. Previously only a single species of Calumza was recognized. Examination of recently- collected material has indicated that a second undescribed species of Calumza exists. While examining types of gobioid fishes, it was discovered that C. bzocellata is a senior synonym of Eleotris godeffroyi Gunther (1877). Inaccuracies in the original description have prevented adequate identification of the species. All of the marine eleotrid species are relatively small sized, ranging from 15 to 35 mm SL as adults. Few specimens have been collected and little is known of their distribution. For example, the species described here is known from only three specimens. While most marine eleotrids are highly specialized forms, Calumza maintains a typical eleotrid physiognomy, with a broad scaled interorbital and a short robust body. The other genera are elongate with a protrusible lower jaw, presumably for burrowing in sand. METHODS Counts and measurements follow those given by Hubbs and Lagler (1958), except as listed below. The lateral scale count is the number of scale rows from the upper pectoral base to the end of the hypural plate. The transverse scale count (TRB) is taken from the anal base upward and backward to the base of the second dorsal fin. Colour notes of C. godeffroy: are based on freshly-collected specimens from the Great Proc. Linn. Soc. N.S.W., 104 (1), (1979) 1980 18 SPECIES OF CALUMIA Barrier Reef. Specimens studied are deposited in the following institutions: Australian Museum, Sydney, AMS; Bernice P. Bishop Museum, Honolulu, BPBM; British Museum (Natural History), London, BMNH; and J.L.B. Smith Institute of Ichthyology, Rhodes University, Grahamstown, RUSI. The osteology was studied from a single cleared and stained specimen of C. godeffroyy. SYSTEMATIC DESCRIPTION Calumia Smith 1958 Calumza Smith 1958: 148 (type species: C. bzocellata Smith 1958, by original designation) . Calumia is readily distinguished from other eleotrids by the following combination of characters. Head depressed. Top of head, cheeks and opercles scaled ; an enlarged scale between eyes. Anterior nostril elongate, positioned on snout just behind upper lip. Gill opening broad, extending forward to below preoperculum or eye. Pectoral rays unbranched. No lateral line head pores. Sensory papillae sparse, in characteristic rows (Fig. 3). Branchiostegal rays 6. First dorsal rays VI. Second dorsal rays I, 6-8. Anal rays I, 6-7. Segmented caudal rays typically 15. Lateral scale rows 21- 25. Adults small sized, reaching 15 to 20 mm SL. Vertebrae 10 + 15. Caudal skeleton with two epurals. First dorsal pterygiophore inserted after third neural spine; second and third between fourth and fifth neural spines; fourth and fifth between fifth and sixth neural spines; sixth between sixth and seventh neural spine; pterygiophore from spine in second dorsal fin between seventh and eighth neural spine, without any interneural gap. Dorsal postcleithrum present. In genera] appearance Calumza is most similar to Ophzocara. Calumiza differs from that genus in lacking head pores, the arrangement of sensory papillae, the simple pectoral rays and the small size of adults. KEY TO SPECIES 1. Mouth short, reaching to below anterior margin of eye. Gill opening extends forward to below posterior preopercular margin. Caudal fin with two enlarged black spots, one at upper caudal base and one on lower caudal base. Tongue tip pointed or slightly rounded. Pectoral rays 16-17. Gill rakers on outer face of lower part of first arch 6; short and stubby. Pelvic rays branched. Third and fourth dorsal spines longer than other spines ............... C. godeffroy: (Gunther) 2. Mouth longer, reaching to below posterior half of pupil. Gill opening broader, extending forward to below middle or posterior end of pupil. Caudal fin without enlarged black spots: Tongue tip bilobed. Pectoral rays 14-15. Elongate and pointed gill rakers on outer face of first arch 13-14. Pelvic rays unbranched. Second dorsallspime/lomgese, ais cia ences Mattes ec aia eee C. profunda n.sp. Calumia godeffroy: (Gunther) Fig. 1 Eleotris godeffroy: Gunther 1877: 188, p. 122, fig. B, (Raiatea, Tahiti) . Calumia biocellata Smith 1958: 148, p. II, K and fig. 8 (Zanzibar). Counts of the holotype of Eleotris godeffroy: are indicated with an asterisk and counts of the holotype of C. bzocellata are indicated with a plus. First dorsal rays VI (in 6)* +. Second dorsal rays I, 6(3)* +; I, 7(3). Anal rays I, 6 (3) +; I, 7 (3)*. Pectoral rays 16 (2); 17 (4)*+. Lateral scale count 21 (1); 22 (4)*+; 23 (1). Transverse backward count 7 (3); 8 (2) +. Segmented caudal rays 15 (6) * +. Lower gill rakers on outer face of first arch 6 (4) +. Predorsal scales 7 (4) *; 8 (1); 9 (1) +. Proc. Linn. Soc. N.S.W., 104 (1), (1979) 1980 H.K. LARSON AND D. F. HOESE 19 Fig. 1. Calumia godeffroy:; holotype of C. bzocellatus (after Smith, 1958). Smith (1958) has described the colouration of this species, under the name Calumza brocellata, in detail. Across the nape is a transverse dark band which begins above the end of the opercle and may be intensified as a distinct black blotch on either side of the nape. The body has five greyish black transverse bands, and a trace of a sixth incomplete band at the base of the caudal rays. At the base of each pelvic fin is a small black spot. The vertical fins are black. The two caudal spots are darkest at the caudal base and tend to fade posteriorly into the dusky anterior half of the caudal. In fresh material from the Great Barrier Reef the posterior third of the second dorsal and anal fins and the posterior half of the caudal fin are yellowish orange. This species is distinctive in the features given in the key and has been adequately described by Smith (1958). Although the original description of Eleotris godeffroyz is brief, the species is well figured. Unfortunately, Gunther (1877) did not mention or figure the two black caudal spots, but only indicated that the vertical fins are black. Examination of the holotype shows the spots and the five transverse body bands. Calumia godeffroy? is a small-sized species, reaching a maximum size of 20 mm SL. The species is known from several localities in the western Indian Ocean (Smith, 1958), Christmas Island just south of Java (Allen, 1979) the Great Barrier Reef, Australia and Tahiti, and is undoubtedly widespread in the Indo-west Pacific. Smith (1958) reported collecting the species at low tide in muddy or weedy areas. On the outer islands of the Great Barrier Reef, the species was collected among coral and rubble at depths of 7 to 30 m. ' Material Examined: BMNH 1877.4.26.8, a 20.5 mm female, holotype of Eleotrzs godeffroyz, Tahiti. RUSI 217, 1 (29), holotype of Calumza biocellata, Zanzibar. AMS I. 19472-086, 2(14-19) , Yonge Reef, Great Barrier Reef, Australia, 7-15 m. I. 19480- 026, 2(19-22) , Yonge Reef, Great Barrier Reef, Australia, 20-30 m. Calumza profunda sp. nov. Figs 2, 3 and 4 Diagnosis: Mouth enlarged, reaching to below middle of eye or slightly beyond. Gill opening broad, extending forward to below middle to posterior end of pupil. Elongate rakers on outer face of first gill arch 13-14. Pectoral rays 14-15. Lateral scale count 24- 25. Transverse scale count (TRB) 8. Second spine of first dorsal fin the longest and slightly prolonged. Seven dark brown transverse bands on body. Caudal fin without Proc. Linn. Soc. N.S.W., 104 (1), (1979) 1980 20 SPECIES OF CALUMIA enlarged black spots. Anterior tip of tongue bilobed. Pelvic rays unbranched. Outer row of jaw teeth not enlarged. Description: Based on holotype and two paratypes. Counts of holotype indicated with an asterisk. Measurements of types given in Table 1. First dorsal rays VI (3) *. Second dorsal rays I, 6 (1); I, 7 (2)*. Anal rays I, 7 (3)*. Pectoral rays 14 (1), 15 (2)*. Lower rakers on outer face of first arch 13 (2)*, 14 (1). Segmented caudal rays 14 (1), 15 (2)*. Lateral scale count 24 (1), 25 (2)*. Transverse scale count (TRB) 8 (3) *. Predorsal scales 8 (3) *. A small species maturing at about 15 to 18 mm SL. Body compressed posteriorly, more rounded anteriorly. Head large, 36 to 39% of SL, distinctly depressed. Eyes lateral, top of eye forming top of head profile, about 4 in head length. Jaws terminal, slightly oblique; end of jaws below posterior half of pupil or below midpupil. Tip of lower jaw protrudes slightly before tip of upper jaw. Anterior nostril an elongate tube about equal to pupil diameter, positioned just behind upper lip. Posterior nostril a raised rim midway between anterior nostril and front of eye. Snout about equal to eye, with slight protuberance on dorsal profile before eye. Dorsal and anal fins short based, shorter than caudal peduncle length. First dorsal fin slightly elongate with a pointed distal margin, formed by the elongate second dorsal spine. Dorsal and anal rays elevated becoming progressively longer posteriorly, giving fins pointed posterior margins; tips of fins reach to base of caudal rays. Pectoral rays slender, unbranched, middle rays longest reaching to above anterior part of anal fin. Pelvic fins separate, composed of one spine and five unbranched rays; first segmented ray short, rays becoming progressively longer, with fourth ray extending to below middle to end of anal base; fifth segmented ray short, about equal in length to first ray. Caudal fin short, oval in shape, shorter than head length. Gill opening broad, with branchiostegal membranes attaching to middle of isthmus below middle of eye. Body scales ctenoid, but cycloid on head, breast, belly and pectoral base. Cheek and opercles covered with large scales. Scales on top of head extend forward to above the end of the eyes and a single enlarged scale between eyes. Both jaws with a band of irregularly spaced small curved pointed teeth, and an innermost row of larger, straight, backward-pointed teeth; bands of teeth extend full lengths of jaws, but become narrower posteriorly. No vomerine or palatine teeth. No TABLE 1 Measurements of types of Calumza profunda and recently collected material of C. godeffroy: in millimetres Measurement C. profunda C. godeffroyz Holotype Paratype Paratype AMS I 19472-086 BPBM AMS I AMS I 21158 17477-026 _20156-001 Sex °} 2 g fo) } Standard length 18 16.5 17 14 19 Head length 7.0 6.0 6.7 4.9 6.8 Head depth at preopercular margin 3.8 3.0 3.3 3.0 2.6 Head width at preopercular margin 4.3 3.8 4.0 2.9 2.9 Upper jaw length 3.0 2.8 2.8 1.6 1.9 Eye length 1.8 1.6 1.6 1.5 1.7 Body depth at analorigin 4.0 3.4 3.5 3.6 4.5 Caudal length = 4.8 4.8 3.8 = Proc. Linn. Soc. N.S.W., 104 (1), (1979) 1980 H.K. LARSON AND D.F. HOESE 21 Fig. 2. Holotype of C. profunda. Drawing by H. K. Larson (caudal fin reconstructed). NS em vg @ REPP,. @eov)sesv® 9g Fig. 4. Top (right) and ventral (left) views of head of C. profunda showing arrangement of sensory papillae. Proc. Linn. Soc. N.S.W., 104 (1), (1979) 1980 22, SPECIES OF CALUMIA open lateral line head pores. Sensory papillae sparse, obscured by scales on cheek, but distinct below eye, on top of snout and on lower surface of head (Figs 3, 4). Colouration in alcohol: Head and body light brown. Centres of scales dark brown. Seven broad bands on body; first behind pectoral base; second under first dorsal fin; third and fourth under second dorsal fin; fifth and sixth on caudal peduncle; seventh at base of caudal. Head with faint brown bars radiating from eye ventrally and posteriorly. Snout, lips and underside of head dark brown. A dark brown blotch on each side of nape above upper end of operculum in front of pectoral base. Pectorals and pelvics with scattered melanophores. A dark brown spot at base of each pelvic fin. Caudal fin uniformly dusky, darker above and below base, where seventh body band extends onto fin. First dorsal fin with broad dark basal band, rest of fin clear. Second dorsal and anal fins dark brown basally, with body bands extending onto bases of fins; upper third of fins clear. Colouration of freshly collected holotype: Head and body chocolate brown. Iris golden yellow. Nostrils white. Head with three orange stripes radiating posteriorly from eye. Posterior third of operculum and branchiostegal membranes orange. Scattered orange mottling on sides and top of head. Body bands chocolate brown, interspaces light brown anteriorly, white posteriorly. Scale centres orange in dark body bands only, forming distinct rows of small orange spots, about half of pupil diameter in size. Base of first dorsal bluish with scattered small brown and orange spots; middle of fin with a broad bright yellow stripe; tip of fin bluish. Second dorsal and anal as for first dorsal, except basal two thirds of fins with large orange spots and yellow stripe above middle of fins. Caudal yellowish above and below, middle of fin clear, with tiny white speckles; two or three small white spots along upper and lower margins near base of fin. Pectoral and pelvic fins clear to whitish. Base of pelvic fin with a black spot. Etymology — from Latin, profunda — of the depths, alluding to its being found about relatively deep coral reefs. Material Examined — Holotype: BPBM 21158, an 18mm female from 38 m depth Alite Reef, near Malaita, Solomon Islands; J. Randall and B. Goldman, 25 July 1973. Paratypes: AMS I.20156-001, a 17mm female, taken with holotype. I.17477-026, a 16.5mm female from 55m depth, Bogacio Island, Espiritu Santo, New Hebrides; G. Allen, W. Stark and D. Popper, 28 June 1973. ACKNOWLEDGEMENTS We would like to thank J. E. Randall for supplying some of the type material and a colour photo of the holotype. We would also like to thank M. M. Smith (RUSI) and A. Wheeler (BMNH) for making types of described species available. J. R. Paxton kindly reviewed the manuscript. References ALLEN, G. R., 1979. — The fishes of Christmas Island, Indian Ocean. Aust. Nat. Parks Wildlife Spec. Publ. 2: 1-81. GUNTHER, A., 1877. — Andrew Garrett’s Fische der Sudsee, Part 6. J. Mus. Godeffroy 4 (13) : 169-216. Husss, C. L., and Lacier, K. F., 1958. — Fishes of the Great Lakes region. Bloomfield Hills, Michigan: Cranbrook Institute of Science. 213 pp. SCHULTZ, L. P., 1966. — Fishes of the Marshall and Marianas Islands. Volume 3. Bull. U.S. Natn. Mus. 202: 1-165. SMITH, J. L. B., 1958. — The fishes of the family Eleotridae in the western Indian Ocean. Ichth. Bull. Rhodes Univ. 1: 137-163. Proc. Linn. Soc. N.S.W., 104 (1), (1979) 1980 The Eelgrass Zostera capricorn in lawarra Lake, New South Wales M. MCD. HARRIS, R. J. KING and J. ELLIS Harris, M. McD., Kine, R. J., & Eis, J. The eelgrass Zostera capricornt in Illawarra Lake, New South Wales. Proc. Linn. Soc. N.S.W. 104 (1), (1979) 1980:23-33. Zostera capricorni Aschers. is the dominant angiosperm in Illawarra Lake where it occurs over a wide range of substrate types (14-98% sand, 0.5-12% organic carbon) and salinity (3 % — normal seawater). Distribution and abundance are related to light availability. The growth cycle shows a maximum in summer, with a winter minimum following shedding of the previous season’s growth. Flowering is extensive but even though seedlings have been observed, propagation appears to be almost entirely vegetative. Zostera, complete with substrate, has been successfully transplanted. M. McD. Harris, Wollongong Institute of Education, Wollongong, Australia 2500; R. J. King, School of Botany, University of New South Wales, Kensington, Australia 2033; and J. Ellis, Department of Chemistry, University of Wollongong, Wollongong, Australia 2500; manuscript received 22 November 1978, accepted in revised form 21 March 1979. INTRODUCTION Illawarra Lake is a coastal saline lagoon which straddles the boundary of the city of Wollongong (34°30'S, 150°50’E) in the north, and the Shellharbour municipality in the south, Fig. 1. The lake has evolved from a broad bay by the formation of a baymouth sand bar (Thom, 1974). Lakes formed in this way tend to be broad, shallow, exposed and turbulent expanses of water with an extensive sandy zone supporting benthic macrophytes. Illawarra Lake is no exception. It has a maximum length of approximately 9.5 km and a width of 5.5 km with an approximate area of 33 km’. The lake is shallow; an estimated 25% is less than 1.2 m deep and the maximum depth is only 3.7 m (Roy and Peat, 1973). The lake is oriented N-S parallel with the coast and is thus exposed to strong southerly and south westerly winds; lake water can be turbulent with wave heights approaching 0.5 m (Eliot et al., 1976). This turbulence coupled with the shallow nature of the lake causes considerable turbidity and is probably a significant factor in maintaining the concentration of dissolved oxygen (Kanamori, 1976). At present the lake enters the ocean near the southern end of the sand barrier where it is partially protected by Windang Island. This rocky prominence, which is usually land-tied by a tombola, dissipates wave energy and thus suppresses the rate of infilling of the entrance channel. The present channel from the lake to the ocean changes continually in position, width and depth depending on factors such as rainfall, wind and wave action. During 1972-1977 the entrance channel has been about 2.5 km long, winding and varying in depth up to 2.5 m. The main channel is seldom more than 100 m wide. It is restricted by a sand bar at the Windang bridge and occasionally the bar has completely choked the entrance. In late 1971 a blocking bar formed and this was subsequently cleared with earthmoving equipment. As a consequence of the restricted access to the sea very little tidal influence extends into the lake even at spring tides. Eliot et al. (1976) report a tidal rise of up to 0.1 m (cf. 2.0 m on the nearby ocean coast) on the western side of the lake at the Tallawarra power station. Ellis et al. (1977) estimate a tidal volume of 1% of the lake volume. Proc. Linn. Soc. N.S.W., 104 (1), (1979) 1980 24 ZOSTERA CAPRICORNI IN ILLAWARRA LAKE SL Ck, is} \ Mullet Ck. Brooks Ck. Kanahooka Pt. Koonawarra Bay Tallawarra Pt. Windang Is. Karoo Bay Fig. 1. Map of Illawarra Lake with geographical names THE FLORA OF ILLAWARRA LAKE Zostera capricorni Aschers. is the only seagrass recorded for Illawarra Lake and its distribution and abundance are the main subject of this paper. The range of morphology exhibited by Z. capricorni in Illawarra Lake is considerably greater than that given by Den Hartog (1970). Ruppza sp. is the only other angiosperm abundant in the benthic flora: it occupies approximately 30% of the eastern weed beds as a dense meadow in water 40-60 cm deep, Fig. 2. In shallow areas growth is reduced to sparse clumps. The change to Zostera with deeper water is abrupt. Isolated patches of Ruppia occur throughout the lake and in Hooka Creek, over a salinity range of 3-329. At all localities Ruppza grows inshore of Zostera, the reverse of the situation outlined by Higginson (1965) in the Tuggerah Lake system. Higginson suggested that Ruppia tended to favour clayey sediments, cf. Zostera on sandy sediments, but this conclusion was not borne out in this study. Wood (1959a) and Higginson (1965) both concluded that Ruppza is intolerant of strong currents and occurs mainly in sheltered bays. In this case high turbulence in Illawarra Lake may be the limiting factor for Ruppia which is then confined to the sheltered localities inshore of Zostera. Proc. Linn. Soc. N.S.W., 104 (1), (1979) 1980 M.M. HARRIS, R.J. KING AND J. ELLIS 25 Eastern Weed Beds a |Windang Cudgeree Entrance Channel Haywards Bay =: Zostera a Ruppia ® Lamprothamnio 4 Gracilaria \ Fig. 2. Distribution of benthic plants in Illawarra Lake Posidonza australis Hooker is not recorded in Illawarra Lake though the reasons for its absence remain obscure. Poszdonza is reported to be intolerant of strong currents and turbulence (Wood 1959a, b; Den Hartog, 1970) and also appears to be intolerant of high turbidity. High turbidity may prevent growth of Pos¢donza in the body of the lake but could not account for its absence in the entrance channel area. Turbulence and current velocities in the channel area do not approach the rip conditions observed in the entrance to Macquarie Lake where Wood (1959a) reports growth of Poszdonza. Halophila ovalis (R. Brown) Hooker was also surprisingly absent from Illawarra Lake. It occurs along the N.S.W. coast on a wide range of sediment types encompassing those found in Illawarra Lake, and over a wide range of conditions of salinity and turbidity. Despite its apparent wide ecological tolerance Halophila has not been observed in Illawarra Lake. Macroalgae were common in the Lake, particularly as epiphytes on Zostera and Ruppia. The most conspicuous were Polysiphonia sp., Enteromorpha intestinalis (L.) Link and Cladophora sp.; the latter species generally occurring in spring and early Proc. Linn. Soc. N.S.W., 104 (1), (1979) 1980 26 ZOSTERA CAPRICORNI IN ILLAWARRA LAKE summer. The Enteromorpha and Cladophora form extensive floating mats in protected bays and in the inshore parts of the eastern weed beds. The benthic alga Gracilaria verrucosa (Huds.) Pap. occurred throughout the year and the broad distribution is shown in Fig. 2. In the southern bays, Koona and Haywards Bays, it was the dominant species occupying the silty sediments in the central portion of the bays. At least in initial stages plants are attached to the sediment. Lamprothamnion was variable in occurrence but mainly associated with Ruppza inshore of Zostera in the eastern weed beds, Fig. 2. METHODS The data and observations presented in this paper were gathered over the period 1971-1976. Complete details can be obtained from Harris (1977). The data include: observations on the distribution and abundance of Zostera capricorni and other components of the benthic flora including epiphytes; details of the relationship between Zostera distribution, biomass and environmental data; long term observations on growth and flowering in Zostera. In the analysis of sediments and water quality the following techniques were used : Particle size analyses were conducted according to Folk (1968) . Organic carbon was estimated from loss on ignition at 550°C as described by Dean (1974). Total phosphorus was determined colorimetrically using the single solution method detailed in Major et al. (1972). pH was measured using a specific ion meter and pH combination electrode (Orzon Model 407A and electrode no. 91-02). Sediment pH is based on interstitial water extracted from the sediment by pressure. Eh was measured using an Eh combination electrode (Orion no. 96-78) standardized using Zo Bel solutions as described by Whitfield (1971). Sediment Eh was made on carefully mixed samples. Salinity was measured as chlorinity using a chloride electrode (Orion no. 96-17). Temperature was measured using a standard 50°C mercury thermometer. Turbidity measurements were initially made with a secchi disc but later using a turbidimeter (Hach Model 2100A). Wherever possible data from other sources, particularly Ellis and co-workers, were used. RESULTS AND DISCUSSION I Distribution of Zostera in Illawarra Lake in relation to environmental factors The major development of Zostera capricorni occurred in the eastern portion of the lake, and particularly off the Windang Peninsula and west of Bevans Island, Fig. 2. A narrow fringing zone seldom more than 20 m wide occurred around most of the bays in the western portion, except where Graczlarza was dominant. (A) Sediment Factors. The composition of sediments supporting Zostera is given in Table 1. Extreme ranges were: particle size, sand 52 to 98%; organic carbon 0.5 to 8.5%; total phosphorus 35 to 120 wg.g™'. Even greater extremes in values for particle size and organic carbon relate to the single site in Hooka Creek: 14% sand and 12% organic carbon. pH and Eh measurements were restricted to the eastern sandy portion of the Lake. Sediment pH ranged from 7.4 to 8.0 and Eh from +10 to —185 mV. This range of sediments, together with the lack of relationship between the distribution of sediment types in Illawarra Lake and the distribution of Zostera suggest that Zostera is not limited by sediment type. Proc. Linn. Soc. N.S.W., 104 (1), (1979) 1980 M.M. HARRIS, R.J. KING AND J. ELLIS 27 TABLE 1 Composition of sediments supporting Zostera in Illawarra Lake Mean values: range given in parentheses Location Number of samples Sand % Organic carbon % _Total phosphorus yg.17? Griffins Bay 12 90 (77-97) 2.3 (0.8-3.5) 82 (35-105) Eastern Weedbeds (off Windang Pens.) 8 96 (95-97) 1.5 (0.5-2.7) 61 (39-111) Bevans Island 18 92 (88-97) 1.8 (0.8-4.3) 72 (53-120) Southern Bays 5 82 (52-97) 3.3 (1.3-8.5) _ Western Weedbeds 5 84 (58-92) 353) (Zhe 522) - Hooka Creek 1 14 12.0 — Where the reduction of Zostera beds occurred in Koona Bay and Koong Burry Bay over the period 1972 to 1977 it appeared to be related to rapid accretion of sediments. In other places in the lake (e.g. the northern side of the entrance channel east of the Windang Bridge, on the delta at the lake end of the entrance channel, in the shallows to the north of Cudgeree Island and the delta of the Griffins Bay tank trap) burial and subsequent recovery has been a frequent occurrence. (B) Water Factors. Water quality in Illawarra Lake was highly variable. This is partially due to the fluctuating level of the lake: records of the N.S.W. Electricity Commission (1971) show an average variation in lake level of about 60cm in the period 1966-70. Salinity. Ellis et al. (1977) showed that mean salinity in the Lake is controlled primarily by rainfall, and varied from 12.8 to 31.3°%, during a two year monitoring period. There was essentially no salinity stratification, with vertical mixing by wave action completed within 2-4 weeks. There was no significant east-west salinity gradient even though the major creeks are on the western side of the lake. Zostera grew and even flowered over a wide range of salinity, from approximately 3%» in Hooka Creek to approximately 35 9%, in the entrance channel. This is outside the range experienced in the lake and it was concluded that salinity did not limit Zostera distribution. Temperature. Ellis and Kanamori (1977) record a mean water temperature for Illawarra Lake in the range 11.6 to 25.6°C. In the Tallawarra Power Station outlet channel, water temperatures at times exceeded 35°C yet Zostera persisted at this site. It is concluded that water temperature was not a limiting factor since the differences in temperature between various sites on the lake was always slight, usually less than 3°C, and new growth was observed throughout the year. Phosphorus. The nutrient status of the lake water, with regard to phosphates was generally beyond the level of enrichment needed to promote algal blooms (Anon., 1975; Wetzel, 1975). The observed total phosphorus range was 4 to 145 wg P.1” (Kanamori, 1976). Because the lake was turbulent and the phosphate level of the sediment high, localized deficiencies in water phosphorus concentrations would be quickly restored by water circulation and by disturbance of the sediment. It is thus unlikely that the distribution would be limited by phosphorus deficiency. Some very high concentrations of total phosphorus, up to 3,600 yg.1™' were observed in small creeks draining from non-sewered urban areas. Associated with this was a high E. cold count indicating that much of the nutrient inflow to Illawarra Lake is derived from domestic effluents and sewage. In areas adjacent to some streams, and in some bays, notably near Albion Creek in Koona Bay, in Kully Bay and Joes Bay Proc. Linn. Soc. N.S.W., 104 (1), (1979) 1980 28 ZOSTERA CAPRICORNI IN ILLAWARRA LAKE (Griffin Bay), Why Juck Bay, and in the Back Channel, Zostera grew sparsely or not at all. In these areas the green alga Enteromorpha grew in large floating masses shading the Zostera. In this way excessive phosphorus levels may have been indirectly responsible for restricting the distribution of Zostera. Nitrate levels in the Lake have a mean value of 2 wg.1-* (Kanamori, 1976) which is lower than values reported by Higginson (1971) for Tuggerah Lakes or Spencer (1959) for Macquarie Lake. pH and Eh. The observed ranges of pH and Eh for lake water were narrow; pH 8 to 8.4 and Eh +310 to +350 mV. State Pollution Control Commission figures (unpublished) give a pH range of 7.4 to 8.9. The narrow range and lack of systematic variation between different areas of the lake suggest that it is improbable that either of these factors would limit Zostera within the lake. Turbidity. Light availability has often been demonstrated as the factor setting the maximum depth to which seagrasses will grow (Backman and Barilotti, 1976). In Illawarra Lake Zostera occurred to a depth of 2 m in the entrance channel which was twice daily filled with low turbidity sea water. Throughout most of the eastern weed beds the outer limit was usually found at 1.5 to 1.8 m even though the sandy substrate continued beyond 2m in depth. In Griffins Bay and off the mouth of Mullett Creek, areas of fine sediment and high turbidity, the limit was inside the 1 m contour. Turbidity values and the depth limit of Zostera growth for near Bevans Island, the eastern weed beds, and one site in Griffins Bay are given in Table 2. Values are given for turbidity of water on the outer edge of the seagrass beds and also within the seagrass bed. Turbidity measure can often change rapidly: in the narrow fringing seagrass beds on the western side of the lake, where sediments are generally finer, turbidity could change from 2 to 40 NTU (nephelometric turbidity units) within 10 min. of a strong southerly change acting upon the lake. In the highly turbid areas of Koong Burry Bay, Haywards Bay and Koona Bay, Zostera is dominated by Gracilaria, in Griffins Bay Zostera and Gracilaria are co-dominant and in the eastern weed beds Gracilarza is only of minor importance. Water Movement. Zostera is reported to grow in regions with considerable water movement (Higginson, 1965). In Illawarra Lake it appeared to tolerate currents of several knots but to be less tolerant of strong wave action. Extensive colonies occurred on the margins of the entrance channel where they experienced strong tidal flow, and colonies in Mullet and Hooka creeks were not obviously disturbed by flood flows. The role of wave action is difficult to assess. On exposed peninsulas like Wollingurry Point, Tallawarra Point, Kanahooka Point and Wollamai Point, or in TABLE 2 Turbidity measure at various sites in Nephelometric Turbidity Units SITE Near Bevans Island Eastern Weed Beds Griffins Bay Depth of weed growth 1.8m 1.8m 1.6m 1.0m Turbidity measure atmargin in weed bed 10.11.75 2.0 0.5 1.5 4.5 1.75 1.0 4.5 9.5 8. 1.76 1.5 3.5 1.0 2.0 2.0 2.0 3.0 3.5 17. 1.76 1.5 15 1.5 1.5 2.0 2.0 2.5 1.5 29. 1.76 1.5 2.75 Wey 0) Neds. Boe 2.0 3.0 8. 2.76 3.0 1.25 1.5 2.5 2.0 1.5 2.757 9350. 14. 2.76 3.5 3.5 3.0 4.75 3.0 3.0 4.5 3.0 Mean Zee 2.0 1.6 2.9 Zell 2.0 3.2 3.9 Proc. Linn. Soc. N.S.W., 104 (1), (1979) 1980 M.M. HARRIS, R. J. KING AND J. ELLIS 29 open bays like Tuggerah, Yallah and Moureendah Bays, strong wave action periodically deposited several centimetres of sediment; then later removed it exposing the underlying rock. Zostera was unable to produce more than minor colonies in these areas. During 1975-76 the Zostera beds in the northern side of the training wall in Yallah Bay degenerated greatly. This occurred during a period of high wave action generated by persistent, strong easterly winds and considerable sediment disturbance was evident. Similar observations were made in the beds south of Wollingurry Creek. Of the environmental factors examined water depth and turbidity appear to be the most important factors limiting the lower distribution of Zostera in the lake. There is no evidence that sediment type plays any major role as has been suggested in the case of submerged aquatic angiosperms in the Tuggerah Lakes system (Higginson, 1965). The minimum water depth limit for Zostera in Mlawarra Lake varied widely. In Griffins Bay, along the eastern weed beds and west of Bevans Island Zostera was sparse in water less than 40 cm deep. These are areas of intensive feeding by ducks and swans. The ducks have been observed feeding on the shoots of Zostera and the swans on the rhizomes of both Zostera and Ruppia. Im areas such as the Back Channel, swans were seldom observed and here Zostera grew well in 15 - 20 cm of water. In September 1976, when lake levels were low Zostera beds in Koonawarra Bay were exposed. During this period several hundred black ducks (Anas superciliosa) congregated in this area and over the next 3 days cropped the exposed Zostera and Ruppia to within 1 cm of the sediment surface. II Zostera biomass in relation to environmental factors Analysis of the transect biomass data with environmental data showed no overall correlation between Zostera biomass and the factors particle size, sediment pH or Eh, ‘water pH or Eh, water temperature, and water or sediment total phosphorus. Despite the greater nutrient content of sediments in Griffins Bay, compared with those near Bevans Island, Zostera biomass at the latter location was significantly higher (1.5 - 3 times) than in Griffins Bay. There was however a distinct relationship between Zostera biomass and water depth, and hence light availability, Fig. 3a. Fig. 3b shows the growth of Zostera expressed as shoot length at the same sites. A similar relationship holds for total plant biomass and water depth. The differences between Bevans Island and Griffins Bay data are consistent with the notion that depth limits of Zostera at a given locality are a function of turbidity. The reduced biomass in water less than 40 cm is presumed to relate to waterfowl grazing pressure. III Vegetative growth of Zostera capricorn The seasonal growth cycle data for Zostera at selected localities during 1972-73 are shown in Fig. 4. The general pattern is similar with maximum leaf length occurring during summer and the minimum in winter. The onset of the new growth cycle occurred in August - September after shedding of the previous season’s growth. Wood (1959a) reported that leaf loss follows flowering and in autumn Zostera flats may seem completely bare of leaves. In this study full leaf development was sometimes maintained until early spring by which time new leaf growth had commenced. In 1973 rapid degeneration of Zostera beds occurred during February and March coincident with heavy rainfall. Similar declines in the standing crop followed heavy late summer and autumn rains in 1974 and 1976. In 1975 when rainfall was 40% less than average little decline occurred until the June - July floods. These changes were most marked in waters shallower than 0.6 m. This relationship between flood rains Proc. Linn. Soc. N.S.W., 104 (1), (1979) 1980 30 ZOSTERA CAPRICORNI IN ILLAWARRA LAKE 200 A Griffins Bay @® Bevans Island Zostera biomass 40 60 80 100 120 Water Depth (cm) Fig. 3a. Zostera biomass (mean values) in relation to water depth — Bevans Island and Griffins Bay Modal Zostera shoot length (cm) 40 60 80 100 120 Water Depth (cm) Fig. 3b. Zosterc shoot length (mean values) in relation to water depth — Bevans Island and Griffms Bay, January 1976 Proc. Linn. Soc. N.S.W., 104 (1), (1979) 1980 M. M. HARRIS, R.J. KING AND J. ELLIS 31 100 EASTERN WEED BEDS 80 60 40 20 100 NEAR BEVANS ISLAND Zostera shoot length (cm) 100 HAYWARDS BAY 80 60 j_ 40 20 Jul Aug Sep Oct Nov Dec Jan 1973 Fig. 4. Seasonal variation in shoot length of Zostera capricorni showing modal shoot length and range. and leaf shedding was most marked in the eastern weed beds while colonies in sheltered localities such as Haywards and Koonawarra Bays or along the southern shore were barely affected. When the Zostera beds have their normal water cover, wave action is suppressed at the outer margin; however, during flooding the increased water depth allows for vigorous wave action throughout the beds, leading to extensive _ shedding of leaves. Associated lower salinities and increased turbidity may predispose Zostera towards leaf shedding but in the absence of mechanical agents it did not appear to arise from these causes alone. IV Flowering and Seed Production Flowering of Zostera in Illawarra Lake is variable both temporally and spatially. Immature flowering shoots were first observed in September and flowering sometimes extended through to August of the following year, with seed production from October to August. Generally peak flowering occurred in summer. Table 3 summarizes data for the season 1975-76. In that season flowering was abruptly terminated with Proc. Linn. Soc. N.S.W., 104 (1), (1979) 1980 32 ZOSTERA CAPRICORNI IN ILLAWARRA LAKE TABLE 3 Percentage of fertile shoots at three locations in summer 1975-76 based on 500 cm? composite sample Number of shoots % fertile shoots Number of seeds examined Site October 1975 November December January 1976 February Near BevansIsland — nil — 992 4.1 57 650 10.6 89 579 13.9 112 406 2.2 7 Eastern Weed Beds 136 6.6 — 1295 7.5 34 679 12.2 61 516 17.2 83 250 1.2 2 Griffins Bay — nl — 257 22.2 186 397 12.1 172 405 13.6 101 — nil — shedding of flowering shoots after heavy January rains. The frequency of flowering shoots showed wide variation between years: in 1972-73 the frequency reached 34% near Cudgeree Island and in Haywards Bay. The majority of flowers did not produce seed. The observed maximum of flowers producing seed was 10.9% in 1976 compared to less than 2.6% in 1973. Germinating seeds were found in sieved sediment samples on only one occasion: near Bevans Island in July 1975. There was no evidence that Zostera was colonizing bare areas by seedlings. In dredged areas any subsequent recolonization occurred by rhizome invasion from adjacent areas. As found by Wood (1964), such recolonization is slow. Preliminary experiments with transplanting Zostera into the back channel near the Tallawarra Power Station and in Griffins Bay were successful when the plants were transplanted complete with relatively undisturbed sediments: washed rhizomes did not recolonize. These small transplants (size range 100 - 200 cm”) were made in June - October 1975 and 3 years later those near the Tallawarra Power Station had expanded to cover some 10 times the original area. This expansion has taken place by marginal growth of the clump into formerly uncolonized sediments. Growth in Griffins Bay has been less pronounced though clumps are still growing. CONCLUSION Within Illawarra Lake Zostera capricornt showed a marked ecological tolerance. Within the range found in the lake the distribution and abundance of Zostera did not appear to be controlled by substrate factors (particle size, total phosphorus, pH, Eh) or water quality factors (salinity, total phosphorus. pH, Eh). Light availability as influenced by water depth and turbidity appeared to control the lowest depth to which the plant grows. Grazing by swans and ducks may have been significant in setting the upper limit. Zostera showed a seasonal cycle with shedding of the previous season’s growth promoted by wave action. Flowering was extensive, though patchy and seed production was observed over a lengthy period, October to August of the following year. Although seedlings were observed in the field there was no evidence to suggest that seedlings play a major role in propagation. Transplant experiments, /using Zostera clumps in relatively undisturbed sediments, have been successful and clumps have been expanded by growth into previously uncolonized sediments. Proc. LINN. Soc. N.S.W., 104 (1), (1979) 1980 M. M. HARRIS, R.J. KING AND J. ELLIS 33 ACKNOWLEDGEMENTS We wish to acknowledge grants from the N.S.W. Electricity Commission, and the Department of Urban and Regional Development, under a National Estate Grant provided to the Wollongong City Council for the Illawarra Lake Environmental Assessment Project. References Anon., 1975. — Re-using sewage water. Ecos 3: 14-18. BACKMAN, T. W., and BariLotTI, D. C., 1976. — Irradiance reduction: effects on standing crops of the eelgrass Zostera marzna in a coastal lagoon. Mar. Bzol. 34: 33-40. DEAN, W. E., Jr., 1974. — Determination of carbonate and organic matter in calcareous sediments and sedimentary rocks by loss on ignition: comparison with other methods. J. Sedim. Petrol. 44: 242- 248. DEN HartToc, C., 1970. — The Sea-Grasses of the World. Amsterdam: North Holland Publ. Co. ELECTRICITY COMMISSION OF N.S.W., 1971. — Tallawarra area climatic and limnological data. (Unpublished) . Exiot, I. G., Younc, R. W., and Crark, D. J., 1976. — Part 4 — Lake hydrology. In Illawarra Lake. Wollongong: Wollongong City Council. Exuis, J., and KANAMORI, S., 1977. — Water pollution studies on Lake Illawarra. II. Thermal behaviour. Aust. J. Mar. Freshw. Res. 28: 479-484. ——, Kanamori, S., and Lairp, P. G., 1977. — Water pollution studies on Lake Illawarra. I. Salinity variation and estimation of residence time. Aust. ]. Mar. Freshw. Res. 28: 467-477. Fok, R. L., 1968. — The Petrology of Sedimentary Rocks. Austin, Texas: Hemphills. Harris, M. M., 1977. — Ecological studies on Illawarra Lake with special reference to Zostera capricorni Ascherson. Kensington: University of N.S.W., M.Sc. thesis, unpubl. Hiccinson, F. R., 1965. — The distribution of submerged aquatic angiosperms in the Tuggerah Lakes system. Proc. Linn. Soc. N.S.W. 90: 328-334. ——, 1971. — Ecological effects of pollution in Tuggerah Lakes. Proc. Ecol. Soc. Aust. 5: 143-152. KANAmorI, S., 1976. Water pollution studies on Lake Illawarra. Wollongong: University of Wollongong, Ph.D. thesis, unpubl. Major, G. A., Dat Pont, G., Kye, J., and NEWELL, B., 1972. — Laboratory Techniques in Marine Chemistry. CSIRO Div. Fish. and Oceanogr. Rep. 51. Roy, P. S., and Peat, C., 1973. — Bathymetry and bottom sediments of Lake Illawarra. Geol. Surv. N.S.W., Report No. GS 1973/295. SPENCER, R. S., 1959. — Some aspects of the ecology of Lake Macquarie N.S.W.., with regard to an alleged depletion of fish. II. Hydrology. Aust. J. Mar. Freshw. Res. 10: 279-296. Tuom, B. G., 1974. — Coastal erosion in eastern Australia. Search 5: 5. WETZEL R. G., 1975. — Limnology. Philadelphia: Saunders. WHITFIELD, M., 1971. — Ion selective electrodes for the analysis of natural waters. AMSA Handbook No. 2. Sydney: Aust. Mar. Sci. Assocn. Woop, E. J. F., 1959 (a). — Some east Australian sea-grass communities. Proc. Linn. Soc. N.S.W. 84: 218- 226. ——, 1959(b). — Some aspects of the ecology of Lake Macquarie, N.S.W., with regard to an alleged depletion of fish. VI. Plant communities and their significance. Aust. J]. Mar. Freshw. Res. 10: 322- 340. ——., 1964. — Studies in microbial ecology of the Australian region. Nova Hedwigza 8: 5-54, 453-568. Proc. Linn. Soc. N.S.W., 104 (1), (1979) 1980 A Key to Estuarine Polychaetes in New South Wales PAT HUTCHINGS and SEBASTIAN RAINER Hutcuincs, P., & RAINER, S. A key to estuarine polychaetes in New South Wales. Proc. Linn. Soc. N.S.W. 104 (1), (1979) 1980:35-48. A key to 184 species of estuarine polychaetes in New South Wales is given together with a reference to an adequate description of each named species. Pat Hutchings, Dept of Marine Invertebrates, Australian Museum, P.O. Box A285, Sydney South, Australia 2000, and Sebastian Rainer, CSIRO Division of Fisheries and Oceanography, Cronulla, Australia 2230; manuscript received 21 February 1979, accepted in revised form 18 July 1979. INTRODUCTION The estuarine polychaete fauna of New South Wales includes many undescribed species and new records. Sheltered bays will share many species in common with estuarine areas. At present we know of 184 species occurring in N.S.W. estuaries of which 125 have been described. Many other species remain to be described, some perhaps belonging to families not included in this key, for example Chrysopetalidae and Amphinomidae. Many of the descriptions were published early this century in journals with limited circulation and often not in English. No key exists to enable most of these species to be identified or differentiated from species already described and this key is intended to remedy this situation. The key is based on material collected during surveys of Careel Bay (Pittwater) and Gunnamatta Bay (Port Hacking) by the authors, from cores collected from Posidonia beds along the coast of New South Wales (PH and others) and other material from the Australian Museum collections. It is likely that many more species will be found in estuarine situations in New South Wales, but the key should provide a reasonable guide to at least the larger species. As it is possible that closely related species not in the key could be confused with keyed species, identifications made with the key should be checked against the literature. The number in brackets accompanying each named species indicates where an adequate description of that species may be found, using the numerical order of the references cited. Species keyed only to genus may represent undescribed species, new records that we have not been able to confirm or may refer to incomplete material that did not permit positive identification. An indication of other recorded species from Australia that may occur in N.S.W. estuaries is given by Day and Hutchings (1979). The key is based on Day (1967) with some modifications and additions using the taxonomy of Fauchald (1977). Reference should be made to Day (1967), for diagrams indicating the important features of individual families and for a glossary of the terms used. KEY TO ESTUARINE POLYCHAETES IN N.S.W. (modified after Day, 1967) 1. —Most of the following characters: prostomium with sensory appendages; pharynx armed with jaws or teeth; parapodia well developed, compound setae OLLENIPTESENE Wiese ewe Ackles ee sheaers leh ey Mine mnewsieanac) alls Polychaeta Errantia 2 —Most of the following characters: prostomium usually Proc. LINN. Soc. N.S.W., 104 (1), (1979) 1980 36 ESTUARINE POLYCHAETES lacking sensory appendages, often fused to peristome, which may bear grooved palps, buccal cirri, stout setae or branchial crown; compound setae rarely PRESENT Ae OI aN E NED. MGs ay ara ame ae cM Polychaeta Sedentaria 68 Polychaeta Errantia 2h —Elytra present on many segments ............... .e eee ee eee eee eee 3 == Fiytravalbsem tie iitascasieel syealtoviot onan cisstcuianeneh cies ee lene, cri amystcch cor ente tutes) cite trae veti eS RAL aR a ge US 12 3. —Compound setae absent; elytra and dorsal cirri alternate fairly regularly...................... F. Polynoidae 4 —Compound setae present; elytra on alternate segments anteriorly, from about setiger 25 onwards Onl allisegments ie 253k cece ain a ea OU Gr Stn yi F. Sigalionidae 11 4. —Lateral antennae terminal, arising at level of median antenna, 15 pairsofelytra .................... Parahalosydna chrysostichtus (13) —Lateral antennae arising below level of median antenna’) 5-16) pairs of elytraiy hy ala’ ie ins Weiter ils rales peteere trae netnrn et alvel etesy Mi lurealbal Mea 5 5. —Lateral antennae subterminal;. ventral lamellae PLESEM lich saeco ossis tar iyrea sts ce tue Sle: obs aa mucus scuanay eieal Shoat tes Paralepidonotus ampulliferus (13) —Lateral antennae ventral; ventral lamellae absent... .....................000% 6 6. —Neurosetae with blades tapering to fine tips, UMI GEN tates sas te won itn aon aaron ane ch alade Antinoe sp. —Neurosetae with blades ending in stout tips, uni- or bidentate {occ woe nana nant me cee MeN dhe fal ihe ea DI anda oh gts SMR Cony Ne anvL Santa 7 Pp —One or more of the basal serrations on both notosetae and neurosetae enlarged to form spinous pockets; prostomium without frontal peaks .............. Scalisetosus sp. — Basal serrations on setae not enlarged, prostomium with frontal peaks.....................00008, Harmothoe 8 8. —Elytra ornamented with multifid tubercles ........ Harmothoe sp. —Elytra ornamented with simple tubercles.......... 2.2... eee eee eee 9 9. —Elytral tubercles with flat-topped apices .......... Harmothoe sp. —Elytralltuberclesiconical: 2/95 foe eee n poenalsha sh Yess aieesiciel euenaamue nl areasieusiinne ests 10 10. —Elytral tubercles numerous.................... Harmothoe sp. —Elytral tubercles short, conical, few, sometimes absent, elytra, margins with elongate papillae...... H. praeclara (13) 11. — Median antenna with basal lappetson ceratophore.. Sthenelazs sp. —Median antenna absent or papilliform and lacking CET atOphore ss site doen ces sist cetadla sce patties mene sts Sigalion ovigerum (15) 12. — Dorsal and ventral cirri foliaceous............... F. Phyllodocidae 13 13. —Five antennae, no occipital papilla; 4 pairs of tentaculan CirTiy eis vette lee LM EMenUR Esc ciaks Eumida sanguinea (13) —Four antennae and often an occipital papilla; 3-4 pairsiofitentacular cirri 55 aie aus gem uatayceie ce a ceee eee see ee mae eel) det es ee eh 14 14. —Setae present on third, or second and _ third, tentacullansepments() 6.01) fide ea fay ee tania at, cul i pear Sita ae rea ue Le 15 —Setae absent from all tentacular segments............... 0.0 cee eect eee 16 15. —Setae first present by second tentacular segment; rustyredimicolourya wens ne sees eee eee Genetyllis castanea ( 3) —Setae first present by third tentacular segment; colour otherwise, iiiyki van ederim gate Ne, Paranaitis (4 spp) 16. | —Pharynx with regular rows of papillae at sides of base, first 3 segments dusky, later segments with 3 dark spots; dorsal cirri large and cordate anteriorly ..... Anattides longipes ( 3) —Pharynx with irregularly arranged papillae; body Proc. Linn. Soc. N.S.W., 104 (1), (1979) 1980 17. 20. 21. DR 23. 24. 25. 26. 27. 28. 31. 32. 33. P. HUTCHINGS AND S.RAINER pale to dark brown with dark intersegmental bands; dorsal cirri almost semicircular................. Phyllodoce novaehollandiae —Prostomium with ventrolateral palps............... 20... 0c eee eee ee 18 — Prostomium:without palps! (0 0, sc8se Scie t gelesen sisse heels aes gleencre 51 —Palps biarticulate, with stout basal joint and smaller Gistalhj orn teens tear neways Me waay cys tape ce een alien geen = Neste neciiay aay hous Sacileranas ran clave! ls Sa] sine ahaere 19 SAL PSISIMMP Lewy wapeierar velar enna eNO cence Nach p eco nece e eieeiin eye Sisal alocauecss Tetenere (eM e e e 35 —Compound setae absent; tentacular cirri two or fewer F. Pilargidae 20 —Compound setae present; tentacular cirri four pairs OTETIVO TS ae ees Apt Nance sce seh smemah ear aflis Uanharie) am Petco a teal lee 51 Sul eoy vedios Uo RTO RBI Saltch Mciracte~ amen etae eng be 21 —Prostomium with three antennae; pharynx muscular Sigambra parva — Prostomium with two antennae; pharynx epithelial . Plargzs sp. —Jaws, if present, usually styliform, denticles absent; tentacular cirri often jointed................... F. Hesionidae 22 —Two toothed jaws present and often horny denticles ; tentacular cirrismooth....................... F. Nereidae 25 FO Mapalns tenctacUlan GME eigenen a cine ccaile wie esi os. cllaiese « shaceee Gl sere pete al eee eaeneleucee 23 SSIHIphtipalrsitentaculary Cai. ctr...) are oreut ty sree ksi aacla ue one UA hie © eiaeey See eae 24 —Two anterolateral antennae and one median antenna, notosetae 1/2 capillaries............... Ophiodromus cf. agilzs —Two anterolateral antennae only; notosetae present OlgabSem twa clete euens wis aae a nual et ousl Tats Gy, Nerimyra sp. —Notopodium reduced, with few capillary setae ..... Gyptzs sp. —Notopodium not reduced, with numerous capillaries. cf. Gyptis sp. —Anterior apodous segment absent behind peristomium ; antennae absent; paragnaths absent.. Micronerezs sp. —Anterior apodous segment present behind peristomium; two antennae present; paragnaths PREsentvOr abseEMtbys «sis sien ee eames anid inamspraieuarsemt tee cae liane de oon at cbrsieuelepaitelay aero tenuis 26 —Chitinous paragnaths entirely absent; a transverse series of glandular ridges at base of anterior PATA POA welen wg.) sie, A els a ea ee ee IE NS, ata a ree Australonerets ehlersi —Chitinous paragnaths present; ventral glandular MIO PEStADSEM CH Loe caine actin ee edeys eesorsh ye) Stee hac ncn eee com oben Sra Uma Bnah Ah teria ass 27 —Paragnaths all separate andconical ................ 0.0... c ee eee eee eee 28 — Paragnaths include pectinate or transverse bars..................0--- eee eeee 34 —Chitinous paragnaths present on both basal and ma Xd ary PUM GS 2, 2 2c sak aulsomaitayen wenpe ouianedamomanerte Sener dee Bien eoaae IevecleRtentaletay ssid sala A 29 —Chitinous paragnaths present on maxillary ring only . —Falcigers present in posterior notopodia, few setae; paragnaths few, absent on I, V and VI, II-1, III +IV- ELV ANY) OereAY) 0 0 Et apenas te eiS, elie yee otter Sener ansae —Falcigers absent in posterior notopodia........... —Notopodial lobe very large on both sides of dorsal cirrus in median and posterior segments .......... —Notopodial lobe not particularly enlarged — Areas I and V of pharynx lacking paragnaths ....... — Areas I and V of pharynx with paragnaths —Paragnaths of area I-2, and area VI-3 cones in in- ventedttrian glenn. eae atk era caer: oe — Paragnaths of area I-4 in triangle, and areas V + VIII — continuous band of cones 4-6 deep............ —Prostomium deeply cleft between antennae; dorsal cirri long; no simple neuropodial falcigers ........ Ceratonerets 33 Nerets postdoniae Neanthes 30 Neanthes oxypoda Fae oie aoe eset Nena ORE 31 N. vaala N. cricognatha C. mirabilis 37 (13) ( 3) ( 3) (13) (13) ( 9) (13) (13) (13) Proc. Linn. Soc. N.S.W., 104 (1), (1979) 1980 38 ESTUARINE POLYCHAETES —Prostomium not cleft; dorsal cirri short; one large simple falciger in posterior neuropodia........... C. erythraeensts (18) 34. —Areas IV, VII + VIII of pharynx with cones and pectinate paragnaths, posterior notopodia with 2-3 homogomph falcigers........................ Platynerets dumerili antipoda (13) —Area VI of pharynx with continuous transverse series of cones extending across V and VI.............. Perinereis cf. brevicirris ( 9) 35. —Barrel-shaped proventriculus posterior to pharynx, pharyngeal armature variable.................. F. Syllidae 36 — Proventriculus absent, four or more pairs of jaws.............-...-0 ee eee eee 56 36. —Ventral cirri absent; dorsal cirri not annulated..... Autolytus sp. —Ventral cirri distinct, dorsal cirri annulated or SITLO OER PRG eS AHN caste il hoo Pala cae PNG ne BEAM ea Cte eB eae eeca bare COUR 37 37. | —Palps separate; dorsal cirrijointed ........... 0.0... eee ee eee 38 —Palps fused basally or for at least half their length; dorsalicirrismoothy cence epee uaa aie abana sia ue aarnsy eater ittama hey sae ee nev a eee eat 43 38. —Setae few, simple, enlarged, with 2 teeth, terminal One \bifid ei oa ee lay ce Meal eas ny eel ick hed ins aia Haplosyllis spongicola ( 3) —Setae mainly or entirely compound............... 0... ee eee eee 39 39. — Mainly compound setae anteriorly, then include a few large simple setae with Y-shaped prongs .......... Syllis graczles ( 3) = Onlyicompound'setaejpresenty os.) caiieie eise sl let et aici ieee a ern 40 40. — Blades of some superior setae much longer than the rest; dorsal cirri with 10-18 joints............... Langerhansza cornuta ( 3) —Blades of setae decrease evenly in length, dorsal cirri Otherwise! seis Ciena, Wate Voce rah ecole Steet iea yak Typosylles 41 41. —Setae unidentate or minutely bidentate, dorsal cirri stout with 8-12 joints ........................ T. armillaris ( 3) —Setae strongly bidentate; dorsal cirri otherwise..................- eee eee 42 42. —Dorsal cirri short, with 7-12 joints............... T. cf. hyalina ( 3) —Dorsal cirri with more than 20 joints............. T. variegata (13) 43. —Palps fused basally; dorsal cirri usually smooth. .................-200 eee ees 44 —Palps fused for at least half their length; dorsal cirri EJretolol a ohh eM eee ite elon amas dc TaRSR TEENS rata COs eA eM MENG Mts at Rn bien aiaate Gg 45 44. —Pharynx unarmed; ventral cirri longer than setigerous lobes; acicula of anterior parapodia enlarged, knobbed.......................... Streptosyllis sp. —Pharynx with a semicircle of recurved teeth; ventral cirri not longer than setigerous lobes; acicula not Knob bed eet Si a He ea a ga ariieea Odontosyllis sp. 45. —Dorsal cirri papilliform; 1 pair of rudimentary tentacular Ginnie is See a eS mittee hat) Exogone 46 —Dorsal cirri flask-shaped; 1 pair of tentacular cirri .. Sphaerosyllzs 48 46. —Dorsal cirrus present on setiger 2, single superior compound seta with dagger-like blade ........... Exogone sp. —Dorsal cirrus absent on setiger 2; superior compound setaeidifferent fromrest):. x y.ai Ppa Misses. eon taeevn ey mice ssa rsteis| ou oe ietl Starman 47 47. —Superior compound setae with swollen shaft-head and broad triangular blade....................... E. heterosetosa ( 3) —Three to five superior compound setae with dagger- like blades, c(i sic apis eile evehectia tera etch snesctisia art E. cf. gemmifera (13) 48. —Body surface and parapodia covered with minute Papillaey rs ire iiss Mirae ied eee eM Miinegs eis 2 fa Gra, ey i ed a at Cou NA canoe ae aa 49 — Body surface and parapodia without papillae ....................... 000s eee 50 49. —Dorsal cirrus on setiger2....................-.. S. cf. semzverrucosa (18) —Dorsal cirrus absent from setiger2 .............. Sphaerosyllis sp. Proc. Linn. Soc. N.S.W., 104 (1), (1979) 1980 50. 51. Be 53. 54. 55. Bite 59. 60. 61. 62. 63. 64. P. HUTCHINGS AND S.RAINER —Dorsal cirrus on setiger2....... —Dorsal cirrus absent from setiger 2 —Body papillose, head indistinct; pharynx unarmed . . —Body smooth, head distinct; pharynx with two or {MOS OLUTION o bg oe odd oto sic obiclod olbipiaa 6b o dla Udo pololmeolo edo dia og o/6\c 52 — Peristomium with parapodia and setae — Peristomium without parapodia or setae —Prostomium pentagonal, body parapodia with lamellae....... square in section; —Prostomium a pointed cone, body circular in section; parapodia-without lamellae’ ssn 2 sas ci lais wees sie cianejoieie ene aus ee Geena ene weer 56 —Prostomium produced anteriorly ; —Prostomium not produced anteriorly; setae short —Branchiae recurved, from setiger long flowing setae. 4; pharynx with 22 longitudinal rows of papillae and single median Papilla yar e eee wien oes —Branchiae recurved, from setiger 5; pharynx with 20 longitudinal rows of papillae and no single median Papillary Wee ssa cs cviely ce sake soatets —Pharynx with four horny jaws; and body not divided into regions parapodia all alike —Pharynx with a pair of toothed jaws and a circle of denticles; body divided into different regions ...... —Branchiae non-retractile, simple; pharyngeal papillae of two types, one with distal flange........ —Branchiae retractile, branched; pharyngeal papillae of two types, without distal flange — Body divided into three regions, parapodia biramous after setiger 34.............. — Body divided into three regions, parapodia biramous after setiger30.............. —Dorsal cirri and antennae present —Dorsal cirri absent or rudimentary; antennae usually ADSEN tae y votes atee a eos —Maxillae of four or five paired plates, plates III and IV fused on right side; antennae variable; branchiae usuallyspresemt,: A. cls ciinct Mua pee ics a) afro aces decaf le el cegielsaemed na aan iv oh lal duasuee cu paancna sir 61 —Mazxillae of numerous small elements in two or four longitudinal series, two antennae palps; branchiae absent ....... and two cylindrical — One to five antennae, without ringed ceratophores . . —Seven antennae, posterior five ceratophores ............... with long, ringed — One antenna; branchiae and tentacular cirri absent —Five antennae; branchiae present —Tentacular cirri absent; anterior margin of prostomium bilobed; comb setae absent, compound setae spinigerous, acicular setae bidentate ........ —Tentacular cirri present....... —Anterior margin of prostomium deeply notched, antennae deeply jointed ; branchiae begin on setigers 3-8; comb setae present, compound setae falcigerous, acicular setae tridentate....... Sphaerosyllis sp. S. sublaevis F. Sphaerodoridae- Sphaerodoridium sp. N. australiensis N. inornata F. Glyceridae 57 F. Goniadidae 58 Glycera tridactyla* G. americana Glycinde armigera Glycinde sp. F. Dorvilleidae 67 F. Eunicidae 62 F. Onuphidae 65 Nematonerets cf. unicornis Sey tesa Ato eae «AIO at mR eRe a 63 Marphysa sanguinea Eunice 64 E. australis *Glycera convoluta Keferstein is synonymous with G. tridactyla Schmarda 39 ( 3) (16) (16) (16) ( 3) (13) ( 9) ( 3) (13) (18) Proc. Linn. Soc. N.S.W., 104 (1), (1979) 1980 40 ESTUARINE POLYCHAETES —Anterior margin of prostomium shallowly notched, antennae nearly smooth; branchiae from setiger 3; comb setae present, compound setae falcigerous, acicular setae tridentate...................... E. wttata ( 3) 65. —Branchial filaments arranged spirally, from setiger 5, pseudocompound hooks unidentate or with secondary toothivery weaken Vmnien gules ee vests si Seaways. letlea ie Diopatra cf. neapolitana ( 3) —Branchial filaments arranged spirally, from setiger 5; pseudocompound hooks bidentate .............. Diopatra sp. 66. —Prostomium conical, body elongate; hooded hooks jointed in first few parapodia, later hooks simple; body reddish or orange....................--. Lumbrineris latreill (13) —Prostomium conical, body elongate; hooded hooks jointed in first few parapodia, later hooks simple; body preemie pai Meena) ah esi entire ee ccmeaee teensy rn ceacnls Lumbrineris sp. 67. —Parapodia uniramous with ovoid dorsal cirri, no cirrophores or notoacicula.................... Protodoruvillea sp. — Parapodia sub-biramous with dorsal cirri mounted on ceratophores containing notoacicula............. Dorvillea australienszs (1) Polychaeta Sedentaria 68. —Head not greatly modified; prostomium well developed; peristomium sometimes with pair of palps.....................+--- 69 —Head modified by development of frilly membrane, buccal tentacles or a branchial crown; prostomium Oftensreduced yer Wye ce em ily a ete vs glos fate coves palaaacniaetse Sh Mr edieteeh Mays Stas 155 69. — Buccal segment with palps or tentacles ............ 0... eee eee ee 70 —Buccal segment without food gathering appendages ......................... 124 70. —Buccal segment with pair of adhesive palps (often broken off) or several grooved tentacles ............ 0.0... c cee eee 71 —Buccal segments with tentacles retractile into the TOUCH Sig lets er seer NG ee tector as F. Ampharetidae 160 71. —Hooded hooks present in posterior setigers; well developed parapodiiay yee) Mos ie Cane Teun ses eaves elo) ales hropaialegelienteaianauceneae anne 72 —Hooded hooks entirely absent; parapodia often poorlydeveloped eins Vii teemitec lets ay eueo tee nen eco ay nia thaws cilane sue Votieunite musi en Roane lit 108 72. —Head not flattened, branchiae often present; palps grooved ; posterior notosetae hooded hooks........ F. Spionidae 73 —Head flattened and spade-shaped; palps papillose, notosetae hooded hooks from setiger 9............ F. Magelonidae 106 73. —Setiger 5 with strongly modified setae .............. 0.02. cee eee ee eee 74 —Setiger 5 without modified setae ............ 0.0... eee ee 85 74. —Branchiae first present posterior tosetiger5 ............ 0... e eee eee eee eee 75 —Branchiae first present anterior to setiger5........... 00-0. eee eee eee 83 75. —Setiger 5 slightly to moderately modified parapodia.. | Pseudopolydora 76 —Setiger 5 greatly modified, with reduced parapodia.............-...--++-++--- 77 76. —Prostomium entire; neuropodial hooded hooks from Sebi pen Ora sary Hi ania ess) aye chen rae amen veren te Olen CO si P. paucibranchiata ( 2) —Prostomium incised; bidentate neuropodial hooded hooks fromysetiger 8 7.cy.0sey mee ee eee tr uieas P. kempi ( 2) 77. —Setiger 5 with spines of one type with or without companion capillarysetae .................... Polydora 78 —Setiger 5 with spines of two types................ Carazziella 82 78. —Setiger 5 with brush-tipped companion setae; specialized posterior notosetae absent............ P. penicillata (13) —Setiger 5 without brush-tipped companion setae; specialized posterior notosetae present or absent ..........-----22+-e seer ee eee 79 Proc. LINN. Soc. N.S.W., 104 (1), (1979) 1980 80. 81. 82. 84. 85. 86. 87. 88. 90. 91. P. HUTCHINGS AND S. RAINER 4] — Hooded hooks with constriction on shaft.......... P. haswelli ( 2) — Hooded hooks without constriction on shaft ............ 0... e ee eee eee ee 80 —Posterior notopodial spines form dense packets of needles; gizzard absent; major spines of setiger 5 with weak subterminal swelling; eyes absent........... P. flava ( 2) — Posterior notopodial spines absent ................ 0... e eee ee eee 81 —Gizzard present internally in setigers 18-19, seen externally as a swelling; major spines of setiger 5 with subterminal boss; eyes present ................. P. socialis ( 2) —Gizzard absent; major spines of setiger 5 falcate, simple seyesjabsentannyeiys acne ara nsie aera Polydora sp. —Hooded hooks from setiger 7; superior dorsal fascicle of notosetae with fimbriated setae............... C. hirsutiseta ( 2) —Hooded hooks from setiger 8; superior dorsal fascicle of notosetae with simple setae.................. C. victoriensis ( 2) —Major spines of setiger 5 of two types, first with expanded ends bearing bristles, second simple, fal Cate pret crane ne seen td seine. Litas UMM nad fu Boccardza chilensis ( 2) — Major spines of setiger 5 of one type, simple, falcate, with smaller companion setae.................. Boccardtella 84 —Branchiae from setiger 2 onwards except for setigers 4 ATID erences cyte sarae yume mo ma ANE eee ee ee bore B. bihamata ( 2) —Branchiae from setiger 2 onwards, on setiger 5 may be RU GIMEM GARY) Cy spaleesitee ests srodunanaia ea al sea satay Mita B. limnicola ( 2) —Prostomium distally pointed............ 0.0... cee eee ee eee 86 —Prostomium not distally pointed, with lateral or frontal horns, anterior margin broadly rounded or aS Ui Bias ve echt vie a RE ATEGe Rae OU EntEE Sn Ook PEL RMD eh RR erate ES TEE UE rey 90 —Branchiae beginning on setiger 1, continuing almost LOMMOStETION.EMGs silo o hla faracs eatiesele) oo) seinda lara sis os Australospio trifida ( 2) —Branchiae beginning on setiger 2, continuing over Vatiablemumiben of setigers)< wists ncn scree craciee acl sche eon or a ev etien clare lel arate eaten 87 —Branchiae completely free from dorsal lamellae, albsentjposterionlys s)sarinniee aie ene ocak Aonzdes oxycephala ( 2) —Branchiae fused to dorsal lamellae and continuing to eEndiofibodye sii sus ley Sees toca ais silane tee sustal Scolelepis 88 —Notosetae present on setiger 1, neuropodial hooks quadnidentate Yee isin) swaenae aula Gets ld heats S. precirriseta ( 2) —Notosetae absent on setiger 1, neuropodial hooks Otherwise; iscsi) i cake ole hence tae Rew aa od teen tear ne eau lelic sn Dut SAM es NM air SINS 89 —Hooded hooks multidentate, from setiger 14-15, in Meuropodia only. oi. es ee oe aol ein elel es S. towra ( 2) —Hooded hooks bidentate, from setiger 24, probably onlyin neuropodia..:...................04.- S. vexzllatus (as Pseudomalacoceros vexillatus) (13) —Prostomium with lateral or frontal horns...............-0-- 0s esse cette tees 91 —Prostomium without lateral or frontal horns .................... 0000s eee eee 94 —Branchiae from setiger]...................... Malacoceros 92 —Branchiae from setiger 2...................... Rhynchosfio —Bidentate ventral hooded hooks from setiger 22... .. M. divisus (13) —Tridentate ventral hooded hooks from setiger 11 or ACT Pee Ley ays ese ee ect eee ie Ma MeN cTectesie MRCP ENE es ntd uate abiuers -aitaplur ae acta ac arehial a) # Sonata ia 93 —Body with dark brown pigment; tridentate ventral hooded hooks from setiger 25 .................. M. tripartitus ( 2) —Body colourless; tridentate ventral hooded hooks from setiger 11........ Malacoceros sp. Proc. Linn. Soc. N.S.W., 104 (1), (1979) 1980 42 Wee why 96. 97. 98. 99. 100. 101. 102. 103. 104. 105. 106. 107. 108. 109. 110. 111. 112. —Neuropodial ESTUARINE POLYCHAETES —Branchiae limited to middle and posterior setigers except for one pair on setiger 2inmales .......... —Branchiae from setiger 1 or 2 —Branchiae concentrated in setigers 1-22 —Branchiae present over most of body —Branchiae from setiger 1 —Branchiae from setiger2...................... —Branchiae otherwise —Branchiae all pinnate —Branchiae both pinnate and cirriform —Three pairs of pinnate branchiae; dorsal ridge across SECIBerul reese —Kighteen to 22 pairs of cirriform branchiae; no dorsal ridge on setiger 1 .. =Branchiae.all cinnformen eee eee Prionospio Paraprionospio sp. Orthoprionospio cirriformia P. ctrrifera Pie aoe eee er ry AUB Re Cat cet ea Pe Reo aI PL MOE a ey i 99 — Three pairs of pinnate branchiae; low dorsal crest on Seliger Mase ee —Four pairs of pinnate branchiae, dorsal crests absent . —First and third pairs of branchiae pinnate (pinnules sparse) , second and fourth pairs cirriform......... —Branchiae otherwise —First three pairs of branchiae cirriform, fourth pair pinnatey ae ade —First and fourth pairs of branchiae pinnate, second and third pairs cirriform — Dorsal transverse crest on setiger 7 only........... — Dorsal transverse crests from setiger 7 to about 30... —Branchiae from setiger]...................... —Branchiae from setiger2..................-.-.. —Neuropodial hooded hooks from setiger 10-11, bidentate; body colourless .................... hooded hooks from setiger 9-11, tridentate; anterior body brown pigmented ....... —Hooded hooks from setiger 9, tridentate (MF:2), accompanied by single short hooded hook per fascicle —Hooded hook from multidentate setiger 9, bidentate or —Hooded hooks multidentate, all hooks within a fascicleisimilarinisizey sa ee ie —Hooded hooks bidentate (MF:1), all hooks within a fascicleisimilarminisize..) ae A eee —Long filamentous branchiae at least on anterior segments; parapodia reduced toridges........... — Two large grooved tentacular filaments —Several grooved tentacular filaments — Capillary setae only present —Acicular hooks and capillaries present just above notosetae dorsalline ....... —Branchiae not long and filamentous; parapodia not imithe form Of Tid ges i. yee del uname apace anaes ec cena moe teen at sae ote Nee —Branchial filaments in middle of body arise laterally —Branchial filaments in middle of body arise from mid —Acicular setae of posterior noto- and neuropodia Proc. Linn. Soc. N.S.W., 104 (1), (1979) 1980 P. aucklandica P. multipinnulata P. paucipinnulata P. fallax P. multicristata Spio Laonice sp. S. filicornas S. pacifica Magelona dakini Magelona sp. Magelona sp. F. Cirratulidae T. marioni T. dorsobranchiata 100° 101 102 103 105 107 109 ( 3) ( 2) ( 2) ( 2) ( 6) (13) ( 3) ( 2) (13) ( 3) ( 3) 113. 114. 115. 116. 117. 118. 119. 120. 121. 122. 123. 124. 125. P. HUTCHINGS AND S. RAINER continuous to form two lateral arcs, on either side of body; acicular hooks present in only last 40 setigers, increasing rapidly to 5-6 per fascicle plus 5-6 Capillaniess apie cis cree enn Chaetozone sp. —Posterior noto- and neurosetae remain in separate uma Tes pee te snes tcuisnararat ch ecchlansbesal ass aberemelonss Caullerzella 113 —Neuropodial hooks from setiger3............... Caulleriella bioculatus —Neuropodial hooks from setiger 3 or later... 1.1.2.0... 0.0 cece eee eee eee ees 114 —Neuropodial hooks from setiger 4, bidentate....... Caulleriella tricapillata —Neuropodial hooks from setiger 31 or later, bidentate........................ 115 —Neuropodial hooks from setiger 31, minutely multidentate, accompanied by capillaries; single acicular seta present in posterior segments; elliptical EV EIS POE ae eet sscysy nye oseiioy seisy ahs naerter aieereyssas fevied cietce sas Caullerzella sp. —Neuropodial hooks from setiger 34, multidentate by setiger 71, accompanied by capillaries; simple acicular hooks posteriorly, sigmoid anteriorly; pair of darkseyeispotss eye iiacysn a) als ie sunce eee o syetnoss ses its Caullerzella sp. —Branchial filaments arise om same segment as tentacullanicirnie ssnyacies 4) cisele es ecm aiameeale als Cirratulus 117 —Branchial filaments arise on all segments anterior to tentacularteimniy aii ut ep pepe deme chad a Cirriformia 119 —Tentacular filaments arise above setigers4-6....... Cirratulus chrysoderma —Tentacular filaments arise otherwise. ......... 20... 0. eee eee eee 118 —Tentacular filaments arise above setigers 6-10; acicular setae absent, capillaries throughout; anterior heavily pigmented.................... Cirratulus nuchalis —Tentacular filaments arise above setiger 3; sigmoid hooks and capillaries present .................. Cirratulus sp. —Tentacular filaments arise above setigers 3-4....... Cirriformia capensis —Tentacular filaments arise above setigers 4-6 0r5-7............... 0000000005: 120 —Tentacular filaments arise above setigers 4-6; capillaries throughout, sigmoid hooks by setiger12.. Crrréformza filigera —Tentacular filaments above setiger 4-6 or 5-7; capillaries throughout, sigmoid hooks from setiger 50 Cirriformia tentaculata —Noto- and neuropodia of anterior parapodia well developed, setiger 1 with elongate setae directed POT WAT ASI tsetse ccs ueik sea cote e Cena psiesn or gual cioctad F. Trochochaetidae- Poecilochaetus serpens —Anterior setigers uniramous, neuropodia lacking; posterior setigers biramous with neurosetae as minute (UHDYSNT OV Sey a ee URN cNIneA amnion GiciAtan Dl eee Sonia nor erase Ole F. Chaetopteridae 122 — Middle region with bilobed notopodia; no tentacular Pel 9 Welt AU PS ac EARN citcett Spee NB LS oO Spiochaetopterus sp. —Middle region with notopodia never bilobed; no temtac ular Cir s) eee 255) .caleh seem eae amy ae istientcltaun sn ate besa calibte geal louis fantap lanes aie aiy tat Alle tate 123 —Body large; palps short; some notopodia of middle region fused to form paddles; parchment tube ..... Chaetopterus variopedatus — Body small; palps large; notopodia of middle regions never fused; fragile sandy tube; often living in dense COLONIES sie Supe Reescis elas ae aici peet ee non eueee ale Mesochaetopterus minutus — entatecrestedshooks absent sisi e ee enciey lei neti ee) ol We clievients) aii ilcliclte rele eetistie eile 125 —Dentate crested hooks present'in posterior segments if INCOXe GEMAb VEC! eb 656 .6.1B'0.4'6 oibLg Ao\ p10. 0/0'0'4. 0°o ol OU'E OlS Beeb Ole GC Oploa'd 06.000. Olan '5 O.0!0 138 —Capillary setae crenulate ..................... F. Orbiniidae 126 = C@apillanysetae smoothiarniy. cite ie rye torres eciei bene acl ner es ete ele) eee) test 132 Proc. LINN. Soc. N.S.W., 104 (1), (1979) 43 ( 3) (13) ( 3) ( 5) ( 3) ( 3) ( 3) ( 3) ( 3) ( 3) 1980 44 ESTUARINE POLYCHAETES 126. —Prostomium round; change from thorax to abdomen about setigen 280.) 72 Sige ces cute ire sateen aes a —Prostomium pointed ; thorax of less than 23 setigers ....................-5---. 127. | —Thorax with several foot papillae and many stomach Papillae yy ie eee ise ee are el aues tile lal ah ok oer eras eas — Thorax with 1-2 foot papillae, no stomach papillae.......................... 128. —No anterior row of hooks among thoracic neurosetae . —Anterior row or rows of hooks among thoracic NEUFOSELAE 7h eva sti cct occult Halts yo elionead AaNteN Sea boy arate ueiiey « Rearenaan Ween oe gee uNse7 es omen 129. — Thorax of 19-22 setigers; branchiae from setigers 8- A Ca ee I eile cara NG ie se oes acrae OUR Sa eae Reh — Thorax of 14-15 setigers; branchiae from setigers 15- UG ye sae h ieee peat eatertapninlae sekim ee Isyattdelieigen cds suum 130. —Single row of slender hooks among thoracic MEUTOSEE AE). eo) Ue zagch su nae al aise een cee h cra uae rolcapa ate —Three to four rows of hooks among thoracic MEUNOSEL AEA cil n Ne nee Sees atu ses: ale Maan otnat a 131. — Thorax of 13-17 setigers; branchiae from setiger 9-11 — Thorax of 16-18 setigers; branchiae from setiger 12- Dai ti Masala co tale cy Sane oan ana tMiou yin ie erere Te Ese Ie oc tm Be 132. —A single long filiform branchia arising from dorsum OSEtIPETs2 OT. See iat ieee ced a neh eae a ote as —Branchiae, if present, not single and median...................0--e see eeeee 133. —Capillaries winged in anterior segments; median antenna may be present ...................... —Capillaries not winged; median antenna never [eices{lelee al oMteee eeuc of beni Me mao ncn bleep olMiog nino tid amie sa thats Midie ian a bina obo g'efh bo 134. —Prostomium with median dorsal antenna; specialized setae, 4 curved unidentate hooks among capillaries of posterior neuropodia ......................0-. —Prostomium without an antenna; specialized setae among capillaries of posterior neuropodia......... 135. —Prostomium a tapered cone; body fusiform, often groovediventrally eer oe bos | ates oetien: —Prostomium notched or lobed; body swollen anteriorly but not grooved ventrally ............. 136. —Ventral groove present; branchiae present from setiger 2 for about 24-25 setigers; eye spots between parapodium of middle segments................ —Ventral groove present, branchiae absent; eye spots El of oin ast its es Vaile a abaiolee be fokata oy ale tupes oracle 137. — Body arenicoliform; posterior parapodia lack ventral and dorsal cirri; branchiae absent ..:........... —Body arenicoliform; posterior parapodia with both ventral and dorsal cirri; branchiae absent......... 138. — Body resembles an earthworm; dentate crested hooks withthoods) ise al os eaten anh 1a ayes Ol Feit ran areal —Body does not resemble an earthworm; dentate crested hooks without hoods ..................... 139. —Genital setae present in both sexes on setigers 8-9; thorax/ofil Ojsetigersiy egy eis eee eel — Genital setae absent or only present in males; thorax Of setigens 2s sry utenti Nave anaes al ay aia WLSsIonG aie arty LEM eer egy ennui eg erie 140. —Genital setae present in males; thorax of nine Proc. LINN. Soc. N.S.W., 104 (1), (1979) 1980 Nainerts grubet australis L. bifurcatus L. normalis Scoloplos (Scoloplos) Scoloplos (Leodamas) johnstonez Scoloplos (S.) simplex Scoloplos (S.) sp. F. Cossuridae-Cossura sp. Aricidea fauveli Paraonis sp. F. Opheliidae F. Scalibregmidae Armandia intermedia Polyophthalmus pictus Hyboscolex dicranochaetus Pseudoscalibregma sp. F. Capitellidae (4, 13) 127 (4, 13) 128 129 130 (4, 13) (4, 13) 131 ( 4) (4, 13) 133 134 135 ( 3) 136 137 ( 3) ( 3) (14) 139 149 (13) 140 141. 142. 143. 144. 145. 146. 147. 148. 149. 150. 151. 152. 153. 154. 155. 156. P. HUTCHINGS AND S. RAINER setigers; hooks thereafter............ — Body colourless; when preserved capillaries in anterior thoracic setigers, — Body with bright red pigment spots.............. —Ten thoracic setigers, with capillaries in setigers 1-4 and hooks in setigers 5-10..... —Morejthaniten' thoracic setigersjisn asses saci a ae ce dea eee ae el eVveEnbENOTACleisebiGensnn hi Uian clan mics Maayncel ential eniie sia thw sync usatiscura tas tye leve = Morethanyl lithoracicisetigersiny «a says ise cic tees oe ieee nes eeiese eo le oe cee — Thoracic setigers all capillaries . — Thoracic setigers with capillaries and hooded hooks —Neurosetae present —Neurosetae absent on first thoracic setiger —Eyes embedded in segment 1; globular branchiae on first thoracic setiger ........ present on posterior abdominal setigers........... —Elliptical eye spots on segment 1; often purple in colour; branchiae absent....................-. — Thoracic setigers 1- — Thoracic setigers 1- —Twelve thoracic setigers; abdomen ends in anal 5 with capillaries, 6-11 with hooks 6 with capillaries, 7-11 with hooks plate; branchiae absent...................... — Thirteen thoracic setigers; no anal plate; retractile branchiae —Middle setigers greatly elongated, never annulated ; branchiae rare... —Middle setigers not greatly elongated but annulated ; branchiae present. —Cephalic plate absent; cephalic ridge well marked; pygidium petaloid with centralanus............. —Cephalic plate well defined, surrounded by raised margin; pygidium variable — Pygidium as a slanting plate with a dorsal anus above it, anal cirri absent —Pygidium encircled by anal cirri with anus sunken in EV IADR OVS ei ee hi React easy ariaherc by oly ace melee eo sels Ale bars BRCM n a esa Water e Wala gum veatae winec. cen acc —Neurosetae of setigers 1-3, four dentate crested hooks similar to subsequent ones —Neurosetae of setigers 1-3, four acicular setae, different from subsequent ones................. —Setigers 1-3 with simple smooth acicular neurosetae; 2 achaetous pre-anal segments; anal funnel with 27- 29 equal cirri plus one longer .................. —Setigers 1-3 with simple smooth acicular neurosetae ; five achaetous pre-anal segments; anal funnel with allicinnilequalhimisizemiar nice iii ror aac nl —Branchiae from setiger 20, branchiferous segments with two annuli; animal small not exceeding 40mm . —Branchiae from setiger 7-17, branchiferous segments with five annuli; animal large.................. —Head with frilled food gathering membrane; lives in firm sandy tube . . —Head without frilled food gathering membrane ead withistoutsetae ian for neo — Head without stout setae Proc. Linn. Soc. N.S.W., 104 (1) Capitella 141 Medea seas Penmaes essctemer amet 142 C. capitata Capitella sp. Mediomastus californiensis 143 144 148 Notomastus 145 SOI ELON ONION Manor eere 147 Notomastus sp. Baa bags Ira i ape ane ON BAe mae ae ects 146 N. torquatus Notomastus sp. Heteromastus filiformzs Barantolla lepte Scyphoproctus djiboutienses Dasybranchus sp. F. Maldanidae 150 F. Arenicolidae 154 Petaloproctus sp. SISO Ico eR Ee TERE roa rAaT 151 Asychis sp. 152 Axiothella sp. Euclymene 153 E. trinalis Euclymene sp. Branchiomaldane sp. Arenicola bombayensis F. Oweniidae-Owenza fusiformis ai Cee rowel coat eNt Wot eb reamed 156 F. Flabelligeridae 157 Hit as Hen AS ne aoh Sta ha 159 45 ( 3) (13) (13) (13) (13) ( 3) (11) (13) ( 3) , (1979) 1980 46 ESTUARINE POLYCHAETES 157. —Neurosetae simple hooks; branchiae filamentous, arise in single marginal row from cephalichood .... = Pherusasp. —Neurosetae not simple hooks; branchiae filamentous or cirriform(\arisejin'2(or, MOre|TOWS))s als. elie ee 158 158. —Neurosetae annulated with bent or minutely hooked tips; a few stout branchiae in 2 distinct groups ..... Diplocirrus sp. —Neurosetae stout compound hooks; numerous fine branchiae in several irregular rows .............. Flabelligera sp. 159. —Head with soft tentacles for deposit feeding; branchiaempresemt ss.) 25h Syste ees ae esi orsitet elec aie fe cen ania baleen -o aratrn er atte are ptr ee 160 —Head with branchial crown for suspension feeding ; segmental }branchiae/absemty. 6 she ei ars aiccssrnicciacein upset ten ree ee eee ents eee 179 160. —Tentacles retractile into mouth, either grooved or Papillose ye) Rye het eMon i amote coh enseetelatiags F. Ampharetidae 161 —Tentacles not retractile into mouth, grooved, never Papillose secs richmn AS Wauwut crc Aaara ECA my caes lala what earls eget aver Aer wt ema dis anon bere 164 161. —Stout postbranchial hooks present; paleae absent; buccal tentaclessmooth ...................... Isolda pulchella ( 3) 162. —Buccal tentacles papillose..................... Pseudoamphicters papillosa (12) —Bucealitentacles smooeh 5.72 /51.05 yrs ye Sia ites ict i cite ete ee talie alee mene aleeete 163 163. —Glandular ridges present; four pairs of smooth gills; 14 uncinigerous thoracic segments; body with green PISMENt Spots see sri ite seen eee ete epee aaa Amphicteis dalmatica (13) —Glandular ridges absent; three pairs of smooth gills; 12 uncinigerous thoracic segments .............. Samythella sp. 164. —Branchiae absent; tentacular lobe expanded ...... F. Terebellidae SF. Polycirrinae 165 —Branchiae present; tentacular lobe expanded or COMP ACC Meee Hii oneal aye yh UN cre ane ea Ceeebs aay usu ai Oe Ate ci ee OR 167 165. — Abdominal setae completely absent ............. Lyszlla 166 — Abdominal setae restricted to acicular notosetae.... Amaeana trilobata (12) 166. —Ten thoracic setigers; notosetae simple smooth capillaries, neurosetae absent.................. L. apheles (11) —Nine to 12 thoracic setigers; notosetae barbed, Meurosetaejabsentar yay ieee cane ae L. pacifica (12) 167. —Tentacular lobe and peristomium compact........ F. Terebellidae 168 —KEither tentacular lobe or peristomium expanded.... _ F.. Trichobranchidae 178 168. —Branchiae simple filaments on setigers1-3.......... 0.0.00... e cee eee eee ee 169 —Branchiae branched or club shaped on setigers 1-3 ................000- 00 ees 174 169. —Uncini of first four rows, heavily chitinized long- handled hooks; following ones avicular........... Hadrachaeta aspeta (12) —Uncini all avicular with forwardly projecting bases ....................000--- 170 170. —Notosetae from segment 2 (first branchiferous) .... Streblosoma 171 —Notosetae from segment 3 (second branchiferous) ....................00-00- 172 171. —Twenty-five—29 pairs of notosetae; three pairs of branchiae forming continuous band across dorsum . . S. acymatum (13) — Twenty-one pairs of notosetae ; two pairs of branchiae with distinct median gap separating left and right hand! pairsye yey incre em hin tees cuekomouet Streblosoma sp. 172. —Notosetae from segment 3 (second branchiferous) ; UN cinitKomNsetiper saree eee cen Thelepus 173 —Notosetae from segment 3 (second branchiferous) ; UNGInipfromiIsetigerO4 Ae Eeiocn i riarece: Rhinothelepus lobatus (11) 173. —Notosetae terminate halfway along abdomen, uncini Proc. Linn. Soc. N.S.W., 104 (1), (1979) 1980 P. HUTCHINGS AND S. RAINER with terminal button; branchiae of numerous fala rrvem siete here save See eee core eau cake Aaeaeatients T. setosus —Notosetae more than 20 pairs; uncini otherwise; three pairs of branchiae with few branchial filaments arising on horizontal ridges, filaments of first extend Vatenalllyies eae its es sauce Vie Ase eb teases bas teehee Thelepus sp. 174. —Branchiae club-shaped; anterior uncini avicular but base produced backwards as long shaft........... Pista typha —Branchiae branched; all uncini similar, either avicular or pectiniform...... IBA RIGHT aM na ce ee tea oi Mee cd Soe 175 175. = Notosetae with; smoothitips Grevillea sericea 0 12 0 6 0 05 O 2.0 0 LOO R Hakea teretifolia 0 10 0 5 0 (aos) AY) 3.5 0 8 100 8 *Pultenaea sp. 0 4 0) 2 0 0.1 O 2.0 — — 100 & *Hakeoa dactyloides 0 4 0 2 0 2.6 0 2.4 = = 100 *Kunzea capitata 0 2 0 1 0 0.5 0 3.5 — 00S *Leptospermum sp. 0 2 0 1 0 0.3 0 2.0 = — 100 *Conospermum longifolium 0 2 0 en wo) 06 O 2.0 — — 100 *Pultenaea elliptica 0 4 Ona 0 06 O 2.5 — — 100 {Overall average ZelB) oe) Za) Pao) +Monocotyledons: not included in RIV calculations *Species that occurred in less than 5% of all the quadrats: not included in RIV calculations {The overall average does not include species marked* and it is not presented in the results. All computations were run on a UNIVAC 1100 computer at Macquarie University. RESULTS TABLES 2 AND 3 When species with an exclusiveness value of greater than 85% were assigned to the soil where they were most frequent, three distinct groups which were readily visible in the field resulted: podzol species, species common to both soil types, and non- Proc. Linn. Soc. N.S.W., 104 (1), (1979) 1980 R.A. BUCHANAN AND G.S.HUMPHREYS 59 podzol species. This classification applies only to the sampled areas, as none of the podzol species is restricted regionally to this soil. The ratio of these three groups (podzol: common: non-podzol) for the full species list at Site A is 1.5: 1: 3.25. Not only is the group of species common to both soils the smallest, but it also contributes only a quarter to the total RIV on the podzol and slightly less than half on the non-podzol. At the more sheltered, moister Site B the podzol group is the smallest, with the common and non-podzol groups the same size (1: 1.5: 1.5). At this site the group of species present on both soils contributes well over half to the RIV total on the podzol and slightly over a half on the non-podzol. Vegetation on the Podzol. The species locally restricted to the podzol and present at each site are Ceratopetalum gummiferum, Ricinocarpos pinifolius, Gompholobium latefolium, Xylomelum pyriforme and Xanthorrhoea arborea. At Site A, C. gummiferum is the principal species on the podzol. This single species contributes 70% of the summed values for the basal area, 40% for height, 26% for density and 16% for frequency to give a total score of 152 out of 400. The next two most important plants on this soil, R. penzfolius (RIV 42) and Phyllota phylicoides (RIV 35), attain a score of less than a third of that for C. gummzferum. Although these two podzol species are quite common, their small size makes them a less important and less conspicuous part of the flora. At Site B there is no clear principal species on the podzol. A species common to both soils, Dzllwynza retorta, has a score of only 94, with C. gummiferum reaching a value of over half this score at 55. Another species common to both soils, Leptospermum attenuatum, is the third most important species (RIV 32). The regionally less-common species Podocarpus spinulosus is confined to the podzol at Site B where it is the second most frequent species. C. gummiferum is less important at the more sheltered Site B than at Site A even though it is usually found in moist, sheltered places. At Site B the plants were larger (average height and basal area 3.5 m and 8 cm’ respectively) than at Site A (average height and basal area 2.5 m and 6 cm’) but only 35 stems were recorded at Site B compared with 184 stems at Site A. This difference may be caused by a lower fire TABLE 4 Principal component analysis, in quadrats (100) of vegetation RIV data: table of components and their respective eigenvalues site component eigenvalue % variance cumulative variance accounted for % A 1 2.5169 9 9 2 1.9165 7 16 3 1.6483 7 23 4 1.4765 5 28 5 1.4134 5 33 6 1.3181 5 38 7 1.2825 5 43 8 1.1935 4 47 B 1 2.2376 10 10 2 1.6529 7 17 3 1.5981 7 24 4 1.5219 6 30 5 1.4715 7 37 6 1.3452 6 43 7 1.1847 5 48 8 1.1707 5 53 Proc. LINN. Soc. N.S.W., 104 (1), (1979) 1980 60 VEGETATION ON PODZOLS frequency, as plants in fire-prone areas tend to have larger numbers of smaller shoots than plants in less fire-prone areas. P. phylicozdes is the only species that grows on the opposite soil at each site but a few species are confined to one soil at one site and common to both soils at the other. Vegetation on the Non-podzol. A species common to both soils, L. attenuatum, is the most important species on the non-podzol at both sites. At Site A there is no predominant species on the non-podzol. L. attenuatum and another species common to both soils, Banksza serrata, are the most important species with RIV totals of 68 and 56 respectively, while the non-podzol species, Petrophile pulchella, has a score of 45. There are a large number of infrequent non-podzol species at this site. At Site B, L. attenuatum has a RIV of 73. The next most important species, Banksia marginata, is mostly restricted to this soil and has a score of 68, while another species common to both soils, Dillwynza retorta, has a RIV of 45. B. marginata has a very high frequency (98%) and is therefore a conspicuous species on this soil even though its RIV is not large. PRINCIPAL COMPONENT ANALYSIS The first component of the row analysis accounted for over 30% of the variability and with the second component over 40% at both sites (Table 5) with the first component representing the change in soil type. The Site A analysis shows three groups (Fig. 6), the podzol group and two groups on the non-podzol. The two podzol border rows, nine and ten, are included within the podzol group but the non-podzol border rows, eleven, twelve and thirteen, lie midway between the podzol group and the other non-podzol rows along the first component. In these three rows, species common to both soils are important ingredients and many of the non-podzol species are absent. Within the non-podzol group there is a gradation from rows fourteen to twenty along the second component. This may relate to drainage and slope. At Site B the podzol group is split into two sub-groups, with the two rows on the steeper slope adjacent to the creek well separated from the other podzol rows along the TABLE 5 Principal components analysis, in rows, of vegetation RIV data: table of components and their respective eigenvalues site component eigenvalue % variance cumulative variance accounted for % A 1 8.5464 32 32 2 3.0693 11 43 3 2.5654 10 53 4 2.3691 8 61 5 1.7961 7 68 6 1.5891 6 74 7 1.5119 5 79 8 1.3026 5 84 B 1 7.0695 31 31 2 3.1869 14 45 3 2.9750 13 58 4 2.2209 9 67 5 1.8840 8 75 6 1.7358 8 83 7 1.4994 6 89 8 0.6869 3 92 Proc. Linn. Soc. N.S.W., 104 (1), (1979) 1980 R. A. BUCHANAN AND G.S. HUMPHREYS 61 Fig. 6. Site A. Plot of the lst x 2nd principal component scores of the twenty rows. The location of rows is shown on Fig. 10. © Podzol row A Non-podzol row. Fig. 7. Site B. Plot of the Ist x 2nd principal component scores of the fourteen rows. The location of rows is shown on Fig. 11. © Podzol row A Non-podzol row. Proc. Linn. Soc. N.S.W., 104 (1), (1979) 1980 62 VEGETATION ON PODZOLS second component (Fig. 7). In both rows, two out of the three most important species are common to both soils but these rows contain the only intrusion of a non-podzol species, Hakea gibbosa. Podzol species such as C. gummiferum and R. pinifolius are also present and the mixture of podzol and non-podzol species guaranteed that these two rows would be plotted well away from the main groups. The podzol border rows, six and seven, are within the main podzol group but the two non-podzol border rows, eight and nine, lie between the podzol and non-podzol groups along the first component. As for Site A, the non-podzol border rows are dominated by species common to both soils, while many non-podzol species are absent. Although the podzol and non-podzol plot out as two distinct groups there is a rough ordering from rows three to fourteen along the first component. NORMAL ASSOCIATION ANALYSIS The first two divisions in the normal association analysis at Site A define the podzol vegetation, while at Site B the first division basically divides the vegetation into podzol and non-podzol (Figs 8 & 9). The community maps (Figs 10 and 11) show that only 6% of the quadrats at Site A and 10% of the quadrats at Site B do not conform to the soil groups. Even this small amount of non-conformity seems to be the result of the highly artificial classification system, as the chance occurrence of one species in a quadrat can dictate its final grouping. When the relative importance values of the species are considered most of LEGEND + Positively associated - Negatively associated N No. of quadrats Ceratopetalum gummi ferum = 2 uJ = 2 [e) O 2 < E a = S re = Epacris itt if Uf Ricinocarpos bay ate) Pinifolius Hibbertia linearis Se anoe Sooes Mapping group No. as used on Fig. !0 b. Fig. 8. Site A. Normal association analysis. Proc. Linn. Soc. N.S.W., 104 (1), (1979) 1980 R.A. BUCHANAN AND G.S.HUMPHREYS 63 these apparent discrepancies disappear. Even the well-defined finger of non-podzol vegetation that intrudes into the podzol on the Site B community map is the intrusion of a single species, B. marginata. This species is unimportant in these quadrats. DISCUSSION All results, whether those of the exclusiveness calculations, the association analysis or the principal components analysis, showed that there was a difference in the vegetation on the podzol and the non-podzol soils at each site. This difference was less evident at the moister, more sheltered Site B than at the plateau site, Site A. At Site B there were more species common to both podzol and non-podzol soils, and these species were more important than at Site A. The vegetation characteristic of the podzol soil is present to the podzol boundary where it ceases abruptly. At both sites, on the non-podzol soil the vegetation close to the soil junction is dominated by species common to both soils, with many of the non-podzol species being infrequent. Though the two podzol sites differ in topographic terms, the vegetation on both podzols looks remarkably similar. Extensive field reconnaissance within the Sydney Basin has shown that the vegetation on these two sites is typical of most podzols on the sandstone plateaux. LEGEND + Positively associated — Negatively associated N No. of quadrats Banksia marginata Dillwynia retorta pe 2 ud = 2 1e) O 2 2 Ee 60 <— Coal and Candle Creek oD + Pittwater | 0) 1 | 2 3 7 5 km 6 | | ay | 3| | © = | 5| zl =| S + | 3! =| a| ay =| m | il G | yee 120 V | 4 60 0) (0) ] km (0) 1 2km Fig. 3. Topographic sections of the Lambert Peninsula. Sections located on Fig. 1. Proc. Linn. Soc. N.S.W., 104 (1), (1979) 1980 78 ; THE LAMBERT PENINSULA these creeks (Fig. 3, sections E-F, G-H) show that the Yeomans Creek valley is steep- sided and narrow, while Salvation Creek occupies a broad valley with gently sloping sides. Steep slopes (Slope Class 1, slope >15-20°) are virtually restricted to the coastal cliffs and some deep gullies on the eastern half of the peninsula, but on the western side these slopes intrude deeply (Fig. 4). The intermediate slope class (Class 2, 5° to 15° or 20°) covers large areas on both sides of the peninsula, but it is most common on Slope classes :- FJ 1. > 15°- 20° N 2. 5%15° or 20° L] 3. <5° — division between east and west drainage SF Gymnoschoenus sphaerocephalus Gahnia sieberana e Banksia robur 5 swamp number 5 podzol number eal ante 0) 1 2 3km Fig. 4. The distribution of the three slope classes, podzols, swamps and three swamp plants, Gymnoschoenus sphaerocephalus, Gahnia steberana and Banksia robur. Proc. Linn. Soc. N.S.W., 104 (1), (1979) 1980 R. A. BUCHANAN 79 the western half. The most gentle slope class (Class 3, <5°) is almost confined to the eastern side, with only very small areas present in the west. The causes of the asymmetry are not known but the gentle easterly slope of the surface of the Hawkesbury Sandstone and the easterly trend of the cross-beds (Standard, 1969) may be responsible. PODZOLS Podzol soils on the sandstone plateaux have only recently been described in detail (Buchanan and Humphreys, 1980) and the vegetation characteristic of these soils was first mentioned in the above paper. All twenty-eight podzol soils (at grid references listed in Appendix 1) which were found on the peninsula occur in low slope areas (Fig. 4). Only six of these are on the western side and these six occur in isolated small areas with a gentle slope. Podzol soils develop in deep (1-4 m) quartz sand deposits which may cover an area from less than 0.1 ha to approximately 5 ha. These deposits frequently occur near creeks or swamps. The vegetation growing on these soils is very similar throughout the peninsula. The trees are usually taller (open-forest/woodland; Specht, 1970) than the surrounding Eucalyptus haemastoma Sm. association of low open-forest/low woodland. They can therefore be identified on aerial photographs with a high degree of confidence using the characteristics of gentle slope and taller vegetation, and in the field, the floristics of the tree and understorey layers aids identification of these soils (Buchanan and Humphreys, 1980). SHRUBLANDS The term shrubland has been selected as the clearest description of shrub- dominated areas, although it has been used in vegetation classifications (Specht, 1970; Forster, Campbell, Benson and Moore, 1977) to refer to shrub communities of specific height and density. The shrub-dominated areas on the peninsula fit into many categories in these detailed classifications and the term shrubland in this paper does not imply a specific height or density of shrubs. In a floristic survey of Ku-ring-gai Chase, Outhred, Lainson, Lamb and Outhred (in preparation) classify shrub- dominated areas in a fashion broadly consistent with that adopted by Specht. The distribution of shrublands does not appear to be influenced by aspect or shelter (Pidgeon, 1938) but rather by soil depth and drainage. Fairly extensive areas of shrubland interspersed with rock outcrops occur on the peninsula, especially at the northern end (Fig. 5). Shrublands develop in these areas as resistant sandstone beds near the surface prevent trees becoming established. However, much of the shrubland is not broken up by rock outcrops and the presence of shrubland in these areas is controlled by a number of factors, all of which result in poorly drained soils. The majority of these moist shrublands have a low surface slope and are most common on the gentle slopes on the eastern side of the peninsula. A puggy material is often present approximately 1 m or less below the surface and it effectively prevents rapid drainage. Extensive sandstone benches also impede drainage and many moist shrublands are perched on benches with the sandstone revealed on the downslope side (Fig. 2). The extremely broken topography of the western half of the peninsula does not allow impeded drainage except on small benches. On the eastern half, the boundary between shrubland and trees is sometimes ill- defined but it is frequently very sharp and coincides with the change from a poorly- drained to a well-drained soil. Observation during and after torrential rain showed that the surface soil under the trees never became waterlogged but the shrubland soil became waterlogged, and remained so for days. This rapid change in soil drainage Proc. Linn. Soc. N.S.W., 104 (1), (1979) 1980 80 THE LAMBERT PENINSULA may occur over as short a distance as several metres, and matches exactly the tree/shrub boundary. The most spectacular examples have a very obvious change in understorey as well, and are often the result of an abrupt junction between clayey sandstone and sandstone (Fig. 6). An equally sharp shrub and tree boundary, but a more gradual change in the understorey, takes place when the clayey sandstone thins or deepens beneath the trees. Many of these moist shrubland/tree boundaries obviously occur at joints which mark this change in rock type and involve little or no change in surface topography. Slope classes :- 1. > 15°- 20° 2. 5°- 15° or 20° (Gul 3° <5¢ division between east and west drainage WW shrubland interspersed with rock outcrops Z shrubland with few rock outcrops swamp Fig. 5. The distribution of the three slope classes; shrubland and swamps. Proc. Linn. Soc. N.S.W., 104 (1), (1979) 1980 R. A. BUCHANAN 81 Joints which control the direction of cliffs often mark a change in vegetation as well as surface elevation. Fig. 2 shows a clear example of shrubland on a rock.shelf and an area covered by trees immediately below the cliff north-west of Podzol 15. Rapid changes in surface and subsurface slope can also cause an abrupt change in soil drainage. SWAMPS The distribution of swamps in the West Head to McCarrs Creek area is strongly controlled by lithology and topography. Areas need a fairly constant inflow of water as well as a slow loss of water for swamps to develop. The simplified and generalized longitudinal section of the swamps on the peninsula (Fig. 6) shows the suitable conditions for swamp development. The first requirement is a gentle slope. Twenty-three of the twenty-seven mapped swamps (grid references listed in Appendix 2) occur in areas with a slope of 5° or less (Fig. 4). Only two of the valley-floor swamps, which form along creeks, occur where the general surrounding slope is greater than 5° (Nos. 17 and 21) but all of the valley- floor swamps and valley-floor elements of composite swamps have a longitudinal slope between 0° and 3°. Some valley-floor swamps are probably situated directly on extensive sandstone benches in these near horizontal segments of the creek beds. Valley-side swamps are frequently perched on rock shelves on the valley slopes and may have a slope of up to 10°. The second requirement is the presence of the puggy material in the swamp catchment. Water percolating vertically through the overlying sandy soil and sandstone beds will saturate the puggy material and water seeping from it provides a fairly slow and constant supply to the swamps in dry periods. This layer may sometimes continue laterally under readily-draining sandstone beds and, if this is so, the catchment of these puggy layers may be considerably larger than augering indicates. The presence of this puggy material near the surface is indicated by the presence of moist shrubland, and all swamps except No. 15 and the valley-side arm of No. 4 receive drainage from moist shrubland. The swamps may occur immediately Cnn ~ [=] sand ' t Lg tohinfer, 1 VV 4 wr UCT Va ren — ea Swamp fill ws sh / = Clayey sandstone ee Sandstone Low woodland Moist shrubland eg. Hakea teretifolia SG RENEE ING Gan ae Swamp e.g. Gahnia SLVR ee it a Se LAIR ie ion . WW) BAN ait (igi be Fig. 6. Simplified and generalized longitudinal section of the swamps on the Lambert Peninsula. Proc. Linn. Soc. N.S.W., 104 (1), (1979) 1980 82 THE LAMBERT PENINSULA downslope of such areas or they may be connected by a creek. Some swamps are directly underlain by the puggy material. Phystographic Types Valley-floor Swamps Valley-floor swamps are linear, as they form along creeks. They have a cross sectional slope of 0° and a longitudinal slope of 0-3°. Swamp 21 (Fig. 7a, Fig. 9a) is an example of the simplest type of valley-floor swamp, as there is no zonation between the tall, dense swamp vegetation and the low woodland (sensu Specht, 1970) growing on the adjacent steep, rocky slopes. The iron/organic swamp fill is up to 2 m deep and a thick layer of sand is present between the swamp fill and bedrock. The main creek channel is on the least sandy side of the swamp, immediately adjacent to the rocky slope. Swamp 11 (Fig. 7b) is an example of a common valley-floor type. In the area of the section, the gradual slope change along one side of the swamp has allowed a very narrow zone of short swamp vegetation to develop between the tall and dense swamp vegetation and the low woodland. In other places along this border a thin zone of dense Banksza ertczfolia has developed and such fringes are fairly common on the peninsula. Many valley-floor and composite swamps have a short (0.5-2 m) steep sandy rise along the edge. A podzol soil supporting a distinctive podzol vegetation occurs on these rises (Buchanan and Humphreys, 1980). Valley-side Swamps These swamps are very variable but frequently have a fairly steep slope (3-8°) and are sometimes controlled by the underlying rock shelf. Hanging swamps described by Pidgeon (1938) are probably valley-side swamps perched on rock shelves. Swamp 14 (Fig. 7c) is not controlled by cupping of the underlying rock shelf, as the shelf slopes upward at approximately the same angle as the soil surface, 3°-7°. No creeks drain into this swamp so water levels must be maintained by downslope seepage, and drainage is probably impeded by the relative scarcity of joints in the rock shelf. The vegetation types indicate fairly dry conditions, as only a narrow zone of dense swamp vegetation occurs. Broader zones of short vegetation occur on either side of the wettest area and the usual fringe of mixed vegetation is present along the rock shelf boundary. Swamp 4 (Fig. 8d, Fig. 9c) is the steepest (slopes up to 14°) in the area and it is the only example of the following type. A cliff 4 m high above a puggy material layer occurs at the upslope edge of the swamp. The presence of tall and dense swamp vegetation at the base of the cliff, as well as the geological relations, indicate that water draining from the overlying sandstone seeps out of the clayey layer at the base of the cliff. Further downslope, drier conditions only enable a swamp with short vegetation to form. Sand washed down the slope has accumulated in irregularities in the bedrock, giving the hillside a smooth rather than terraced profile. The iron/organic fill forms a continuous skin over the sand and rock. On each side this hillside swamp is bordered by well-drained soils carrying a low woodland of Eucalyptus haemastoma, and the boundary between swamp and low woodland is remarkably sharp. Composite Swamps These swamps consist of a valley-floor element and the bordering gentle (0-3°) hillslope. A decrease in soil moisture and a greater fluctuation in soil moisture occurs from the valley-floor up to the hillslope. The water-table fluctuations are influenced by such features as the surface and bedrock slope, the permanence of the creek, the Proc. LINN. Soc. N.S.W., 104 (1), (1979) 1980 R. A. BUCHANAN (a) fk sandstone al SWAMP: vegetation- sb A = puggy material ; swamp fill —— podzol pan surface low woodland tall and dense —— approx. height of the vegetation ( understory in low woodland ) st (b) 10 SWAMP:- vegetation- 8 low woodland low woodland m 6 short talland dense 4 LEO - ple as 0) 20 40 m 60 80 100 (c) SWAMP: vegetation- a low woodlan 8 ea mixed shrubland short dense short Tee eet we Fig. 7. Swamp sections: a) Swamp 21, valley-floor. b) Swamp 11, valley-floor. c) Swamp 14, valley-side. Proc. Linn. Soc. N.S.W., 104 (1), (1979) 1980 84 THE LAMBERT PENINSULA distance from the creek, and the depth, thickness and extent of the puggy material. The type and extent of swamp vegetation on the hillslope is therefore very variable. Swamp 13 (Fig. 8e) shows the zonation up the hillside. As usual, the tall and dense swamp vegetation is present on the valley-floor component. A change in slope from 0° to 2° and the presence of puggy material cause a rapid decrease in vegetation height to an area dominated by Gymnoschoenus sphaerocephalus. A gradual but still readily distinguishable change from short to mixed swamp vegetation, then to moist shrubland occurs as the soil becomes progressively drier upslope. At Swamp 13 the zone with mixed vegetation characterized by Lepzdosperma flexuosum is only a narrow and discontinuous band. Vegetation Types Four distinct but intergrading swamp types occur in the Lambert Peninsula area. Listed in order of decreasing soil moisture, they are swamps with 1) tall and dense po (d) 22. GRRE ED Gr TaaS SRT sandstone SWAMP: vegetation- [-] sand =| puggy material swamp fill —— podzol pan surface -} tall and —— approx.height of the vegetation ( understory in low woodland ) (0) 20 40 m 60 80 100 (e) 8 : p | low woodland SWAMP: vegetation- low woodland_> 6 tall and dense short mixed moist shrubland 20 2° ea _— bb 0 0) Ouse = = —— : Cok ere 0) 20 40 m 60 80 100 Fig. 8. Swamp sections: d) Swamp 4, valley-side. e) Swamp 13, composite. Proc. Linn. Soc. N.S.W., 104 (1), (1979) 1980 R. A. BUCHANAN 85 vegetation, 2) dense vegetation, 3) short vegetation and 4) mixed vegetation. Moist shrubland is frequently associated with swamps and is included in this section. Only nine species have been recorded in swamps with tall and dense vegetation but as the swamp type becomes drier, the number of species present becomes greater. This trend is partly reflected in Table 1 where only the most common species are listed. TABLE 1 List of typical species present in the four swamp types and moist shrubland Swamps: vegetation — Moist talland dense short mixed shrubland dense Utricularia cyanea R. Br. Banksza robur Cav. Baeckea linifolia Rudge Leptospermum juniperinum Sm. Aotus ericoides (Vent.) G. Don Gleichenza dicarpa R.Br. Gahnia steberana Kunth Baumea arthrophylla or sp. aff. Empodisma minus (Hook.f) Johnson & Cutler syn. Calorophus minor Hook f. Lepidosperma forsythzz Hamilton L. longitudinale Labill. Cassytha glabella R.Br. Epacris obtustfolza Sm. Sprengelia incarnata Sm. Banksia ericifolia L.f. Viminaria juncea (Schrad.) Hoffmgg. Lepidosperma flexuosum Labill. L. limicola N. Wakefield Schoenus paludosus (R. Br.) Poir. Schoenus sp. Gymnoschoenus sphaerocephalus (R.Br.) Hook.f. Xanthorrhoea resinosa Pers. ssp. restnosa Leptocarpus tenax (Labill.) R.Br. Drosera spathulata Labill. D. pelata Sm. ex Willd. Xyrzs operculata Labill. Lycopodium laterale R.Br. Baeckea imbricata (Gaertn.) Druce Leptospermum squarrosum Soland. ex Gaertn. Bauera rubioides Andr. : Dillwynia floribunda Sm. var. floribunda Hakea teretzfolia (Salisb.) J.Britt. Banksza asplenitfolia Salisb. Lepyrodia scariosa R.Br. Restio complanatus R.Br. R. fastigcatus R.Br. Actinotus minor (Sm.) DC. Angophora hispida (Sm.) Blaxell syn. Angophora cordifolia Cav. Kunzea capitata Reichb. Grevillea speciosa (Knight) D. McGillivray syn. Grevillea punicea R.Br. Isopogon anethzfolus (Salisb.) Knight Petrophile pulchella (Schrad.) R.Br. syn. P. fuctfolia (Salisb.) Knight ‘Persoonia lanceolata Andr. Epacris pulchella Cav. HK mh OO Ph PK PS Ke PS PS OS OS PS PS OS OK OO OO mmm MK ~*~ x ~ Ke KM MM KKK mm mm RK RK Kh RO Proc. Linn. Soc. N.S.W., 104 (1), (1979) 1980 86 THE LAMBERT PENINSULA Two of the plant species which occur in swamps have interesting distributions (Fig. 4). Banksza robur occurs only in the southern and eastern corner of the area. Its absence from apparently suitable habitats in the northern swamps is difficult to explain, especially as it occurs immediately north of the peninsula in the Gosford district. The western swamps may be too dry. A very common swamp species in the Blue Mountains and south of Sydney, Gymnoschoenus sphaerocephalus, occurs only in the Salvation Creek catchment. Like B. robur, its absence from other swamps is unexplained, as apparently suitable habitats occur elsewhere on the peninsula. Gahnia steberana, by contrast, occurs in all suitable habitats on the peninsula and only the largest occurrences have been marked on Fig. 4. This bird-dispersed species appears to spread more rapidly than the wind- or water-dispersed B. robur, as mature individuals occur in moist places along the verges of the West Head Road. Because of the anomalous distribution of some major species, the wide range of water tolerance of some species, and the importance of fire frequency on species distribution, it is necessary to divide swamp types on criteria other than species presence or absence. The four swamp types and moist shrubland were divided by the characteristic height and abundance of some of the larger species (Table 2). Swamp species such as B. robur, Gahnia steberana, Leptospermum juniperinum and Empodisma minus become shorter and more scattered with a decrease in soil moisture. Species most abundant and vigorous in moist shrubland become progressively shorter and less dense with an increase in soil moisture, for example Hakea teretifolia, Banksia ericifolia and Banksza aspleniitfolza. The Specht classification (Specht, 1970) is not very suitable for describing the four swamp types. In the swamps in the wetter areas (vegetation tall and dense) species from the families Restionaceae and Cyperaceae combine to form a dense layer but a sparse layer of shrubs emerges above this mass (Fig. 9a). Specht’s classification using the projective foliage cover of the tallest stratum has been rejected and the swamps have been classified by the dominant tallest stratum (Beadle and Costin, 1952; Forster, Campbell, Benson and Moore, 1977). Several structural formations in the Specht classification are needed to describe fully the range of swamps with short vegetation, although this type is readily distinguishable in the field. A description of the four swamp types and of moist shrubland and conditions in which they usually occur is given below. 1. Swamp: vegetation tall and dense (Fig. 9a). Classification according to Specht (1970), tall closed-sedgeland. The water-table is near or above the surface for most of the year, as this swamp type is closely associated with creeks. The iron/organic fill is fairly free of sand and is 1-3 m deep. Gahnia sieberana is often the dominant species but it may be co-dominant with Empodisma minus. The dense G. steberana and E. minus form a thick layer from the soil up to approximately 2 m. Scattered shrubs of Leptospermum juniperinum, Baeckea linifolia and heads of G. szeberana 3-4 m tall emerge above the dense layer. Banksza robur, if present, is usually 1.5-3.5 m tall and Aotus ertcotdes is usually only 1-1.5 m tall. All shrubs provide support for the weakly twining E. minus. The fern Glezchenza dicarpa is scattered or dense and up to 1 m tall. The dense Gahniza steberana and E. minus may be interrupted by drainage lines where Baumea arthrophylla or sp. aff., E. minus and the small herb Utricularia cyanea are the only vascular plants present. 2. Swamp: vegetation dense (Fig. 9b). Classification according to Specht (1970) mid-height closed-herbfield. The water-table is less frequently above the surface than for swamps with tall Proc. Linn. Soc. N.S.W., 104 (1), (1979) 1980 R. A. BUCHANAN 87 Fig. 9. a) Swamp 21 — vegetation tall and dense. Dense Gahnia sieberana overtopped by scattered Leptospermum juniperinum. b) Swamp 9 — vegetation dense. Canopy height more even than in (a). Broad leaved shrub is Banksza robur. The white zone at the edge of the swamp is Hakea teretzfolza in flower (moist shrubland). c) Swamp 4 (valley-side arm) — vegetation short. Rocks in the foreground are part of a 4 m high cliff. There is a sharp swamp/low woodland boundary. d) Vegetation mixed. Lepidosperma flexuosum frequently forms the tallest layer and gives this swamp type a uniform appearance. Scattered Hakea teretzfolza is visible. and dense vegetation, as these swamps are associated with less permanent creeks or are at a greater distance from the main creek channel. The iron/organic fill is slightly sandier and is usually 0.5-1.5 m deep. Sand usually occurs between the iron/organic fill and the underlying rock. E. minus and Gleichenza dicarpa frequently form a dense layer from the soil surface to between 0.5-1.0 m. A second but less dense layer composed of Gahnza steberana, Baeckea linifolia, L. juniperinum and Banksia robur occurs at 1.5-2.0 m. Drainage channels, with Baumea arthrophylla or sp. aff. the commonest species, may be present. Plants from drier areas may be scattered throughout. Swamp: vegetation short (Fig. 9c). Classification according to Specht (1970), mid-height closed-herbfield/herbfield, closed-heath/open-heath. This swamp type frequently occurs on shallow soils with rock less than 1 m below the surface. Such soils provide only a small reservoir of water in dry periods Proc. Linn. Soc. N.S.W., 104 (1), (1979) 1980 88 THE LAM BERT PENINSULA and high water levels are maintained by flooding from drainage lines during wet periods and/or from water in puggy material. The iron/organic fill may be sandy and almost absent or up to 1 m deep, but it is commonly between 0.3-0.6 m deep. No dominant species occurs in this swamp type, although in individual swamps one or more dominant species may be recognized. As the species composition is so variable, this type is best recognized by the height and abundance of some of the most constant species (Table 2). Glezchenia dicarpa may be dense, in dense patches or scattered. The average height of the vegetation is commonly 0.5-1.0 m and it is usually less thick than the vegetation of the two preceding types. 4. Swamps: vegetation mixed (Fig. 9d). Classification according to Specht (1970), mid-height herbfield/open-heath. This swamp type often occurs in shallow sandy soils approximately 0.2-0.5 m deep and it frequently forms a zone between a rock shelf and moist shrubland. Swamps with mixed vegetation are subject to widely fluctuating soil moisture and to drier conditions than other swamps. The iron/organic fill may be reduced to a thin sandy skin or up to 0.3 m deep. The vegetation is a mixture of species occurring in swamps and moist shrublands. No dominant species occur in this swamp type, but Lepzdosperma flexuosum frequently forms the tallest layer between 0.75-1.0 m and gives it a characteristic and often uniform appearance. The L. flexuwosum layer is often only interrupted by a few scattered shrubs, usually Banksza ericifolia, Banksia TABLE 2 Abundance and height of species which characterize swamps with vegetation : 1) talland dense 2) dense 3) short 4) mixed, and moist shrubland. Swamps: vegetation — Moist shrubland tall and dense dense short mixed Banksia robur Abundance scattered scattered very scattered — — Height (m) 1.5-3.5 1.5-2 <1.5 Leptospermum juniperinum Abundance scattered scattered very scattered — = Height (m) 2.5-4 1.5-2 <1.5 Gahnia sieberana Abundance _ dense-scattered scattered very scattered _ = Height (m) 2-3 Wea <1.5 Empodisma minus Abundance dense- dense- scattered- very scattered very scattered scattered scattered very scattered Height (m) 1-2 0.5-1 0.25-0.75 0.25 0.25 Hakea teretifolia Abundance = _ very scattered- scattered scattered-dense scattered Height (m) <1 <1 1-2.5 Banksza ericifolia Abundance — usually absent very scattered- scattered scattered scattered Height (m) 1-2 $2°0 WD = 1O TO €T°0 (ST°0) UO lpr jePe WO Oe Sie@ seu T0> 36T'0 PD GEG Ee Dau c° 97 6°66 8°ST OWE. 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FROST 99 sampled rocks whole rock analyses were also carried out. These data were also used for comparison between rock bodies. REGIONAL GEOLOGY Fig. 1 shows the sites which provided fresh samples for this investigation. In addition, data from an area near Yeoval (32° 45’ S, 148° 40’ E), sampled by Gulson (1972), have been included as site D. Table 1 indicates the ages of the rocks used in this investigation, although no radiometric age data are available for many sites. All the granitic rocks are “massive”, and most are of the Bathurst-type association (Vallance, 1969). Similarly the extrusive rocks show evidence of only minor deformation in thin section, although they have been folded with meridional trends. The intrusive rocks have been emplaced into Ordovician to Devonian metamorphosed sedimentary and mafic extrusive rocks of the Lachlan Fold Belt (Packham, 1969). Outcrops of the Devonian granitic rocks follow the regional meridional trends, although adjacent to the Sydney Basin such trends were apparently not imposed by post-emplacement tectonic activity. The Carboniferous granitic rocks along the Basin margins cut across the trends of the older rocks. Both Devonian and Carboniferous granitic intrusive rocks have mineralogical and chemical affinities with — and thus apparent genetic relationships to — adjacent extrusive rocks, such as near Bullio and Yerranderie (localities M, N, O, Pin Fig. 1), and near Rylstone (Day, 1969) (locality C). Chappell and White (1974, 1976) recognized two types of granitic rocks in the Lachlan Fold Belt. These two types are distinguished using chemical criteria, and have been interpreted to indicate two different types of source material — I-type from igneous material and S-type from sedimentary material (Chappell and White, 1974). PETROGRAPHIC AND CHEMICAL DATA New chemical data are presented here for 18 of the localities of Table 1 and Fig. 1, although chemical data have previously been published for some of the sites. Analyses for major oxides and some trace elements are listed in Table 2. Table 3 contains new results of analyses for Th and U for 18 sites, and also summarizes published K, Th and U data for 5 sites. PETROGRAPHY Petrographic descriptions for the samples analysed in this investigation are summarized in Appendix 1. The descriptions are based on both thin section and polished section study. The adamellite from Hartley has been described in detail by Joplin (1931), whose data are supplemented by new observations here. The Gooloo granite (analysis 23 in Table 2) is a small inlier of granite exposed in Gooloo Creek and possibly also in Conjola Creek (MclIlveen, 1974; 1975). Roadworks TABLE 2 (Continued) NOTES: The locality code corresponds to Table 1 and Fig. 1. Grid localities are for the (named) 1:250,000 Map sheets. Sample numbers refer to the University of Wollongong reference collection. In some cases the specific gravity has been averaged for a locality. n.d. - not determined. Ages are given as Carboniferous (C) or Devonian (D). Major oxide analyses (XRF) were by R.H. Flood and S.E. Shaw, except analyses 7 and 8 (I.R. Plimer in Facer, 1977, table 2), and 23 (AMDEL). Trace element analyses (AAS) by A.M. Depers. a 1. R7571. Small quarry (several blocks), Dubbo 243001. 13. R7573. Drill core, 209m depth, Wollongong 321784(approx.). 2. R6619. Roadworks (several blocks), Dubbo 206988 14. R7235. Pulpit Rock member of Bindook Porphyry, natural outcrop, 3. (Anal. 3 supplied by E.R. Phillips) (locality near that for 2). Wollongong 317757. 4. R7585. Roadworks (2 blocks), Dubbo 295946. 15. R7236. Rileys Range member of Bindook Porphyry, natural outcrop, 5. R7574. Natural outcrop, Sydney 312904. Wollongong 316758. 6. R6631. Road cutting (several blocks), Bathurst 245871. 16. R7237. Natural outcrop, Wollongong 314757. 7. Facer (1977, table 2, 1 and 5) A dash indicates n.d. for one sample. 17. 7238. Natural outcrop, Wollongong 318753. 8. Facer (1977, table 2, 2 and 3) Roadworks and cutting, Bathurst 277866. 18. R7575 and R7576, Roadworks, average of two analyses, Goulburm 294696. 9. R6621. Roadworks (2 blocks), Sydney 300857. 19. R6695. Altered vein, natural outcrop, Wollongong 339690. 10. R6624. "Opera House Quarry", average of two analyses, 20. R6697A. At altered vein, natural outcrop, Wollongong 339690. Bathurst 285850. 21. R6697B. 10cm fram altered vein, natural outcrop, Wollongong 339690. 11. 6626 and R7578. Roadworks, average of two analyses, 22. R6696. 3m from altered vein, natural outcrop, Wollongong 339690. Sydney 315855. 23. R7581. Roadworks (2 blocks), Ulladulla 344651. 12. R6620. Roadworks, Bathurst 213846. 24. R6472. Roadworks (several blocks), Ulladulla 311564. Proc. Linn. Soc. N.S.W., 104 (2), (1979) 1980 sask|euy uL SaunBLy quediy.ubLs jo ADuaqstsuod uLequLew 0 Auessadau sem HuLpunou siu]) JOU PLP SUOUdd DALZELNWND zeYUg |uNSus Oj UayYe} SEM auPd “pe suiskjeue “2 a1 qe (4 TOW 07 69W Saskjeue “] aged “e/6l) “Le 3a UlssL4N "(229W ‘STOW “89W 0} GOW saskieue “] a1qey “g/6T) “Le 38 UlssL4N *(€9W 07 TOW Sasfkjeue “T aged “g/6T) “Le Je Ulsyt4y "Ez siskjeue “2 ajqel *22 pue [2 sashjeue *2 alqey "el sishjeue “2 alqel UU Wee Sok COrg LG'S GENE OLY) Qi MEG OU WP LOS BUG. SL EUG HEAT GENERATION 9L°¢2 ¥9L°? ¥9L°? 91°22 G)G WY SG BOG “GES 100 EA OSs OG wre WE EG Stew ew Wore We GEE Le EW? 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OL? See? 65°2 ET°2? L6°T ell/mn (11e°d SE uoLqenba ‘9/61 Sydeqhy) uoLqeuauab zeaH /8°T 96°2 T0°E 8BLl°2 0S°2 eld LL°e? Te°e 99°2 6T°2 20°2 oll/mn lv°y 80°2L O¢°L S9°9 86°S 80°S €9°9 €5°¢ LE°9 He°S E8°D 99S wo/LP2.7_O1 (2d ‘uotyenba ‘c/6T *°[e Ja 4ayung) uoLlqeuauab yeay SIG OF2G “We Gusy-G us OL°2 G9°2 ¥L9°2 $S°2 89°C 99° eS Ole Comme Oat esenal Gpeteen Vice Vato inet Ss eS GSS I re Sd (wdd) A 6°€l 9°61 G*6l S°ST I°ST 2°61 BEL T°I2 HST O°8T HST 2°HT (wdd) yt LOSS S9eI= 00Re —t9s let. S520 post —98ad =c9ne ces 00sec 9ne = 88a (%)x ejep Leoiwayy D) (B)9 G 9 9 9) aby z| 3 ( 2) q Vv AzL [e907 Proc. LINN. Soc. N.S.W., 104 (2), (1979) 1980 R. A. FACER, A.C. HUTTON AND D.J. FROST 101 at Gooloo Creek indicate an unconformable relationship between the Gooloo granite and the Sydney Basin. The name Bundundah granite is used here for the “Bundundah Porphyritic Microgranite” referred to by MclIlveen (1975, p. 6) and based on mapping of granite in the Bundundah, Yarramunmun, Danjera and Yalwal Creeks area (Towey, 1965; Wall, 1965; Frost, 1977). Like the Gooloo granite the Bundundah granite is overlain by Sydney Basin rocks, but the Devonian sedimentary and volcanic rocks into which it is emplaced are also exposed. CHEMISTRY The chemical data in Table 2 indicate that all the rocks analysed are silica-rich, no granites (sensu lato) containing less than about 65% SiO,. The tonalite of analysis 24 is marginally less siliceous than the other rocks, but this analysis is similar to those of Griffin et al. (1978, table 1) for the Moruya Tonalite. Allowing for slightly different sample-sites, degree of weathering and techniques, analysis 11 is similar to analyses IX and X of Joplin (1931, p.53). The Carboniferous rocks are generally more siliceous than the Devonian samples, but detailed comparisons would require more accurate age data. As indicated in Table 1 some sites have not been dated by radiometric techniques — in which case their most likely age is indicated. Chemical analyses for the Bundundah granite of site R (Table 2, analyses 19 to 22; with petrographic descriptions in Appendix 1) indicate that the distribution of major oxides in the two phases of the granite differs from that in the hydrothermally altered zone in Fe content and oxidation state, Na,O and Al,O;. Co, Cu, Cd and Pb increase markedly towards the altered zone. In addition, Th (23.1 ppm) and U (6.3 ppm) are high in the vein (cf. Table 3, entry R for Th and U content away from the vein). These increases apparently indicate that hydrothermal solutions have introduced trace metals, including Th and U, and hence only analyses 21 and 22 (Table 2) have been used for heat-generation calculations. HEAT GENERATION An indication of the generation of heat by the heat- producing elements in rocks is provided by the equation (after Bunker et al., 1975) : Heat Generation = [ (0.27K% + 0.20Th ppm + 0.73U ppm) ee x 0.418 uW/m? (1) (1 heat-generation unit (HGU)) is 107? cal/cm*sec = 0.418 ~W/m!). Equation 1 is similar to that given by Rybach (1976, equation 3, p.311), who also gave details of the decay processes giving rise to the heat generation. Isotopic equilibrium is assumed when using such an equation. Values of heat generation obtained using equation 1 (Table 3) average 1.028 times those determined using Rybach’s (1976) equation. However, as equation 1 follows the decay data in Rogers and Adams (19696, p.92-B-2), and as much published heat generation information has been published using these decay data comparison will be facilitated by adopting them. Discussion here will be based on determinations using equation 1. Some of the determinations in Table 3 are for rocks which outcrop beyond the present margin of the basin, but near outliers of Permian sedimentary rocks (such as Wuuluman, site b, cf. Dulhunty, 1964) — or as major rock bodies which may have a significant influence on basement heat generation (such as Carcoar). Table 3 also contains chemical data for sites D, K, T, U and V, for which no calculations of heat generation were Proc. Linn. Soc. N.S.W., 104 (2), (1979) 1980 102 HEAT GENERATION published with the data. The information in Table 3 for the Durandal Adamellite is modified from Facer (1977) using additional data. Bunker et al. (1975) have presented heat-generation data for the Bathurst batholith (although the last entry in their table 2-2 should be located at (33° 24’ S, 149° 20’ E), one site in schist from Apsley (33° 34’ S, 149° 34’ E) ; and one site from the Moruya batholith. The data of Bunker et al. (1975) have been converted into heat-generation units using S.G.’s of 2.65 (based on measurements of other samples) for the Bathurst batholith and 2.60 for Apsley schist, and by converting data from Sass et al. (1976, p.13) for the Moruya batholith. These recalculated data are: Bathurst batholith — 3.02 u.W/m?; Apsley schist — 2.44 4.W/m?; and Moruya batholith — 1.45 wW/m’. Heat-generation values determined by Bunker et al. (1975), recalculated here, for the Bathurst batholith agree well with those of the present investigation in Table 4. Similarly, for the Moruya batholith the mean (Table 4) agrees with that of Bunker et al. (1975). Heat generation in the Nelligen Granodiorite (entry T in Table 3) is approximately twice that in the minor intrusions (Table 3, U) adjacent to the main mass of the Moruya Tonalite and the tonalite (Table 3, V and W). Entry U of Table 3 includes data for a “gabbroic diorite” phase of the Mogendoura Granodiorite (Griffin et al., 1978, p.238 and table 1), although exclusion of this mafic phase would only raise the value of the heat generation to 1.57 uW/m? — still only about half that for the Nelligen Granodiorite. The mean heat generation for all 22 values based on equation 1 (Table 4) is 2.31 TABLE 4 Mean heat generation in siliceous igneous rocks in the basement to the Sydney Basin Igneous rocks mass Number Heat generation Entries in Table 3 or group of rocks of analyses uW/m> Mean s.d. Bathurst batholith 6 2.77 0.40 F to K Carboniferous rocks 12 AS O27 A to C, E to K, R and § Carboniferous rocks and 13 2.53 0.46 A toc, EtoK, RtoT Nelligen Granodiorite Moruya batholith 2* Ase U to W Devonian rocks 9 1.98 0.39 D, LtoQ, U tow Devonian rocks and 10* 2.07 0.46 D, L toQ, T tow Nelligen Granodiorite All rocks 22% Aodlk OoSil All All rocks, except 17* 2.13 0.44 A to E, L tow Bathurst batholith Note: The entries marked * include a mean value for V and W of 1.46 uW/m> Proc. Linn. Soc. N.S.W., 104 (2), (1979) 1980 R. A. FACER, A.C. HUTTON AND D.J. FROST 103 HW/m? (s.d. = 0.51 wW/m?). For the 17 values (V and W combined), after omission of entries F to K, the mean is noticeably lower than the mean for the Bathurst batholith (Table 4), although the two values (2.77 uW/m? s.d. = 0.40 uW/m? and 2.13 h.W/m?, s.d. =0.44 ~.W/m?) are within 2 s.d.’s. DISCUSSION The siliceous igneous rocks forming part (25%) of the basement to the Sydney Basin (Table 1) range from Devonian to Carboniferous in age, with the younger rocks outcropping more to the north and the older (Devonian) rocks more to the south of the Bathurst batholith (Fig. 1). Part of the Yeoval batholith may be as old as Late Silurian (Gulson and Bofinger, 1972). Table 2 indicates that only three of the rocks for which new chemical data are presented contain less than 65% SiO. No distinctive chemical differences were noted between intrusive and extrusive rocks. The Carboniferous rocks, especially those of the Bathurst batholith, tend to be more siliceous and potassic than the Devonian rocks. Similarly the Carboniferous intrusions plot slightly towards the A apex on AFM diagrams. The granites (sensu lato) analysed here fit into the I-type classification of Chappell and White (1974) using the first three criteria of their table. However, analysis 8 of Table 2 for the Durandal Adamellite may represent an S-type rock, notwithstanding that analysis 7 fits the I-type classification. There are no apparent mineralogical differences between these adamellite samples sufficient to explain the chemical differences. Aplites and contact adamellite from this site yield an initial ®87Sr/*°Sr ratio of 0.7051 + 0.0016 (Facer, 1976) which fits one I-type criterion of Chappell and White (1974, p.173). Entry 8 of Table 2 is an average of analyses of different samples by two analysts (cf. Facer, 1977, Table 2), yet has the apparent S- type characteristic of Mol[Al,03;/(Na,.O + K,O0 + CaO)] = 1.28. One possible explanation is that, by coincidence, the analyses 2 and 3 in table 2 of Facer (1977) each contain minor sedimentary xenolithic material which was not observed in the hand specimen blocks prior to crushing, and which was not intersected by thin (or polished) sections. The Durandal Adamellite does contain xenoliths, although those of sedimentary origin are at least subordinate, most having an apparent igneous origin (cf. Mackay, 1964; Facer, 1977). These xenoliths comprise both igneous country rocks (Mackay, 1964) and fragments of a more granitic nature which could have been stoped from the early-cooled parts of the intrusions — and igneous inclusions, some of which may have been assimilated, would tend to suggest an I-type origin. Th and U contents are generally lower in the older rocks (Table 3). The other trace elements, despite variations, show no strong trends. The SiO,, K,0, Th and U (and to a lesser extent V, Co, Ni and Cu) trends shown by the new analyses and those of Griffin et al. (1978, table 1) indicate that the Nelligen Granodiorite may be Carboniferous, and hence not part of the Moruya batholithic complex (cf. McIlveen, 1974; 1975, p.6). Griffin et al. (1978, p.244) used chemical data to suggest (qualitatively) a slightly different source for the Nelligen Granodiorite from that for the main Moruya batholith. Several cluster analysis dendrograms were calculated and indicate that results for the Nelligen Granodiorite tend to cluster with the Carboniferous rocks of this investigation. However, lack of complete discrimination between Devonian and Carboniferous rocks precluded definite inclusion of the Nelligen Granodiorite in the Carboniferous group. The Th and U contents of the Carboniferous rocks (Table 3) are generally at or above the levels listed by Clark et al. (1966, figs 24-6 to 24-9) as means and medians for granodiorites (Th 9.3 ppm, 9.0 ppm respectively; U 2.6 ppm, 2.3 ppm Proc. Linn. Soc. N.S.W., 104 (2), (1979) 1980 104 HEAT GENERATION respectively) and siliceous igneous rocks (Th 20 ppm, 16 ppm respectively; U 4.7 ppm, 3.9 ppm respectively). For the older rocks of this investigation the Th and U contents are closer to, or below, these averages. However differences between the present calculated means (Table 4) and those of Clark e¢ al. (1966) are not marked. The overall Th: U ratio (with localities V and W combined as one locality) is 4.52 (s.d. = 1.08), not significantly different from the value of 4.0 suggested in fig. 24-13 of Clark et al. (1966), and very close to the mean for granitic rocks of 4.63 (s.d. = 0.85) in table 90-E-1 of Rogers and Adams (1969a). For the Bathurst batholith this ratio is 3.85 (s.d. = 0.38). For the Bundundah granite the Th: U ratio ranges from 3.67 (for the vein) to 5.50 (10 cm from the vein), with an overall mean of 4.50 (s.d. = 0.85). As this ratio for other samples in Table 3 extends outside the range for the Bundundah granite the introduction of Th and U along the vein does not influence the ratio. Reflecting the overall K, Th and U content, the heat generation in the Carboniferous rocks, especially in the Bathurst batholith, is higher than in the older rocks. This heat generation is at or above an “average” value for granitic or siliceous igneous rocks based on the data of Clark et al. (1966). Although specific isotopes are responsible for production of heat, the heat generation values are based on total K, Th and U content (equation 1). The older rocks do not generate less heat than the Carboniferous rocks only because of greater time for radioactive decay. Disequilibrium in the isotopes of K, Th and U could introduce errors in heat- generation studies, for example in analysis of small samples. Table 4 summarizes the heat-generation data from Table 3, arranged in various groupings — which indicate higher heat generation by the Carboniferous rocks. Because of the possible uncertainty in the age of the Nelligen Granodiorite, the Nelligen data are included in both Carboniferous and Devonian groups. Inclusion of the Nelligen data in the Carboniferous mean makes little change in that mean. Heat generation by the Nelligen Granodiorite is approximately twice that of the Moruya batholith. Although variation in uranium content strongly influences the magnitude of heat generation (and can be redistributed by weathering) all three elements K, Th and U in the Nelligen Granodiorite are closer in content to the Carboniferous rocks than the Devonian rocks. The further work planned on the distribution of K, Th and U may help in the interpretation of the possibly anomalous place of the Nelligen Granodiorite in the sequence of Devonian and Carboniferous intrusions. The narrow range in S.G.’s of the rocks of this investigation (Table 3) precludes determination of accurate relationships between heat generation, S.G. and seismic velocity (cf. Rybach, 1976). The possible relationship between (high) heat flow and (low) seismic velocity for the Lachlan Fold Belt, discussed by White et al. (1974, p.161), may partly reflect the relatively high heat generation in at least some of the siliceous igneous rocks which make up approximately 25% of the fold belt. As yet heat-generation data for the other rocks of the Lachlan Fold Belt are inadequate for discussion of the relationship between heat generation and seismic velocity. The P velocity of 6.52 km/sec reported by Doyle et al. (1966) for the layer under the southern and southwestern Sydney Basin corresponds to a low heat generation of approximately 0.8 ~wW/m? using Rybach’s (1976) fig. 2. Thus the relatively “cool” Devonian igneous rocks of this basement may have been emplaced into rocks of even lower heat generation, although the “wedge of a few kilometres of 6 km/sec. material” (Doyle et al., 1966, p. 355) immediately under the basin rocks would correspond to a heat generation of approximately 1.2 »W/m:. Comparatively high heat generation in some basement siliceous igneous rocks may contribute to high heat flow (relative to eastern Australia) within the southern Proc. Linn. Soc. N.S.W., 104 (2), (1979) 1980 R. A. FACER, A.C. HUTTON AND D.J. FROST 105 portion (but not the extreme southernmost area) of the Sydney Basin (Munroe et al., 1975; Sass et al., 1976, p.15). However, the lack of heat-flow data from levels below the Triassic rocks of the basin, and the low heat-flow value from near Moruya (Sass et al., 1976), make a detailed thermal properties investigation an interesting problem for research of the present type. The Moruya heat flow may be low partly because the Moruya batholith generates low amounts of heat relative to other granitic rocks of the basement. Although such a programme has commenced, more data are required. It is apparent that a careful study of variation of heat generation in both basement rocks and the Permian basin rocks needs to be integrated with other criteria of thermal history — such as “coal rank’ measurements, even on accessory carbonaceous detritus in the basin rocks. Heat flow, which is partly influenced by heat generation, has an important influence on coal, and may be a significant factor in coal rank variation in the Sydney Basin. The heat which has influenced and still may influence the coal rank was, and is, generated by the basement rocks, as well as rocks below the Illawarra Coal Measures (and within the coal-bearing horizons) . The rocks below the coal measures are igneous and sedimentary (including volcanoclastic) rocks. As these igneous rocks are potassium-rich they may be significant contributors to the heat generation — but preliminary data indicate that many of the sedimentary rocks below and within the coal measures also generate more heat than the Moruya batholith. A full investigation of the basement rocks and their distribution (using, for example, gravity surveying) is required. This would help in establishing the relative contribution of basement and basal rocks to the thermal history of the coal within the basin. Such an assessment should assist in evaluating the role of the younger (Jurassic and younger) igneous rocks in and on the basin to the heat flow of the basin. Towards the centre (and northern part) of the Sydney Basin the Carboniferous volcanic rocks may be important generators of heat. CONCLUSIONS Analyses of siliceous igneous rocks making up approximately 25% of the basement along the northwestern, western and southern margins of the Sydney Basin have revealed chemical differences between Carboniferous and Devonian rocks. Carboniferous rocks, which tend to outcrop in the northern portion of the Lachlan Fold Belt sampled in this investigation, contain higher proportions of SiO, and K,O than the Devonian rocks. Values for Th and U are generally higher in the Carboniferous rocks, being at or above means in tabulations of world-wide data. On the basis of available chemical data the Nelligen Granodiorite shows more similarities to the Carboniferous granitic rocks than to the Devonian Moruya batholith. The Carboniferous and Devonian granitic intrusions are I-type, indicating igneous source material. Because of the higher proportions of the heat-producing elements K, Th and U, the Carboniferous rocks generate more heat (cf. equation 1) than the Devonian rocks. Values of heat generation have been determined for 18 sites, based on new chemical data. When combined with published chemical data for 5 sites, heat generations at 22 sites (the Moruya batholith is in both groups) are available. The overall mean value for heat generation at these 22 sites is 2.31 wW/m? (s.d. = 0.51 wW/m’). For the Carboniferous rocks (Nelligen Granodiorite included) the mean heat generation is 2.53 uW/m? (s.d. = 0.46 h.W/m?, n = 13), whereas for the Devonian rocks, with the Nelligen Granodiorite (2.83 u~W/m?) excluded, the mean heat generation is 1.98 HW/m? (s.d. = 0.39 WW/m?,n = 9). The relatively high heat generation in the Carboniferous rocks along the basement margins of the Sydney Basin could influence seismic velocity through the Proc. Linn. Soc. N.S.W., 104 (2), (1979) 1980 106 HEAT GENERATION upper crust. It also apparently influences heat flow through the Sydney Basin, which is high for this portion of eastern Australia, and could thus affect the coal rank within the basin. The pre-Carboniferous intrusions which outcrop near or south of 35°S generate less heat than the Carboniferous rocks — and are south of the relatively high heat flow area and coal rank area between Wollongong and Sydney. ACKNOWLEDGEMENTS This investigation was encouraged by E. R. Phillips. P. F. Carr, S. Holland, B. G. Jones and P. C. Mackenzie each collected one of the samples. B. E. Chenhall, and J. W. Pemberton made computer programs available. P. F. Carr, B. E. Chenhall and A. J. Wright read the manuscript. All this assistance is gratefully acknowledged, as is that of P. Kolbe and J. H. Sass in clarifying the location of a sample from Vittoria (in a satellite of the Bathurst batholith) studied by Bunker et al. (1975). Sample M was obtained from the N.S.W. Department of Mines core library. Financial assistance through University of Wollongong Special Researrh Grants 17/070/92 and 16/164/02 is especially acknowledged. References BRANAGAN, D. F., HERBERT, C., and LANGFORD-SMITH, T., 1976. — An outline of the geology and geomorphology of the Sydney Basin. Sydney: Dept of Geology & Geophysics, Univ. of Sydney (for 25th Internat. geol. Congr.). BRUNKER, R. L., and Rosz, G., 1969. — Sydney Basin 1:500,000 Geological Sheet (Special). Geol. Surv. N.S.W., Sydney. BunkKER, C. M., Busu, C. A., Munrok, R. J., and Sass, J. H., 1975. — Abundances of uranium, thorium, and potassium for some Australian crystalline rocks. U.S. geol Surv. Open-file Rept, 75-363: 39 pp. CHAPPELL, B. W., and WuitTeE, A.J. R., 1974. — Two contrasting granite types. Pacific Geol., 8: 173-4. ——, and ——, 1976. — Plutonic rocks of the Lachlan mobile zone. 25th Internat. geol. Cong., Field Exc. Guide 13C: 40 pp. CiarK, S.P., PETERMAN, Z. E., and HetEr, K. S., 1966. — Section 24. Abundances of uranium, thorium and potassium. Jn Clark, S. P. (ed.), Handbook of physical constants. Mem. geol. Soc. Amer. 97: 521-41. Day, J. F., 1969. — Carboniferous system. Jn Packham, G. H. (ed.), The geology of New South Wales. J. geol. Soc. Aust., 16: 178-9. DoyLe, H. A., UNDERWOOD, R., and Po.ak, E. J., 1966. — Seismic velocities from explosions off the central coast of New South Wales. J. geol. Soc. Aust., 13: 355-72. DuLHuntTy, J. A., 1964. — Our Permian heritage in central eastern New South Wales. J. Proc. R. Soc. N.S.W., 97: 145-55. EVERNDEN, J. F., and RICHARDS, J. R., 1962. — Potassium-argon ages in eastern Australia. J. geol. Soc. Aust., 9: 1-49. Facer, R. A., 1976. — Palaeomagnetism, radiometric age and geochemistry of an adamellite at Yetholme, N.S.W./J. geol. Soc. Aust., 23: 243-8. ——, 1977. — Geochemistry and heat generation in the Durandal Adamellite at Yetholme, New South Wales. Proc. Linn. Soc. N.S.W., 102: 26-35. ——, 1978. — New and recalculated radiometric data supporting a Carboniferous age for the emplacement of the Bathurst batholith, New South Wales. J. geol. Soc. Aust., 25: 429-32. ——, Cook, A. C., and Beck, A. E., 1980. — Thermal properties and coal rank in rocks of the southern Sydney Basin, New South Wales. (Prepared for submission) . FELTON, E. A., 1974. — Goulburn 1:250,000 Metallogenic Map, Sheet SI 55-12. Geol. Surv. N.S.W., Sydney. Frost, D. J., 1977. — The geology of an area east of Danjera Dam. Wollongong: University of Wollongong, B.Sc. (Hons) thesis, unpubl. GRIFFIN, T. J., WHITE, A. J. R., and CHAPPELL, B. W., 1978. — The Moruya batholith and geochemical contrasts between the Moruya and Jindabyne suites. J. geol. Soc. Aust., 25: 235-47. GuLson, B. L., 1972. — The high-K diorites and associated rocks of the Yeoval diorite complex, N.S.W. Contr. Mineral. Petrol., 35: 173-92. , and BoFINcER, V. M., 1972. — Time differences within a calc-alkaline association. Contr. Mineral. Petrol., 36: 19-26. Proc. LINN. Soc. N.S.W., 104 (2), (1979) 1980 R. A. FACER, A.C. HUTTON AND D.J. FROST 107 Hutton, A. C., 1977. — Geology of an area south-east of Bullio, New South Wales. Wollongong: University of Wollongong, B.Sc. (Hons) thesis, unpubl. Jones, J. G., McPui, J., and Roots, W. D., 1977. — Devonian volcano at Yerranderie. Search, 8: 242-4. Joptin, G. A., 1931. — Petrology of the Hartley district. I. The plutonic and associated rocks. Proc. Linn. Soc. N.S.W., 56: 16-59. KANTSLER, A. J., 1973. — The geology of an area near Bungonia, New South Wales. Wollongong: Wollongong University College, B.Sc. (Hons) thesis, unpubl. Mackay, R. M., 1964. — The Yetholme granite. A study in the genesis of potash feldspar megacrysts. Sydney: University of Sydney, Ph.D. thesis, unpubl. Matson, C.R., 1974. — Dubbo 1:250,000 Metallogenic Map, Sheet SI 55-4, Geol. Surv. N.S.W., Sydney. McILVEEN, G. R., 1974. — Ulladulla 1: 250,000 Metallogenic Map, Sheet SI 56-13. Geol. Surv. N.S.W., Sydney. ——, 1975. — Part 2. A metallogenic study of the Ulladulla 1: 250,000 sheet. Geol. Surv. N.S.W., Sydney: 16 pp. MunroE, R. J., Sass, J. H., MiLBuRN, G. T., JAEGER, J. C., and TamMemacl, H. Y., 1975. — Basic data for some recent Australian heat-flow measurements. U.S. geol. Surv. Open File Rept, 75-567: 90 pp. PackHaM, G. H. (ed.), 1969. — Geology of New South Wales. J. geol. Soc. Aust., 16: 1-654. PHILLips, E. R., and Carr, G. R., 1973. — Myrmekite associated with alkali feldspar megacrysts in felsic rocks from New South Wales. Lzthos, 6: 245-60. Pottock, E. N., 1977. — The spectrophotometric determination of uranium and thorium in ores. Anal. Chimica, 88: 399-401. Ruopes, J. M., 1969. — The application of cluster and discriminatory analysis in mapping granite intrusions. Lithos, 2: 223-37. Rocers, J. J. W., and Apams, J. A.S., 1969a. — 90-E. Abundances (thorium) in common igneous rocks. and 90-N. Behavior in metamorphic reactions. In Wedepohl;, K. H. (ed.), Handbook of Geochemistry, 11-4: 90-E-1 — 90-E-12 and 90-N-1. Berlin: Springer-Verlag. , and , 19696. — 92-B. (Uranium) Isotopes in nature; heat production in common rocks. and 92-N. Behavior in metamorphic reactions. In Wedepohl, K. H. (ed.), Handbook of Geochemistry, II-4: 92-B-1 — 92-B-3 and 92-N-1. Berlin: Springer-Verlag. RyBAcH, L., 1976. — Radioactive heat production in rocks and its relation to other petrophysical parameters. Pageoph, 114: 309-17. Sass, J. H., JAEGER, J. C., and Munrog, R. J., 1976. — Heat flow and near-surface radioactivity in the Australian continental crust. U.S. geol. Surv. Open-File rept, 76-250: 91 pp. STEIGER, R. H., and JaGeER, E., 1977. — Subcommission on Geochronology: convention on the use of decay constants in geo- and cosmochronology. Earth Planet. Sci. Lett., 36: 359-62. Towey, P. E., 1965. — The geology of Yalwal Creek, Bundundah Creek and Grassy Gully. Sydney: University of Sydney, B.Sc. thesis, unpubl. VALLANCE, T. G., 1969. — Southern and central highlands fold belt. Plutonic and metamorphic rocks. In Packham, G. H. (ed.), Geology of New South Wales. J. geol. Soc. Aust., 16: 180-200. WALL, V.J., 1965. — The geology of Yalwal south. Sydney: University of Sydney, B.Sc. thesis, unpubl. White, A.J. R., CHAPPELL, B. W., and CLEARY, J. R., 1974. — Geologic setting and emplacement of some Australian Paleozoic batholiths and implications for intrusive mechanisms. Pacific Geol., 8: 159-71. APPENDIX I PETROGRAPHY OF THE SAMPLES ANALYSED Samples were collected from localities A to C, EtoJ, LtoS, and W (Fig. 1). (Only the designating letter is used in the following description.) Table 3 contains chemical data, and references to published petrographic descriptions. The petrographic descriptions are generally restricted to the samples analysed, except for the rocks near Bullio (N,O,P) (Hutton, 1977) and Yalwal (R) (Frost, 1977) where more general petrographic descriptions are given based on petrographic studies of several thin and polished sections. References in this Appendix are included in the list following the text of this paper. A. Sample R7577 is a porphyritic granodiorite from the Gulgong Granite (Matson, 1974), with feldspar phenocrysts up to 15 mm set in a groundmass with an average grainsize of 2 mm. The composition is quartz (29%); perthitic potash feldspar (16%); and albite-rimmed plagioclase (44%), with rim myrmekite; biotite (6%), (a = pale brown, Bf = y = dark brown, with apatite and zircon inclusions) ; and accessory minerals (2%) — magnetite and sphene. Alteration minerals include clinozoisite, chlorite, epidote and “sericite”. B. The Wuuluman adamellite has been described by Phillips and Carr (1973), being distinctive in containing tabular potash feldspar megacrysts up to 75 mm in length, some of whict exhibit rapakivi textures. (The analytical data correspond to the petrography described by Phillips and Carr, 1973.) Proc. Linn. Soc. N.S.W., 104 (2), (1979) 1980 108 HEAT GENERATION C. Day (1969) has described the tuffaceous rocks which outcrop north and northwest of Rylstone. Sample 7585 is a fawn tuffaceous dacite — close to rhyodacite — with feldspar, quartz and lithic fragments up to 3 mm set in a fine-grained groundmass of partly devitrified glass (58%). As noted by Day (1969, p.179), the 5% clear quartz grains are fractured, and embayed, and some small grains have small acicular “overgrowths”. The feldspar crystals are also fractured, and consist of both potash feldspar, 10% (sanidine; Day, 1969) and plagioclase, 21% (altered, possibly about An;,), occurring both as large grains and in the groundmass. Minor biotite (a = yellow brown, 8 = y = dark brownish green), hornblende (a = brown, fB = brown green, y = dark green, with apatite inclusions); magnetite, and zircon are also present. Alteration products include “sericite”, hematite, chlorite and calcite. The lithic fragments comprise a sufficiently small proportion that they probably do not significantly influence the chemical analysis, especially as they appear to be similar in rock type to the main rock. E. The porphyritic rhyolite from this site consists of quartz and feldspar grains (3 to 4 mm across) set in a grey-green aphanitic groundmass and has been termed the “Huntingdale Porphyry” (S. Holland, pers. comm., 1977). Clear, fractured, embayed quartz grains (16%) contain inclusions of rutile and tourmaline. The feldspar grains include cloudy perthitic potash feldspar (19%) and strongly sericitized plagioclase (5%). Magnetite comprises less than 1%. The (59%) groundmass, which may include some devitrified glass (although difficult to identify definitely) , contains quartz and feldspars. In addition to “sericite” and clay minerals, alteration has produced epidote and calcite. F to K. These sites are from various granitic phases of the Bathurst batholith. Vallance (1969) has presented a summary of descriptions of rocks of this batholith, which is a composite suite of massive (undeformed) intrusions ranging from granites to relatively minor mafic phases (the latter not having been sampled in this study). At Dunkeld (F) a grey, even-grained (3 mm) adamellite outcrops, consisting of 25% quartz with rutile inclusions; 25% perthitic potash feldspar and 40% plagioclase (An3,), with rim and bulbous myrmekite; 5% strongly pleochroic biotite (@ = brown tostraw, f = y = dark brown) with dark haloes around zircon inclusions; 4% strongly pleochroic hornblende (a = pale brown, B = green, y = dark greenish brown) ; and 1% accessory minerals (magnetite, spinel, apatite). Alteration products include “sericite”, epidote and chlorite. Descriptions of the Durandal Adamellite (G) have been given by Mackay (1964) and Facer (1977), and of the granodiorite at Hartley (K) by Rhodes (1969). Joplin (1931, pp.23-27) has described in detail the granite at Hartley (J). The porphyritic adamellite from Sodwalls (H) consists of 24% quartz, with inclusions of rutile and tourmaline; 46% orthoclase (tabular crystals up to 6 mm in length), with ribbon perthite, and altered to “sericite”; 27% plagioclase (An3, to An,2), altered to “sericite”, epidote and minor calcite; 1% biotite (a = yellow brown, f = y = dark greenish brown) with inclusions of zircon; and 1% horn- blende(a = greenish brown, f = brown, y = dark brown); and approximately 1% apatite and magnetite. Both biotite and hornblende are partly chloritized. The Carlwood granite (I) is pink, coarse and even-grained (average 4 mm). Quartz comprises 36% and is free from inclusions. Perthitic orthoclase comprises 42%, and albite-rimmed plagioclase 19%, with rim myrmekite. Minor biotite(@ = pale brown, f = y = dark brown), brown to green hornblende and magnetite are also present. Alteration minerals include “sericite”, epidote and chlorite. L. “The Carcoar Granite appears to be discordant” (Vallance, 1969, p.194) with a range in composition which includes granite and quartz diorite. Other Devonian granitic intrusions in the Lachlan Fold Belt are concordant. The sample analysed is a grey, medium-grained (3 mm) granodiorite, and contains 20% clear quartz, 20% perthitic potash feldspar and 45% plagioclase (Anjo to An,;), which may be zoned with sericitized cores. Biotite comprises 10% (a = yellow brown, B = y = reddish brown) and twinned hornblende 5% (a = pale brown, ff = greenish brown, y. = dark green). Magnetite is accessory. Alteration minerals include “‘sericite” and epidote, and localized clinozoisite and prehnite. M. The rhyodacite from Yerranderie is strongly altered, with little of the original phenocrysts remaining. It was sampled from drill core, but field relationships are unknown — except that it appears similar to the Bindook Porphyry (cf. Vallance, 1969, p.194). The feldspar phenocrysts are sericitized, and the mafic phenocrysts altered to chlorite. Quartz is abundant. N to P. The Bindook Porphyry (N) is dacitic to rhyodacitic, and has been subdivided into two members (Hutton, 1977). It contains phenocrysts of embayed quartz (8%) and plagioclase in a fine-grained groundmass of quartz and orthoclase, with minor biotite and hornblende. The plagioclase phenocrysts (26%) are zoned, with cores of An;, to Ans, and rims of Anz. to An,,. Hornblende (a = pale green, B = green, y = dark green to brown) phenocrysts comprise 4%; and slightly pleochroic hypersthene, clinopyroxene and biotite are also present. Magnetite, zircon and topaz are accessories. Alteration minerals include “sericite” and epidote in plagioclase cores, and chlorite, clinozoisite and prehnite. The mineralogy of the granodiorite from locality O is similar to that of the rocks from locality N, except that the plagioclase is more calcic (cores of An3g to An,;) and hypersthene is absent. This granodiorite is Proc. LINN. Soc. N.S.W., 104 (2), (1979) 1980 R. A. FACER, A.C. HUTTON AND D.J. FROST 109 non-porphyritic, with grains averaging 2 to 3 mm across. The granodiorite of locality P is distinct from that of locality O, being coarse-grained, with elongate hornblende phenocrysts up to 15 mm in length set in an even-grained pale grey groundmass. Quartz comprises 13% of the rock, orthoclase 19% and plagioclase (An;; to Any; cores, Anzo rims) 40% — with minor myrmekite. The hornblende (a = pale green, B = green, y = dark green to brown) comprises 20% and biotite (a = pale brown, 8 = brown, y = dark brown) comprises 5%. Accessory minerals include magnetite, zircon and apatite. Alteration includes sericitization of plagioclase, especially cores, and chloritization. Relationships between the rocks at localities N to P will be discussed in a separate presentation by Hutton (in prep.). Q. The granodiorite at Bungonia (Marulan Granite) has been described by Kantsler (1973), and is the subject of a separate study by P. F. Carr et al. (in prep.). Two samples were analysed in this investigation, each being even- and medium-grained (2 to 3mm), and each containing quartz, potash feldspar, plagioclase and minor mafic phases. Magnetite is the main opaque phase, and is accompanied by minor hematite and ilmenite. R. Four samples from the small outcrop of the Bundundah granite were analysed, including a fracture zone of hydrothermal alteration about 0.5 m wide. The granite has two phases — an outer pale fawn porphyritic microgranite, (average grainsize 1 mm) and an inner pink porphyritic granite (average grainsize 4 mm) which contains xenoliths of the fine-grained phase. Aplite dykes and hydrothermally altered fracture zones are common, being subparallel to the outer contact of the porphyritic microgranite. These features indicate that emplacement of these two granitic phases was not quite synchronous. The fine-grained phase contains phenocrysts, up to 10 mm, of quartz in an hypidiomorphic granular groundmass of quartz, microcline, plagioclase and minor biotite, apatite, sphene and hematite after magnetite. Lack of quartz phenocrysts is the only major difference between the porphyritic granite and the fine-grained phase. The overall approximate proportions are quartz: 34%, potash feldspar: 42%, plagioclase: 16%, biotite: 4%, and accessory minerals: 5%. In the alteration zone (centred on a sulphide-rich vein) the quartz and biotite contents remain the same, but most of the feldspar is altered to sericitic micas and epidote, and pyrite and chalcopyrite comprise 5%. Although the alteration vein has sharp contacts, the host granite contains sulphides within 5 cm of the vein. S. The small inliers of granite in Gooloo and Conjola Creeks are exposed below the Permian Conjoia Sub- group of the Sydney Basin. In Gooloo Creek the granite is even- and coarse-grained (5 mm), and, although moderately weathered, is fresher than the outcrop in Conjola Creek (S. H. Hickey, pers. comm.) . Quartz comprises 4% of the granite. The perthitic potash feldspar is heavily clouded by sericitic alteration, and comprises 62%. Plagioclase (An,,) is also altered — to “sericite”, clay and calcite — and comprises 27%. Biotite (a = yellow, Bi = y = dark brown) and weakly pleochroic hornblende (brown and green) each comprise 3%. Magnetite and sphene are very minor accessories. W. One of the phases of the Moruya batholith is the tonalite analysed here. Sample R6472 is a grey, even- and medium-grained (2.5 mm) tonalite which contains xenoliths, although xenolithic material was avoided during preparation for analysis. Quartz comprises 11% of the tonalite and contains rutile inclusions. Potash feldspar (21%) and plagioclase — An3;, — (53%) are the main constituents, with 9% zircon-bearing biotite (@ = yellow brown, B = brown green, y = dark green brown) and 5% twinned hornblende (a = yellow green, $ = green, y = dark green) being the ferromagnesian minerals. Magnetite, sphene, apatite and zircon make up the accessory minerals. Alteration products include minor “sericite’, chlorite and epidote. Proc, Linn. Soc. N.S.W., 104 (2), (1979) 1980 Dating of Rocks from the Bungonia District, New South Wales P. F. CARR, B. G. JONES and A. J. WRIGHT Carr, P. F., Jones, B. G., & WricuT, A. J. Dating of rocks from the Bungonia district, New South Wales. Proc. Linn. Soc. N.S.W. 104 (2), (1979) 1980: 111-117. The lower part of the Bungonia Limestone contains fossils of Ludlovian (late Silurian) age but no age-diagnostic fauna has been identified from the upper part of the formation or from the overlying Tangerang volcanics. The K-Ar radiometric age determination reported in this study from the Tangerang volcanics (399 m.y.) appears to be too low, suggesting radiogenic argon loss. K-Ar radiometric data for rocks from the southern part of the Marulan Batholith yield a mean age of 398 m.y. (early Devonian) . Since the Tangerang volcanics overlie the Bungonia Limestone and are intruded by the Marulan Batholith they are probably early Devonian. It is suggested that the Tangerang volcanics are a correlative of the Bindook Porphyry which is also intruded by the Marulan Batholith. The southern part at least of the Bindook Porphyry is therefore probably also early Devonian. Extrusion of the Tangerang volcanics, deformation of the Ordovician to early Devonian strata and intrusion of the Marulan Batholith are considered to have been related to the Bowning Orogeny. P. F. Carr, B. G. Jones and A. J. Wright, Department of Geology, University of Wollongong, P.O. Box 1144, Wollongong, Australia 2500; manuscript received 11 July 1979, accepted after revision 24 October 1979. INTRODUCTION Bungonia lies approximately 150 km southwest of Sydney near the western margin of the southern Sydney Basin. Rocks in the Bungonia district (Fig. 1) range in age from Ordovician to Devonian with a few erosional remnants of younger sedimentary and volcanic rocks. The Ordovician to Devonian strata were deposited in the eastern part of the Lachlan Fold Belt and have been described or mentioned by many earlier authors (e.g. Woolnough, 1909; Naylor, 1935, 1936, 1939, 1950; Packham, 1969; Moore, 1976). The aim of the present study was to determine the age of the Bungonia Limestone, Tangerang volcanics and Marulan Batholith. This investigation provides new data derived from K-Ar dating and fossils. All radiometric age determinations presented in this study were carried out by S. Lafferty and D. C. Green using facilities at the Department of Geology and Mineralogy, University of Queensland and techniques outlined by Sutherland et al. (1973). The K-Ar ages have been calculated using the preferred decay constants of Steiger and Jager (1977). PRE-PERMIAN REGIONAL SETTING The Ordovician sequence consists of multiply-deformed siltstones, cherts and quartzites yielding late Ordovician graptolites at a few localities (Naylor, 1935, 1938). Early Silurian shales and siltstones overlie the Ordovician rocks in a small area 6 km west of Bungonia (Naylor, 1935). East of Bungonia the Ordovician strata are unconformably overlain by, or faulted against, late Silurian limestones and shales (Woolnough, 1909) which contain corals, brachiopods, bryozoans, crinoids, nautiloids, trilobites and graptolites (Moore, 1976; Carr et al., at press). Regionally the late Ordovician and late Silurian strata appear to occupy two asymmetrical meridional synclines reaching as far north as the Wombeyan Caves (Naylor, 1935, Proc. Linn. Soc. N.S.W., 104 (2), (1979) 1980 112 DATING OF ROCKS FROM BUNGONIA MARULA is ULAN L \— Cre x — SS iN xii ie ee aly x xX KX X KX KX KK XK X ‘ rc] Berane \X Oxf x x x *78959\ eG “Ne ° ° SSS =< —— [Yl Ln) Ue ep ohait KS Ny / 6 3 5 5 e +f, 0 olf +BUNGONIA Wits 7 7x i Wp ae ee ee if HH] i) wd eer mioa Magica hei) Ole ir. feos ih eo ae ih Bl gravels BINDOOK tuffs,dac.,rh CAINOZOIC silcrete | EARLY PORPHYRY : hbl. daci LATE sst.,congl. 5°] DEVONIAN TANG ANG | acites —— DEVONIAN VOLCANICS | sst.,dac., tuffs adamellite Bea LATE BUNGONIA ay LATE LLONG Devonian BATHOLITH | granodiorite X »% ORDOVICIAN pte sh. cht.sl,sst. [J] GEOLOGICAL ___ SAMPLE FAULT ——— BOUNDARY ~ — LOCATION 7895¢ ROAD —~—— Fig. 1. Locality map and geology of the Bungonia area. 1950) and extending southwards to Windellama (Garretty, 1937) and Bendithera Caves (Packham, 1969). In the South Marulan area Wass and Gould (1969) have shown that the late Silurian limestones and shales are conformably overlain by the Tangerang volcanics which comprise dacites and tuffaceous sedimentary rocks. This sequence is known to extend southwards to Bungonia (Kantsler, 1973; Moore, 1976; Carr et al., at press). Wass and Gould (1969) suggested that the Tangerang volcanics are late Silurian to early Devonian in age. Dacitic and tuffaceous outcrops of the Bindook Porphyry (McElroy and Relph, 1961; Packham, 1969) extend north from Marulan for approximately 70 km to Yerranderie and show many characteristics in common with the Tangerang volcanics. The age of the Bindook Porphyry is known on stratigraphic grounds to be between latest Silurian (Packham, 1969, p.134) and late Devonian (Powell and Edgecombe, 1978). All the Ordovician and Silurian units have been intruded by the Marulan Batholith (Woolnough, 1909; Osborne, 1949) which is a composite body extending almost continuously from near Bungonia to about 8 km south of Bullio. The batholith contains a variety of rock types including granite, granodiorite and quartz- hypersthene porphyry (Osborne, 1949; Joplin et al., 1952; Osborne and Lovering, 1953). AGE DETERMINATIONS Bungonza Limestone. Previous estimates of the age of the Bungonia Limestone, based largely on corals, were middle to late Silurian (Woolnough, 1909; Wass and Gould, Proc. Linn. Soc. N.S.W., 104 (2), (1979) 1980 P.F. CARR, B.G. JONES AND A.J. WRIGHT 113 1969). More recently Moore (1976) suggested a late Silurian age based in particular on a graptolite fauna including Bohemograptus bohemicus tenuis (locality 1, Appendix I), and shelly fossils including encrinurid and phacopid trilobites and the brachiopod Plectodonta bipartita (locality 2, Appendix I). These fossils occur in the lower part of the Bungonia Limestone. Rickards et al. (1977, fig. 45), indicated that B.b. tenuis is late Ludlovian, ranging from the lezntwardznenszs zone to the kozlowski zone. Conodont data (Pickett, 1972; Dean-Jones, pers. comm., 1978) are in agreement with this late Silurian age. No age-diagnostic fossils have yet been identified from the upper part of the formation. Therefore the lower part of the Bungonia Limestone is late Ludlovian, and the uppermost beds should prove to be either latest Silurian or early Devonian. Marulan Batholith. The Marulan Batholith intrudes the Bungonia Limestone near South Marulan (Osborne, 1931) and is unconformably overlain by late Devonian sedimentary rocks to the west of Bungonia (Naylor, 1939). Hence on stratigraphic grounds the batholith is younger than late Silurian but older than late Devonian. Evernden and Richards (1962) obtained a Carboniferous age (313 m.y.; recalculated using new constants) for biotite from the batholith and were aware of the anomaly as were Vallance (p.198, zn Packham, 1969) and O’Reilly (1972). In the present study a biotite separate from each of three different phases of the batholith was dated (Table 1 and Fig. 1). The three age determinations are consistent with the sequence of emplacement demonstrated by field studies (z.e. granodiorite (oldest), quartz gabbro, adamellite) , although when the errors (Table 1) are considered, there is no significant age difference between the three dates. The mean age for the emplacement of the southern part of the Marulan Batholith is 398 m.y. (early Devonian) which is consistent with its age on the basis of the local stratigraphy. The age obtained for the southern part of the Marulan Batholith by Evernden and Richards (1962) is inconsistent with the stratigraphy and the ages obtained in the present study. Radiogenic argon was probably lost by the sample. Tangerang volcanics. The only previous published reference to the age of the Tangerang volcanics is that of Wass and Gould (1969) who suggested a late Silurian to early Devonian age for the toscanites, tuffs and tuffaceous sandstones which appear to overlie the Bungonia Limestone conformably. In the Bungonia area the Tangerang volcanics consist of plane-bedded, cross-bedded or massive lithic to sublithic sandstones (tuffaceous in part) and thick lensoidal dacite and hornblende dacite units. The dacites in the upper part of the Tangerang volcanics contain hornblende phenocrysts which are absent from the lower dacites. TABLE I K-Ar data for igneous rocks from the Bungonia area K,0 tb 40 Sample Material Latitude Longitude Ar* % 40 Ag Number REE uYne dated south east (av.) (107°ce/gm) Ar® (m.y.) 7892 adamellite biotite 34°51.7' 149°56.5' 6.63 9.413 90.5 ag Sy 7893 quartz gabbro biotite 34°50.9' 149°56.9' 7.23 10.313 74.8 395 2 8 7895 granodiorite biotite 34°49 ,9' 149°58.2' 7.05 10.374 94.8 406 +7 7896 hornblende hornblende BASS Oeil MEQ? 7/ aif Ioil2 1.616 93.4 399 + 7 dacite dg = 4.962 x 1071” yr? a, + 90 = 0.581 x 10729 yr}, 4% = 9.01167 atom % Errors are taken at the 95% confidence level. Sample numbers refer to the University of Wollongong rock collection. Proc, Linn. Soc. N.S.W., 104 (2), (1979) 1980 114 DATING OF ROCKS FROM BUNGONIA Fossils found within this unit (localities 3 and 4, Appendix I) indicate that it was at least partly deposited under marine conditions. However, the fossils, which are poorly preserved bryozoans, crinoid ossicles and rare corals, do not provide a refined age for the unit. A K-Ar age determination was carried out on a hornblende separate from sample 7896 of the hornblende dacite (Table 1, Appendix II). The age of 399 m.y. is very close to the mean age obtained for the emplacement of the Marulan Batholith which intrudes the volcanics. Thus the 399 m.y. date for the Tangerang volcanics is probably too young to represent the age of extrusion of the hornblende dacite, and may result from loss of radiogenic Ar by the hornblende. On the basis of the K-Ar ages for the Marulan Batholith, the Tangerang volcanics were extruded more than 398 m.y. ago. The maximum age of the formation is provided by the Bungonia Limestone, so the Tangerang volcanics must have been extruded during the early Devonian (or possibly the latest Silurian) . Woolnough (1909), Naylor (1935) and Osborne and Lovering (1953) considered the silicic volcanic rocks in the Marulan area (Tangerang volcanics of Wass and Gould, 1969) to be shallow intrusions and to be intimately associated in time, and possibly comagmatic, with the rocks of the Marulan Batholith. O’Reilly (1972) , however, concluded that the Marulan Batholith and the silicic volcanics were ‘discrete entities’. The new data show that the volcanics and the rocks of the batholith are indeed closely associated in space and time and a genetic relationship between the two, as suggested by earlier workers, is possible. Bindook Porphyry. The Bindook Porphyry is a meridionally-trending belt of dacites, rhyolites, crystal and lithic tuffs and hypersthene porphyrites (McElroy and Relph, 1961). At Yerranderie only the upper dacite flows in the Bindook Porphyry contain biotite and hornblende (Joplin et al., 1952). Jones et al. (1977) noted the abundance of ash-flow tuffs in the Yerranderie area and suggested that the dacites and tuffs are remnants of an early to middle Devonian volcano. Powell and Edgecombe (1978) concluded that late Devonian strata unconformably overlie the Bindook Porphyry near Yerranderie. O'Reilly (1972) described part of the western margin of the Bindook Porphyry (invalidly named ‘Brayton Volcanics’ as Brayton limestone [Naylor, 1950] has priority) as a series of extrusive toscanites and dacites and associated tuffs. She assigned (O’Reilly, 1972) a late Silurian to early Devonian age to the unit based on its apparent conformity with the Silurian sequence in the Brayton area, and the contact metamorphic effects where the Bindook Porphyry is intruded by part of the Marulan Batholith (Lockyersleigh adamellite) . It is suggested that the Tangerang volcanics are a correlative of the Bindook Porphyry based on the following: (1)although the units are separated by intrusions of the Marulan Batholith, the Tangerang volcanics form a possible southerly extension of the Bindook Porphyry ; (2) both occupy a similar stratigraphic position in that at least part of each unit conformably overlies late Silurian limestones (Wass and Gould, 1969; O'Reilly, 1972) ; and (3)both are similar, consisting of hypersthene-bearing acid volcanics, with hornblende dacites largely restricted to the upper parts of the sequences. The suggested correlation of the Bindook Porphyry and Tangerang volcanics implies an early Devonian age (possibly extending to latest Silurian) for at least the southern part of the Bindook Porphyry. IMPLICATIONS The new stratigraphic and radiometric data contribute to our understanding of Proc. LINN. Soc. N.S.W., 104 (2), (1979) 1980 P. F. CARR, B.G. JONES AND A.J. WRIGHT 115 the Bungonia district. The unconformity below the late Devonian strata indicates that there was post-early Devonian folding. In terms of the orogenies recognized in this part of the Lachlan Fold Belt, this phase of folding could represent either the Bowning Orogeny or the Tabberabberan Orogeny. However, the K-Ar ages (mean 398 m.y.) indicate that the southern part of the massive Marulan Batholith was emplaced during the early Devonian. Thus the Bungonia area records the Bowning Orogeny which was responsible for movements occurring at the end of the Silurian and throughout the early Devonian (Packham, 1969). Associated with the orogeny in this area was the extrusion of the Tangerang volcanics, the subsequent folding of the Ordovician to early Devonian strata, and the intrusion of the batholith. Acid volcanics of early Devonian age — which occur at Yarrangobilly, Canberra, south of Cowra, northwest of Forbes and west of Molong (Packham, 1969) — are possible correlatives of the Bindook Porphyry and Tangerang volcanics, as are the volcanics in the Bowning Group at Bowning (Link and Druce, 1972). In addition to the Marulan Batholith, other large granite and granodiorite batholiths including the Kosciusko Granite, the Murrumbidgee Batholith and the Gunning-Wyangala Batholith were emplaced during the Bowning Orogeny (Packham, 1969). ACKNOWLEDGEMENTS We thank the University of Wollongong Research Grants Committee for financial support. The assistance given by A. Ewart and E. Thompson in connection with dating facilities at the Department of Geology and Mineralogy, University of Queensland is greatly appreciated. We acknowledge with gratitude A. C. Cook who encouraged geological research at Bungonia. A. C. Cook, R. A. Facer and D. C. Green kindly read an early version of the manuscript. R. B. Rickards supplied information concerning graptolite ranges. References Carr, P. F., Jones, B. G., KANSTLER, A. J., Moore, P.S., and Cook, A. C., (at press). — The geology of the Bungonia district, New South Wales. Proc. Linn. Soc. N.S.W. EVERNDEN, J. F., and RicHarps, J. R., 1962. — Potassium-argon ages in eastern Australia. J. geol. Soc. Aust., 9: 1-49. GaRRETTY, M. D., 1937. — Geological notes on the country between the Yass and Shoalhaven Rivers. J. Proc. R. Soc. N.S.W., 70: 364-374. Jones, J. G., McPuie, J., and Roots, W. D., 1977. — Devonian volcano at Yerranderie. Search, 8: 242-244. Jopiin, G. A., Hanon, F. N., and Noakegs, L. C., 1952. — Wollongong — 4 mile Geological Series. Explan. Notes Bur. Miner. Resour. Geol. Geophys. Aust. KANTSLER, A., 1973. — The geology of an area near Bungonia, New South Wales. Wollongong: Wollongong University College, B.Sc. (Hons) thesis, unpubl. Link, A. G., and Druce, E. C., 1972. — Ludlovian and Gedinnian conodont stratigraphy of the Yass Basin, New South Wales. Bull. Bur. Miner. Resour. Geol. Geophys. Aust., 134. McE roy, C. T., and RELpH, R. E., 1961. — Explanatory Notes to accompany geological maps of the inner catchment, Warragamba storage. Tech. Rep. Dept. Mines N.S.W. (1958), 6: 65-80. Moore, P. S., 1976. — Silurian sediments at Bungonia, New South Wales. Sedzmentological Newsletter, 7: 21-22). Naytor, G. F. K., 1935. — Note on the geology of the Goulburn district, with special reference to Palaeozoic stratigraphy. J. Proc. R. Soc. N.S.W., 69: 75-85. ———, 1936. — The Palaeozoic sediments near Bungonia: their field relations and graptolite fauna. /. Proc. R. Soc. N.S.W., 69: 123-134. —— , 1938. — Graptolites of the Goulburn district, New South Wales. Part I. Some forms and localities. /. Proc. R. Soc. N.S.W., 72: 129-135. ——, 1939. — The age of the Marulan Batholith. J. Proc. R. Soc. N.S.W., 73: 82-85. ——, 1950. — A further contribution to the geology of the Goulburn district, N.S.W. J. Proc. R. Soc. N.S.W., 83: 279-287. Proc. Linn. Soc. N.S.W., 104 (2), (1979) 1980 116 DATING OF ROCKS FROM BUNGONIA O’REILLY, S. Y., 1972. — Petrology and stratigraphy of the Brayton district, New South Wales. Proc. Linn. Soc. N.S.W., 96: 282-296. Osporn_, G. D., 1931. — The contact metamorphism and related phenomena in the neighbourhood of Marulan, New South Wales. Part I: The quartz-monzonite — limestone contact. Geol. Mag., 69: 289-314. ——, 1949. — Contributions to the study of the Marulan Batholith. Part I. The contaminated granodiorites of South Marulan and Marulan Creek. J. Proc. R. Soc. N.S.W., 82: 116-128. ——, and LovERING, J. F., 1953. — Contributions to a study of the Marulan Batholith. Part II. The granodiorite-quartz porphyrite hybrids. J. Proc. R. Soc. N.S.W., 86: 108-118. PACKHAM, G. H. (ed.), 1969. — The geology of New South Wales. J. geol. Soc. Aust., 16: 1-654. PickETT, J. W., 1972. — Fossils from the limestone near Bungonia Caves. N.S.W. Geol. Surv. Pal. Rep. No. 72/1 [unpubl. ]. PowELL, C. McA., and EDGECOMBE, D. R., 1978. — Mid-Devonian movements in the northeastern Lachlan Fold Belt. J. geol. Soc. Aust., 25: 165-184. Rickarps, R. B., Hutt, J. E., and Berry, W. B. N., 1977. — Evolution of the Silurian and Devonian graptoloids. Bull. Br. Mus. nat. Hist. (Geol.), 28. STEIGER, R. H., and JAGER, E., 1977. — Subcommission on geochronology: convention on the use of decay constants in geo- and cosmochronology. Earth Planet. Sci. Lett., 36: 359-362. SUTHERLAND, F. L., GREEN, D. C., and Wyatt, B. N., 1973. — Age of the Great Lake basalts, Tasmania, in relation to Australian Cainozoic volcanism. J. geol. Soc. Aust., 20: 85-94. Wass, R. E., and Gou.p, I. G., 1969. — Permian faunas and sediments from the South Marulan district, New South Wales. Proc. Linn. Soc. N.S.W., 93: 212-226. WooLnouGH, W. G., 1909. — The general geology of Marulan and Tallong, N.S.W. Proc. Linn. Soc. N.S.W., 34: 546-553. APPENDIX I FOSSIL LOCALITIES Locality 1. Bungonia Limestone. Ludlovian (late Silurian) . Grid reference 715365, Kooringaroo 1 : 25,000 Series Topographic Map. Fauna includes: trilobites, ? Encrinurus and cf. Phacops crosslez; brachiopods, Plectodonta bipartita, cf. Visbyella. Identifications by A. J. Wright. Locality 2. Bungonia Limestone. Ludlovian (late Silurian). Grid reference 729396, Bungonia 1:25,000 Series Topographic Map. Fauna includes Bohemograptus bohemicus tenuis. Identification by G. H. Packham. Locality 3. Tangerang volcanics. Possibly latest Silurian in part, probably early Devonian. Grid reference 005017, Caoura 1:31,680 Series Topographic Map. Fauna includes indeterminate crinoid ossicles, corals and bryozoans. Identifications by P. F. Carr and B. G. Jones. Locality 4. Tangerang volcanics. Possibly latest Silurian in part, probably early Devonian. Grid reference 732427, Bungonia 1:25,000 Series Topographic Map. Fauna includes indeterminate corals and crinoid ossicles. Identifications by P. F. Carr and B. G. Jones. APPENDIX II Brief descriptions of samples dated by K-Ar method. Sample localities are specified by grid references from the Bungonia 1: 25,000 Series Topographic Map. 7892 Medium- to coarse-grained adamellite consisting of K-feldspar, plagioclase, quartz, biotite, hornblende, apatite, zircon, sphene and iron-titanium oxides. Alteration has produced chlorite, sericite, epidote and prehnite. The biotite is slightly chloritized and contains minor prehnite. G.R. 689385. 7893 Medium- to coarse-grained quartz gabbro consisting of plagioclase, augite, biotite, hypersthene, hornblende, iron-titanium oxides, interstitial quartz and minor apatite and K-feldspar. Alteration has produced sericite, carbonate, fibrous amphibole and pyrite. The biotite is slightly chloritized. G.R. 697397. 7895 Medium- to coarse-grained granodiorite consisting of plagioclase, K-feldspar, quartz, biotite, hornblende, iron-titanium oxides, diopside, hypersthene, apatite and zircon. Alteration has Proc. LINN. Soc. N.S.W., 104 (2), (1979) 1980 P. F. CARR, B.G. JONES AND A.J. WRIGHT 117 produced chlorite, fibrous amphibole, prehnite, epidote and kaolinite. The biotite is slightly chloritized. G.R. 716416. 7896 Porphyritic hornblende dacite with phenocrysts of quartz, hornblende, plagioclase and hypersthene in a very fine-grained groundmass of quartz, plagioclase, K-feldspar, hornblende, biotite, hypersthene and iron-titanium oxides. Alteration has produced chlorite, sericite and kaolinite. The hornblende is slightly chloritized. G.R. 709412. Proc. Linn. Soc. N.S.W., 104 (2), (1979) 1980 The Benthos of the Kosciusko Glacial Lakes B. V. TIMMS Timms, B. V. The benthos of the Kosciusko glacial lakes. Proc. Linn. Soc. N.S.W. 104 (2), (1979) 1980: 119-125. Twenty-one macrobenthic species are recorded with a range of 8 to 12 species per lake. Common species include Antzpodrilus davidis, the phreatoicid isopod Metaphreatoicus australis, Chironomus ?oppositus and Pisidium tasmanicum. The latter three species together with an unidentified gammarid amphipod are typical of highland lakes in south-eastern Australia. Relative numbers and distribution in the lakes appear to be influenced by fish predation. Momentary biomass levels range from 2.4-14.9 g m® and in some lakes benthic production must be based largely on allochthonous organic matter. B. V. Timms, Science Department, Avondale College, Cooranbong, Australia 2265; manuscript recetved 5 March 1979, accepted in revised form 24 October 1979. INTRODUCTION Blue Lake, near Mt. Kosciusko, was one of the first Australian lakes to be dredged for benthic invertebrates; Hedley took samples from 28m there sometime during 1905/6. Descriptions of three worms (Antipodrilus davidis, Branchiura pleurotheca ( = Rhycodrilus coccineus) , Phreodrilotdes notabilis) and two endemic molluscs (Glactdorbis hedleyi, Glacipistum kosciusko) were subsequently published (Benham, 1907 and Iredale, 1943, respectively). There have been few further investigations on Blue Lake and the other nearby lakes (Cootapatamba, Albina and Club) despite their being the only glacial lakes in mainland Australia, and the highest in altitude (1890m, 2070m, 1920m, 1950m, respectively) in all Australia. Information is available on their physiography (Dulhunty, 1945), water chemistry (Williams, Walker and Brand, 1970), phytoplankton (Powell, 1970), zooplankton (Bayly, 1970) and on some other invertebrate inhabitants (e.g. Ball, 1977; Hynes and Hynes, 1975). The present paper is concerned with the composition, diversity and standing crops of the benthic invertebrates of the lakes. Only the herpobenthos was sampled and attention was focused on macro-invertebrates. This paper is one of a series on the benthos of Australian lakes, aspects of which have recently been reviewed by Martin and Timms (1978) , and Timms (in press) . METHODS The lakes were visited during February 7-11, 1976. Sampling stations were chosen in each lake to represent the area and depth range as adequately as possible. In Blue Lake there were 7 stations at roughly 4m depth intervals from 1 to 26m. There were 8 stations in Lake Albina, 4 in each basin. Five stations were used in Cootapatamba but only two in the small Club Lake. At each site quadruplicate samples were collected with a Birge Ekman grab of 200 cm? gape and sieved through mesh of aperture 0.4 mm. The organisms retained were sorted alive in the field and then preserved in 70% alcohol. This results in up to a 10% weight loss (Weiderholm and Erikson, 1977). In the laboratory the number of individuals of each species and the wet biomass of each taxonomic group were determined for each sample. In the preparation of samples for weighing, excess external water was blotted and the shells of molluscs removed beforehand. A mean Proc. Linn. Soc. N.S.W., 104 (2), (1979) 1980 120 BENTHOS OF THE KOSCIUSKO LAKES weighted biomass was calculated for each lake by integration using bathymetric charts given in Dulhunty (1945). Samples of the substrate were taken from the deepest station in each lake and stored at 5°C before drying. Then they were analysed for organic matter by % loss on ignition at 550°C and for %C and %N by the CSIRO Microanalytical Service. SOME PHYSICOCHEMICAL FEATURES OF THE LAKES The water of all four lakes is very fresh (salinity < 3 ppm) with a pH near 6 (Williams, Walker and Brand, 1970). Their water is transparent (eg. Secchi disc depth of ca 6m in Blue Lake). Seasonal temperature regimes are unknown, but all four freeze over for several months during winter; Blue Lake was stratified (11°C at surface and 8°C at 12m), Albina was weakly stratified while the two shallow lakes, Lake Cootapatama and Club Lake, were isothermal when visited in February. Thus at least two of the Kosciusko glacial lakes are of the warm thereimictic type (see Bayly & Williams, 1973) while Blue Lake is possibly dimictic and as such would be the only known example of this type on mainland Australia, though examples occur in highland Tasmania (P. Tyler, personal communication). There were no indications of hypolimnetic oxygen deficiencies in Blue or Albina. TABLE 1 Some chemical characteristics of the lake muds Sample Organic Carbon Nitrogen Lakes depth Matter % % C/N ratio (m) % Blue 26 12.1 5.21 0.56 9.30 Club 2 7.1 2.44 0.36 6.77 Albina 8.5 23.1 11.59 0.80 14.48 Cootapatamba 3 16.5 6.49 0.73 8.89 Bottom substrates were largely sandy-grit to sandy-mud in Lake Cootapatamba (except at stations > 2m) and at stations <]m in Club Lake and Lake Albina, and <5m in Blue Lake. In the latter visible organic detritus was particularly obvious in the 8 and 12m stations. Deeper stations in all lakes were of fine organic mud. Muds from the deepest stations in each lake had organic matter contents ranging from 7.1 - 23.1%, carbon contents 2.4 - 11.6% and nitrogen levels 0.36 - 0.80% (Table 1). Carbon/nitrogen ratios are <10 in Blue Lake, Club Lake and Lake Cootapatamba, but in Lake Albina the ratio is much higher (14.5) indicating considerable input of allochthonous organic matter (Hansen, 1959). The source of at least some of this could well be septic effluent from Albina Hut. RESULTS (a) Blue Lake. Twelve macrobenthic species were recorded from Blue Lake; the dominants were Antipodrilus davidis, Chironomus 2oppositus and Glacipisidium kosctusko (Table 2). At least two mesobenthic species — the ostracod Candonocypris n. sp. and the mite Oxus australicus Lundblad live associated with the bottom. Number of species, abundance and biomass were greatest in the sub-littoral (Table 2). Despite the lake being relatively deep, there were no species restricted to the profundal, the common species there being the dominants. Mean weighted biomass was 12.3 gm”, with chironomids the most important contributor (63%) and oligochaetes next (25%). Proc. Linn. Soc. N.S.W., 104 (2), (1979) 1980 B. V. TIMMS 121 TABLE 2 Blue Lake benthos — species present, their abundance (as individuals m™) and biomass with depth. Species lm 4m 8m 12m 16m 20m 26m unidentified large nematode = - 11 — — — = aan, cans 177 499-1289 965 810 1209 477 Tubificidae n. gen. Metaphreatoicus australzs — 11 399 11 11 = = Procladzus sp. — 11 78 33 11 11 33 Polypedilum nr tonnozre = = 11 22 = ~ _ Chironomus ?oppositus 1132 3274 3951 3152 3340 2642 2120 Tasmanophe bia nigrescens _ 11 = = = ~ — Ramrheithrus dubitans 11 22 - — 11 ~ = unidentified tipulid larva 22 = _ - - = _ Glactdor bis hedleyz — 11 — - _ _ —_ Glactpisium kosciusko 44 1100 1643 1798 739 480 242 Total Numbers (individualm™) 1386 4939 7325 5981 4922 4342 2872 Total Biomass (g m7) 3.67 14.72 23.49 14.40 11.49 12.17 7.05 (b) Club Lake. Eight macrobenthic (Table 3) and three mesobenthic species (Candonocypris n. sp., the cladoceran Bzapertura affinis and the copepod Macrocyclops albidus) were noted in the 8 grabs. Chironomus ?oppositus was dominant while Prszdium tasmanicum and unidentified turbellarian were common. Mean weighted biomass was 2.4 g m™” with chironomids the most significant contributor (60%). TABLE 3 Club Lake benthos — species present, their abundance (as individuals m™) and biomass with depth. Species lm 2m unidentified green turbellarian 855 355 unidentified large nematode 66 177 Antipodrilus davidis 344 89 Metaphreatoicus australis - 11 Procladzus sp. 33 111 Chironomus ?opposztus 1432 4074 Glacidor bis hedleyz 11 — Pisidium tasmanicum 455 333 Total Numbers (as individual m™”) 3196 5150 Total Biomass (as gm”) 2.30 3.12 (c) Lake Albina. Both basins yielded nine species (Table 4). There were no significant differences in distribution patterns between the basins or at different depths. The phreatoicid isopod Metaphreatozcus australts and Pisidium tasmanicum were dominant, while Antzpodrilus davidis, Procladius villosimanus and Tanytarsus paskervillensis were relatively important. Isopods were the main contributor (91%) to the mean weighted biomass of 14.9 gm”. (d) Lake Cootapatamba. Ten macrobenthic species and Candonocypris n. sp., were noted in the 20 grabs (Table 5). The dominant species numerically was Antzpodrilus davidis; it and other common species including Metaphreatozcus australis and Pisidtum tasmanicum occurred at all depths sampled. Proc. Linn. Soc. N.S.W., 104 (2), (1979) 1980 122 BENTHOS OF THE KOSCIUSKO LAKES TABLE 4 Lake Albina benthos — species present, their abundance (as individuals m™) and biomass with depth. South Basin North Basin Species 0.5m lm 2m 3.5m 3m 5m 6.5m 8.5m Spathula truculenta 11 33 — = 11 33 22, 55 Antipodrilus davidis 22 11 311 644 344 455 888 533 unidentified gammarid amphipod 11 — - - 11 11 710 67 Metaphreatoicus australis 722 2387 1199 1265 444 533 1276 1210 Procladius villosimanus 56 244 400 588 211 211 255 233 Tanytarsus paskervillensis - 11 200 544 322 11 11 33 Chironomus ?oppositus — — 44 56 33 66 122 89 Glacidor bis hedleyz — = 22 — 22 — 55 Pisidium tasmanicum 33 599 737 333 732 866 2309 3109 Total Numbers (individual m””) 855 3285 2913 3430 2130 2186 5593 5384 Total Biomass (g m™) 9.92 30.64 12.72 21.66 7.33 9.02 36.98 26.70 TABLE 5 Lake Cootapatamba benthos — species present, their abundance (as individuals m™”) and biomass with depth. Species 0.5m lm 1.5m 2.2m 3m unidentified green turbellarian - 11 _ ~ _ Antipodrilus davidis Tubificidae n. gen. 1565 3052 577 1121 133 Dero furcatus unidentified gammarid amphipod 477 55 155 78 67 Metaphreatoicus australis 388 178 311 444 200 Procladius villosimanus -- -- 11 33 56 Tanytarsus sp. — 100 122 400 200 Chironomus ?oppositus — — - 11 — Austretthrus sp. 11 = = = = Pistdium tasmanicum 144 325 335 389 267 Total Numbers (individual m”) 2585 3721 1511 2476 923 Total Biomass (g m™) 10.37 9.13 10.33 9.77 5.64 Mean weighted biomass was 9.5 g m™, with isopods the most important (71%) and oligochaetes next (21%). DISCUSSION (a) Community Structure. Twenty-one macrobenthic species were collected from the four lakes, with a range of 8 to 12 in each (Table 6). Typically each lake contained a turbellarian, an oligochaete, an isopod, two to three chironomids including Chironomus ?oppositus, a snail and a sphaerid bivalve. This low diversity is typical of lakes in Australia (Timms, in press) but it is even less than “average” (cf. mean of 16.6 species in 16 lakes in lowland of south-eastern Australia and 21.3 in 7 Tasmanian lakes — Timms, 1978). Possible reasons for the general situation are given in Timms (in press), while in the case of the Kosciusko lakes, factors such as physicochemical harshness and small size (and hence high homogeneity) could restrict diversity further. Most species listed in Tables 2-6 have been recorded from the area before, many as stream dwellers, e.g. the crustaceans, mayfly and caddisflies. In that the Proc. Linn. Soc. N.S.W., 104 (2), (1979) 1980 B. V. TIMMS 123 TABLE 6 Presence and relative abundance of macrobenthic species in the Kosciusko Lakes. (Key: + + + + = verycommon, + + + = common, + + = present; and + = uncommon). Blue Club Lake Lake Species Lake Lake Albina Cootapatamba Platyhelminthes Spathula truculenta Ball +r unidentified green turbellarian +++ af Nematoda unidentified large nematode + cP ar Oligochaeta Antipodrilus davidis ) Par oP Tubificidae n. gen. fe fy oh Dero furcatus (Muller) Crustacea Metaphreatoicus australes +f ar qP ae aR AP ap) ae unidentified gammarid amphipod ~ + Insecta: Ephemeroptera Tasmanophlebia nigrescens Till. at Insecta: Trichoptera Austrheithrus dubitans Mos. + Ramrhetthrus sp. + Insecta: Diptera Procladius villosemanus Kieffer +++ + Procladius sp. at State Tanytarsus paskeruvillensts Glover ++ Tanytarsus sp. ++ Polypedilium nr. tonnozrz Freeman + Chironomus ?oppositus Walker oP AP ap ar ar qF ar + unidentified tipulid larva + Mollusca Glacidor bis hedleyi Iredale + ar + Glacipistum kosciusko Iredale ap ar Ie Pisidium tasmanicum Ten. Wood +P ap ar qP ar ar ap oF + + + + inadequately described Glactpistum kosctusko appears to be synonymous with Pisidium tasmanicum, the presence of the latter is not new. Two notable absences are Benham’s worms, Rhycodrilus coccineus and Phreodrilotdes notabilis which must be uncommon and easily overlooked or no longer present. At least three new species have been found — a tubificid worm, a candonocyprid ostracod, and a gammarid amphipod. They are to be described in due course by the appropriate taxonomists (see acknowledgements) . Although there is a core of species common to all lakes, there is a marked difference in the distribution and relative abundance of some species between Blue and Club Lakes in which the mountain minnow Galaxzas findlay: is common and Lakes Albina and Cootapatamba which lack fish (Table 6). To illustrate, Chironomus ?oppositus is abundant, Metaphreatoicus australis uncommon and the gammarid amphipod not present in the benthos of Blue and Club Lakes, while in Lakes Albina and Cootapatamba, Chironomus ?oppositus is uncommon, Metaphraetotcus australis very common and the amphipod is present. A continuing study on the littoral fauna of the lakes (Timms, unpublished) is revealing other differences in the distribution and relative numbers of invertebrates and tadpoles in the two lake groups, while Hebert (1977) notes the absence of the large planktonic cladoceran, Daphnia nivalis (syn. D. alpina) from the two lakes with fish. It seems Proc. Linn. Soc. N.S.W., 104 (2), (1979) 1980 124 BENTHOS OF THE KOSCIUSKO LAKES then, that predation by fish is an important determinant of community structure in these lakes, as it is some lakes elsewhere (eg. Tuunainen, 1970). (b) Zoogeography. Of the species identified only a few (e.g. Procladzus villostmanus, Antipodrilus davidis) are common components of benthic communities of Australian lakes. Five species, Metaphreatoicus australis, Tasmanophlebia nigrescens, Austrheithrus dubztans, Spathula truculenta, and Glacidorbis hedleyi are restricted to the highlands of south-eastern Australia. There appear to be no endemic species, unless the undescribed or unidentified species are. All the dominant species (Metaphreatotcus australis, Chironomus 2oppositus, Pisidium tasmanicum) and many of the common ones belong to a group important in Lake Tarli Karng (the only other deep lake in the highlands of southeast mainland Australia; Timms, 1974) and in the highland Tasmanian lakes investigated by Timms (1978). This reinforces the biographical relationships between the highland areas of south-eastern Australia noted for other communities. (c) Bzomass. Taken that the mean biomass figures for the lakes are not annual means, but momentary values, and that the figures for Lakes Cootapatamba and Albina may be elevated due to lack of fish predation (by up to a factor of 2 — Kajak, 1972) the figures for all lakes except Club are unexpectedly high for lakes which on other criteria (e.g. water chemistry, sparse phytoplankton) appear oligotrophic. It seems this is because benthic production is based largely on allochthonous organic matter input (cf. Bretschko, 1975). Although no data are available on organic matter input, particulate input must be significant at least in Blue Lake and Lake Albina where partly decomposed leaves and twigs were commonly recovered from samples; additionally in Lake Albina, the septic effluent from Albina Hut probably adds organic matter. Percent organic matter is greatest in Lake Albina mud where the C/N ratio indicates considerable input of allochthonous matter and least in Club Lake where the flushing of the lake prevents any accumulation. Mean biomass figures apparently reflect the levels of organic matter in the four lakes (Table 7). However the correlation is not statistically significant (r = 0.840 P = 0.05). By comparison, some other lakes at high altitudes in southeastern Australia e.g. Lakes St. Clair, Dobson, Tarli Karng (Timms, 1974, 1978) also have considerable allochthonous organic matter input and associated higher, benthic standing crops than expected on other criteria. The dominant contributors to biomass in each lake are surface feeding detritivores — Metaphreatozcus australis in Lakes Cootapatamba and Albina and Chironomus ?oppositus in Blue and Club Lakes. Oligochaetes and molluscs (almost TABLE 7 Percentage contribution to total biomass by species according to eight taxonomic groupings. Parameter Cootapatamba Albina Club Blue % organic matter in mud 16.5 23.1 7.1 12.1 Mean Standing Crop (g/m?) 9.48 14.87 2.44 12.31 % contribution to biomass Planarians 0.1 0.1 Ze Oligochaetes 20.5 3.5 14.2 24.5 Phreatoicids 70.6 91.3 0.4 4.0 Amphipods 6.4 1.1 Chironomids 0.4 2.7 59.7 62.9 Snails 0.1 0.1 Bivalves 1.8 1.2 12.9 7.8 Others 0.2 0.6 0.7 Proc. LINN. Soc. N.S.W., 104 (2), (1979) 1980 B. V. TIMMS 125 entirely of sphaerid bivalves) are relatively important in at least two lakes (Table 7). It is the importance of Chzronomus ?oppositus, crustaceans and sphaerid bivalves which characterize the Kosciusko glacial lakes, separating them from lakes of lowland eastern Australia where these taxa are absent or unimportant (Timms, in press) and even from highland Tasmanian lakes, where although Chzronomus ?opposztus and crustaceans are often important, sphaerid bivalves usually are not (Timms, 1978) . ACKNOWLEDGEMENTS I am indebted to Donna Craig, Greg Gambrill, Tony Martin and Gary Paul for field assistance, to N.S.W. National Parks and Wildlife Service for permission to collect in protected areas and to Dr. P.S. Lake for his comments on the manuscript. Identifications by the following taxonomists are appreciated: Dr. I. Ball (Turbellaria), Dr. R. Brinkhurst (Oligochaeta) , Mr. N. Colman (Gastropoda), Mr. P. DeDekker (Ostracoda), Dr. B. Knott (Isopoda), Mr. K. Kuiper (Bivalva), Dr. J. Martin (Chironomidae), Mr. D. Morton (Cyclopoida), Dr. A. Neboiss (Trichoptera), Dr. E. Reik (Ephemeroptera), Dr. K. O. Viets (water mites), and Prof. W. D. Williams (Amphipoda) . References BALL, I. R., 1977. — A monograph of the genus Spathula (Platyhelminthes: Turbellaria: Tricladida). Aust. J. Zool. Suppl. Ser. No. 47. 1-43. BayLy, I. A. E., 1970. — A note on the zooplankton of the Kosciusko region. Aust. Soc. Limnol. Bull. 3: 25-28. , and WILLIAMS, W. D., 1973. — Inland Waters and their Ecology. Melbourne: Longman. BENHAM, W. B., 1907. — On the Oligochaeta from the Blue Lake, Mount Kosciusko. Rec. Aust. Mus. 6: 251-264. BRETSCHKO, G., 1973. — Benthos production of a high-mountain lake: Nematoda. Verh. Int. Verezn. Limnol. 18: 1421-8. DuLuHunty, J. A., 1945. — On glacial lakes in the Kosciusko region, J. Proc. Roy. Soc. N.S.W. 79: 143-152. HANnsEN, K., 1959. — The terms gyttja and dy. Hydrobiologza 13: 309-315. HEBERT, P. D.N., 1977. — A revision of the taxonomy of the genus Daphnia (Crustacaea: Daphnidae) in south-eastern Australia. Aust. J. Zool. 25: 371-398. Hynes, H. B.N., and Hynes, Mary, E., 1975. — The life histories of many of the Stoneflies (Plecoptera) of south-eastern mainland Australia. Aust. J. Mar. Freshwat. Res. 26: 113-153. IREDALE, T., 1943. — A basic list of the freshwater Mollusca of Australia. Aust. Zool. 10: 188-230. Kayak, Z., 1972. — Analysis of the influence of fish on benthos by the method of enclosures zm “Productivity Problems in Freshwater’ (edits. Z. Kajak and A. Hillbrient-Ilkowska) Proceedings of the IBP- UNESCO Symposium, Poland, 1970. MartTIN, J., and Timms, B. V., 1978. — The benthos of Australian lakes with particular reference to the Chironomidae. In Tvtles and Abstracts, North American Benthological Society, 26th Annual Meeting. Compiled by D. M. Rosenberg. PowLING, I. Joan, 1970. — A note on the phytoplankton of the Kosciusko region. Aust. Soc. Limnol. Bull. 3: 29-32. Tims, B. V., 1974. — Aspects of the limnology of Lake Tarli Karng, Victoria. Aust. J. Mar. Freshwat. Res. 25: 273-279. ——, 1978. — The benthos of seven lakes in Tasmania. Arch. Hydrobzol. 81: 422-444. ——, (in press). — The benthos of Australian lakes. In W. D. Williams (ed.), A Bzological Baszs for Water Resource Management in Australia. Canberra: A.N.U. Press. TUUNAINEN, P., 1970. — Relations between the benthic fauna and two species of trout on some small Finnish lakes treated with rotenone. Ann. zool. Fennici 7: 67-120. WIEDERHOLM, T., and Ericksson, L., 1977. — Effects of alcohol-preservation on the weight of some benthic invertebrates. Zoon. 5: 29-31. WILLIAMS, W. D., WALKER, K. F., and BRAND, G. W., 1970. — Chemical composition of some inland surface waters and lake deposits of New South Wales. Aust. J. Mar. Freshwat. Res. 21: 103-116. Proc. LINN. Soc. N.S.W., 104 (2), (1979) 1980 Living Australian Schizasterid Echinoids K. J. MCNAMARA and G. M. PHILIP McNamara, K. J., & Puitip, G. M. Living Australian schizasterid echinoids. Proc. Linn. Soc. N.S.W. 104 (2), (1979) 1980:127-146. Seven schizasterid echinoid species are recognized from Australian waters. Four of these Schizaster (Ova) myorensis, S. (Ova) portjacksonensis, S. (Schizaster) sp. A and S. (Schizaster) sp. B are new. The ontogenetic development of S. (Ova) myorensis is described and discussed. Schizaster is re-interpreted and emended. Diploporaster Mortensen 1951 is considered a synonym of S. (Ova) Gray 1825; and Hypselaster H. L. Clark 1917 a synonym of Proraster Lambert 1895. K. J. McNamara, Western Australian Museum, Perth, Australia 6000, and G. M. Philip, Dept of Geology and Geophysics, University of Sydney, Australia 2006; manuscript recetved 21 March 1979, accepted in revised form 19 December 1979. INTRODUCTION The living irregular echinoids of Australia are poorly known. Since H. L. Clark’s (1921, 1932, 1938, 1946) monographs, description of Australian echinoid faunas has been in abeyance. Moreover, Clark dealt largely with a few, poorly localized museum specimens. Detailed taxonomic and ecological work on the irregular echinoids is urgently needed. This paper aims to rectify the situation to a small degree by describing the schizasterid echinoids of Australia. They comprise three genera: Schizaster, Proraster and Moira. Previously (H. L. Clark, 1921, 1932, 1946; Mortensen, 1951; Endean, 1961) the only species of Schzzaster to have been recorded from Australian waters was S. lacunosus (Linnaeus). We propose to show that a further four species of this genus are present, and that the distribution of S. lacunosus is much more restricted than hitherto considered. Two species of Ova, a subgenus of Schizaster, are described: one from Moreton Bay, Queensland, based on relatively large, well-localized collections made by Dr. R. Endean and by Professor W. Stephenson of the University of Queensland; the other is based on two specimens collected from Port Jackson, N.S.W. and housed in the Australian Museum. In the past, species of Schzzaster have been described on the basis of small numbers of specimens. The large collection of the Moreton Bay species has allowed a detailed description and enabled us to study both intraspecific variation within adults of the same population, and the ontogenetic development of the species. Two new species of Schizaster (s. s.) from northern Queensland are described. As each is known only from a single, incomplete test, open nomenclature is employed. In the light of this paper it is to be hoped that more collections will be made of the species to allow them to be named formally. In addition, H. L. Clark’s (1938) “Hypselaster dolosus” from Western Australia is discussed and re-interpreted. Species of Schzzaster occur as far as 35°S on the eastern coast of Australia, but only as far south as 21° on the west. Mozra occurs around the entire Australian coastline. Proraster is confined to warm seas although again extending further south on the east (27°S) than on the west (18°S). SYSTEMATIC DESCRIPTIONS Family SCHIZASTERIDAE Lambert, 1905 According to Mortensen (1951) and Fischer (1966) representatives of the family Schizasteridae possess both peripetalous and lateroanal fascioles. However, a number Proc. Linn. Soc. N.S.W., 104 (2), (1979) 1980 128 LIVING AUSTRALIAN SCHIZASTERID ECHINOIDS do not possess both fascioles. In Proraster the lateroanal fasciole may be incomplete or absent. The genus Abatus, which Mortensen (1951, pp. 250-251) placed in the Schizasteridae, possesses a lateroanal fasciole in the juvenile stage, but this is lost in adults. Amphipneustes lacks both peripetalous and lateroanal fascioles, yet is also included with Mortensen’s and Fischer’s Schizasteridae. In Brisaster the lateroanal fasciole may be reduced or lost in the adult (Mortensen, 1951, p. 280). Both Trzpylus and Parabrissus possess an incomplete lateroanal fasciole; in Parabrissus the lateroanal fasciole is “not observed” (Mortensen, 1951, p. 348). The work of Kermack (1954) and Nichols (1959) suggests that fascioles are not such an important taxonomic feature of spatangoids as has hitherto been considered. The genera included within Mortensen’s and Fischer’s Schizasteridae can be separated into groups based on a combination of morphological characters. As is discussed in more detail elsewhere (McNamara and Philip, 1980) we prefer to describe as schizasterid echinoids genera with the gross test features of Schzzaster, 7.e. the genera Brisaster Gray 1855, Kena Henderson 1975, Mozra Agassiz 1872 (= Motropsis Agassiz 1881), Proraster Lambert 1895 (= Hypselaster H. L. Clark 1917) and Schizaster Agassiz 1838 with subgenera Dzpneustes Arnaud 1891, Paraster Pomel 1869, and Ova Gray 1825 (= Dzploporaster Mortensen 1951). The term is therefore used in a much more restricted sense than either Mortensen (1951) or Fisher (1966). Our current revision of other fossil and living spatangoids should allow formal recognition of the group as a separate family. Genus SCHIZASTER Agassiz 1836 Type Spectes. Schizaster studert Agassiz 1836, p. 185; by subsequent designation of the Thirteenth International Congress of Zoology in Paris; opinion 209, 1948 (Bull. Zool. Nomenclature London, vol. 4, p. 527). Emended diagnosis. Apical system located posteriorly of centre; with two to four genital pores. Ambulacrum III and anterior notch shallow to deep and with pore pairs arranged in single or double rows. Anterior petals at least twice length of posterior petals. Peripetalous and lateroanal fascioles both present and complete. Remarks. A number of schizasterid genera have, in the past, been distinguished largely on the number of genital pores. For instance, Schzzaster was characterized by Mortensen (1951) as possessing two genital pores, Brisaster three and Paraster four. Likewise Dzploporaster was considered to be generically distinct from Ova as it possessed four genital pores, whereas Ova was considered to have only two; though why Dzploporaster should have gained generic rank (Fischer, 1966) whereas Ova was regarded as a subgenus of Schizaster is unclear. Likewise Paraster has sometimes been considered to be only a subgenus of Schzzaster (Kier, 1957; Henderson, 1975). Pomel (1869) proposed Paraster as a genus for species previously referred to Schizaster which possessed four genital pores. However, whether the type species of Schizaster, S. studert, has two or four genital pores remains uncertain. Cotteau (1886, p. 36) thought it had four, though Mortensen (1951, p. 287), thought it had but two. Accordingly, Mortensen characterized Schzzaster as possessing two genital pores and Paraster as having four, irrespective he said, of whether or not the S. studerz was found to include specimens with four genital pores. Henderson (1975, p. 14) believed that S. studert would “probably prove to have four gonopores” but employed Schzzaster for species with only two. Mortensen considered the number of genital pores to be of generic importance, even though he noted that Abatus phillipi Loven may equally often have two or four. Lambert and Thiéry (1924) did not use the number of genital pores as a generic character. Likewise Duncan and Sladen (1882), Currie (1925) and Cooke (1942) Proc. Linn. Soc. N.S.W., 104 (2), (1979) 1980 K. J. MCNAMARA AND G. M. PHILIP 129 have considered this feature to be of only specific importance. Kier (1957) “for the sake of convenience” referred species with four genital pores to the subgenus Paraster, even though he noted intraspecific variation in the number of genital pores in many echinoids. More recently both Chesher (1966) and Kier (1975) have reverted to regarding forms with four genital pores as generically distinct from those with two. The growth and development of S$. (Ova) myorensis sp. nov. shows that at the onset of sexual maturity the posterior pair of genital pores appears first, followed, in most cases, by one of the anterior pair, then the other. However, in some specimens either one, or both, of the anterior pair may fail to develop. Consequently, most members of the population studied possess four genital pores, about 14% have three, and a similar percentage produced only two; these specimens are all large adults. We believe, however, that it is useful to distinguish Paraster as a morphological subgenus of Schzzaster, but not on the basis of the number of genital pores. Based on the morphology of the respective type species, Paraster is employed for species which differ from typical species of Schzzaster s. s. in having a shallower ambulacrum III, a more circular test, a less posteriorly-situated apical system, and straighter anterior ambulacral petals which diverge more strongly. The pore pairs in ambulacrum III are set more transversely in Schzzaster s. s. The evolutionary relationship of the subgenera is discussed elsewhere (McNamara and Philip, 1980). Key to the Australian schizasterid genera Ieelateroanalitasciole rudimentary orabsent 574/24) 8 5 Sa Proraster IALETO AVA pASCLOLE EMULE 2, cates eae eee Is Sas og oveeeey ees Sue il sie aang ye 2. Pore-pairs in ambulacrum III in irregular double series ....... Schizaster (Ova) Pore-pairs in ambulacrum III in regular single series..................... 3. SenetalsionOadalndrOpeniy. °F Jaca 4 aunt. ce aebemu er ee eas Oe Schizaster (Schizaster) etalsemanrowrandiveryidee pn. 6. 5.) re ne il, cee aero Ped ates estas cilcaial sceateteae cit Crate Motra Key to the Australian species of Schzzaster 1. Pore-pairs in ambulacrum III in irregular double series Pore-pairs in ambulacrum III in regular single series 2. Four genital pores and relatively long posterior petals ....... S. (Ova) Pivoneners Two genital pores and relatively short posterior petals .. S. (Ova) portjacksonensis 3. Paired petals narrow, anterior pair weakly flexed distally ; laibuimyshonrt and broadly s)he. ei eens Be S. (Schizaster) sp. nov. B maine dap evalsibrOad.s's (O2))59 SO (Ga) — C0 Coo) 4ee 0) Width ant. paired petals 30.7 (54.0) 32.0 (53.0) 33.0 (51.5) 30.0 (55.5) Width post. paired petals 15.5 (27.0) 15.4 (25.5) 16.0 (25.0) 16.3 (30.0) Length amb. II/IV (36.5) (41.0) (37.5) (37.0) Length amb. I/V 11.7 (20.5) 9.2 (15.2) 10.5 (16.5) 12.0 (22.0) Width peristome 9.0 (16.0) 9.4 (15.5) 7.5 (11.5) 7.0 (13.0) Diameter periproct 6.3 (11.0) 8.4 (14.0) 8.5 (est) 8.8 (16.5) Length labrum to ant. 8211425) Wea S30) ele 272s) nO Ol ise) No. genital pores four two four four Nature of pore pairsin amb. III double double single single Proc. Linn. Soc. N.S.W., 104 (2), (1979) 1980 K.J. MCNAMARA AND G. M. PHILIP 143 teratological specimen. The adoral surface is malformed and the labrum is grossly misshapen (Fig. 10F). A singular feature is the presence of tuberculation on the periplastronal area. This region is virtually free of tuberculation in the holotype (Fig. 10D). Genus PRORASTER Lambert 1895 [ = Hypselaster Clark 1917] Type species. Schizaster atavus Arnaud zn Cotteau 1883, p. 13. Remarks. Mortensen (1951, p. 228) characterized Proraster by its possession of a deep ambulacrum III, with deep anterior notch in the test; a peripetalous fasciole, but not lateroanal fasciole; and four genital pores. On the basis of this definition Proraster differs from Schzzaster only in its lack of a lateroanal fasciole. The genus Hypselaster is here considered to be synonymous with Proraster, as the lateroanal fasciole is rudimentary or lacking. Mortensen (1951, p. 312) noted that Hypselaster is “an unsatisfactorily limited genus”. He further observed that the lateroanal fasciole may be present in a rudimentary form or be entirely absent: yet he gave the main character of Hypselaster as the presence of a rudimentary fasciole. Five specimens in the Australian Museum collection (AM J6625) collected by H. L. Clark from Roebuck Bay, Broome, Western Australia, lack the lateroanal fasciole entirely, while one specimen shows a small segment ventro-lateral of the periproct. It straddles the junction of two interambulacral plates, indicating that it appeared in maturity and did not degenerate to this condition. H. L. Clark (1917) also characterized Hypselaster by the possession of only two genital pores: Proraster has four. This difference is not considered to be sufficient to merit generic separation. Lambert’s Proraster ranges from the Cenomanian to Senonian, whilst species referred to Hypselaster by H. L. Clark (1917) and Mortensen (1951) are all living species. Mortensen (1951, p. 313) tentatively placed H. perplexus Arnold and Clark (1927) in Hypselaster; this species is from the Eocene (?) of Jamaica. Fig. 11. Proraster jukesw (Gray 1851), AM J6625, from Roebuck Bay, Broome, Western Australia: A, aboral view; B, adoral view; C, lateral view, all x1. Proraster jukesiz (Gray 1851) (Figs 11A-C, 12A) 1851 Schizaster jukesi Gray, p. 133 1855 Schizaster jukesi Gray, p. 61, Pl. 3, fig. 4 1925 Hypselaster fragzles Clark, p. 208, Pl. 11, figs 1-3 1938 Hypselaster dolosus Clark, p. 430, Pl. 28, figs 4-7 1946 Hypselaster dolosus Clark; Clark, p. 367 1951 Hypselaster dolosus Clark; Mortensen, pp. 319-320, Pl. 32, fig. 6 Proc. Linn. Soc. N.S.W., 104 (2), (1979) 1980 144 LIVING AUSTRALIAN SCHIZASTERID ECHINOIDS 1951 Hypselaster jukesa (Gray) ; Mortensen, pp. 315-319, Pl. 22, figs 14-17, Pl. 52, figs 2, 9, 21, 22 1961 Hypselaster yukesa (Gray) ; Endean, p. 294 1972 Hypselaster jukesit (Gray) ; A. M. Clarke & Rowe, p. 167, footnote 16. Type specomen. The specimen figured by Gray (1855, Pl. 3, fig. 4) and identified and figured by Mortensen (1951, p. 318, Pl. 22, figs 15-17) and in the collections of the British Museum (Natural History) . It is from “Cape York”. Localities. Mortensen (1951, p. 316) gave the geographic range of P. jukeszz as “from the Torres Strait region to the Queensland coast (Bowen)”’. H. L. Clark’s “H. dolosus” was based on specimens from Broome and Augustus Island, Western Australia. Six specimens studied in this paper were collected by Clark from tidal falts at Roebuck Bay, Broome. Endean (1961, p. 294) records two specimens from Myora, Moreton Bay and four from Dunwich, Moreton Bay. These were taken at L.W.N. from sand flats. Remarks. H. L. Clark (1946, p. 367) distinguished his Western Australian specimens from those from eastern Australia by the position of the apical system, which he considered to be slightly posterior of centre in the Western Australian form P. “dolosus” but anterior of centre in P. jukeszz, and by differences in petaloid area and shape of the valve of the globiferous pedicellariae. Mortensen (1951, p. 318) further suggested that P. “dolosus” has narrower posterior paired petals than P. jukeszz. A. M. Clarke and Rowe (1971, p. 167, footnote 16) have pointed out that neither of these supposed differences in test character is borne out by Mortensen’s (1951, Pl. 22) illustrations of the species. We therefore follow these authors in placing dolosus in synonymy with jukeszz. Fig. 12. Labrum and adjoining ambulacral plates of, A, Proraster jukesez (Gray 1851), AM J6625, from Roebuck Bay, Broome, Western Australia, x2.5; B, Mozra lethe Mortensen 1930, QM G12093, from Moreton Bay, Queensland. Globiferous pedicellariae are not common in P. jukeszz. A Western Australian specimen shows the pedicellariae to have two teeth at the distal end as is typical. However, in comparison with Mortensen’s illustration (Pl. 52, fig. 21) of a globiferous pedicellaria of P. jukeszd, the Western Australian specimen has valves which are relatively longer. However, this is judged to be insufficient grounds to warrant the separation of the two forms as different species. Genus MOIRA Agassiz 1872 Type species. Spatangus atropos Lamarck 1816, p. 32. By subsequent designation of the International Commission of Zoological Nomenclature ; Opinion 209, 1948. Mozrra lethe Mortensen 1930 (Figs 12B, 13A-D) 1926 Mozra stygia Lutken, Clark, p. 191 1930 Mozra lethe Mortensen, p. 392, Pl. 3, figs 1-4 Proc. Linn. Soc. N.S.W., 104 (2), (1979) 1980 K. J. McNAMARA AND G. M. PHILIP 145 1938 Mozra stygza Lutken, Clark, p. 432 1946 Mozra stygza Lutken, Clark, p. 369 1951 Mozra lethe Mortensen; Mortensen, pp. 334-335, Pl. 19, figs 12, 18, 22; PI. 55, figs 12, 24. Localitzes. Mortensen (1951, pp. 334-335) records this species from Bowen, Queensland; “Liverpool, (!) N.S.W.”; Broome, Western Australia; and South Australia. Specimens have also been found by one of us (K. J. McN.) on the eastern side of Bribie Island, Queensland and at Myora, Moreton Bay, Queensland. It is also known from Albany, Western Australia and from Port Phillip Bay, Victoria (A. M. Clarke, 1966, p. 292). Fig. 13. Mozra lethe Mortensen 1930, QM G12092, from Moreton Bay, Queensland; A, aboral view; B, adoral view; C, lateral view; D, posterior view; all x1. As noted by Mortensen (1951, p. 334) this species is most similar to M. stygza, from which it can be distinguished by the deep, sagittal depression between the periproct and lowest part of the lateroanal fasciole (Fig. 13D), and by its shorter labrum (Fig. 12B). ACKNOWLEDGEMENTS We would like to thank Drs F. W. E. Rowe (Australian Museum, Sydney, AM), L. Cannon, (Queensland Museum, Brisbane, QM), Mrs L. Marsh (Western Australian Museum, WAM) and Dr R. Woolacott (Museum of Comparative Zoology, Harvard, MCZ) who loaned the material on which much of this study was based; Dr E. Frankel (University of: Sydney) who also provided material; and Professor W. Stephenson and Dr R. Endean (University of Queensland) for supplying information on specimens collected by them. Our work on Australian Cainozoic echinoids is supported by the Australian Research Grants Committee. References Acassiz. L., 1836. — Prodrome d’une Monographie des Radiaires ou Echinodermes. Mém. Soc. Scz. nat. Neuchatel. I: 168-199. ARNOLD, B. W., and Crark, H. L., 1927. — Jamaican fossil echini: with descriptions of new species of Cainozoioc Echinoidea by H. L. Hawkins. Mem. Mus. comp. Zool. Harv. 50(1) : 1-84. CHESTER, R. H., 1966. — Redescription of the echinoid species Paraster floridienses (Spatangoida: Schizasteridae). Bull. Mar. Scz. 16: 1-19. Ciark, H. L., 1917. — Hawaiian and other Pacific Echini. Spatangina. Mem. Mus. comp. Zool. Harv. 46 (2) : 81-283. —— 1921. — The echinoderm fauna of Torres Strait. Publ. Carneg. Instn 10 (214) : 1-244. —— 1925. — A catalogue of the Recent Sea Urchins (Echinozdea) in the collection of the Bretesh Museum (Natural History). London: British Museum (Nat. Hist.). —— 1926. — Notes on a collection of echinoderms from the Australian Museum. Rec. Aust Mus. 15: 183- WY —— 1932. — Echinoderma (other than Asteroidea) of the Great Barrier Reef Expedition, 1928-1929. Scient. Rep. Gt. Barrier Reef Exped. Proc. Linn. Soc. N.S.W., 104 (2), (1979) 1980 146 LIVING AUSTRALIAN SCHIZASTERID ECHINOIDS —— 1938. — Echinoderms from Australia. Mem. Mus. comp. Zool. Harv. 55: 1-597. —— 1946. — The echinoderm fauna of Australia. Its composition and its origin. Publ. Carneg. Instn 566: 1-567. CLARKE, A. M., 1966. — The Port Phillip Survey 1957-1963. Echinodermata. Mem. nat. Mus. Vict. 27: 284-384. ——, and Rowe, F. W. E., 1971. — Monograph of shallow water Indo- West Pacific echinoderms. London: British Museum (Nat. Hist.). Cooke, C. W., 1942. Cenozoic irregular echinoids of eastern United States. J. Paleontol. 16: 1-62. Correau, G., 1883. — Echinides j jurassiques, crétacés et €océnes du Sud-Ouest de la France. Ann. Soc. Sct. nat. Gharente: -Inférieure 19: 45-253. —— 1885-1889. — Paléontologie frangaise. Terrain Tertzaire I. Echinides Eocénes. 672 pp. Paris. CurRIE, E., 1925. — The collection of fossils and rocks from Somaliland. Part 5, Jurassic and Eocene Benimeidest Monogr. geol. Dept. Hunter. Mus. 46-76. Duncan, P. M., and SLapEN, W. P., 1882-1886 — Fossil Echinoidea of Western Sind and the coast of Baluchicern and of the Persian Gulf, from the Tertiary formations. Palaeont. Indica, ser 14, 1 (3) : 1-382. ENDEAN, R., 1961. — Queensland faunistic records. Part VII. Additional records of Echinodermata (excluding Crinoidea). Pap. Dep. Zool. Univ. Qd 1 (13) : 289-298. FIscHER, A. G., 1966. — In Moore, R. C. (ed.), Treatzse on Invertebrate Paleontology, Part U, Echinodermata 3, Asterozoa — Echinozoa. Lawrence, Kansas: University of Kansas Press. FourTAu, R., 1904. — Contribution a l'étude des Echinides vivant dans le Golfe de Suez. Bull. Inst. égypt. ser. 4, 4: 407-446. Gray, J. E., 1825. — An attempt to divide the Echinida, or sea eggs, into natural families. Ann. Phil. 26: 423-431. —— 1851. — Description of some new genera and species of Spatangidae in the British Museum. Ann. Mag. nat. Host. ser 2, 7: 130-134. —— 1855. — Catalogue of the Recent Echinida, or sea eggs, in the collection of the British Museum. Part I — Echinida Irregularza: 1-69. London: British Museum. HENDERSON, R. A., 1975. — Cenozoic spatangoid echinoids from New Zealand. Palaeont. Bull. N.Z. 46: 1- 90. KerMACK, K. A., 1954. — A biometrical study of Mzcraster coranguinum and M. senonensis. Phil. Trans. R. Soc. Lond. B, 237: 375-428. Kier, P. M., 1957. — Tertiary Echinoidea from British Somaliland. J. Paleontol. 31: 839-902. —— 1975. — The echinoids of Carrie Bow Cay, Belize. Smzthson. Contrib. Zool. 206: 1-45. KogHer, R., 1914. — Echinides du Musée Indien a Calcutta. I. Spatangides. Calcutta: Indian Museum. LAMARCK, J.-B. de, 1816. — Histozre naturelle des animaux sans vertébres. III (Echinides) : 1-59. Paris: Verdiére. LaMBERT, J., and Turéry, P., 1909-1925. — Essaz de nortentlature raisonnée des Echinides. Chaumont: Ferriere. McNamara, K. J., and Purp, G. M., 1980. — Australian Tertiary schizasterid echinoids. Alcheringa 4: 47-65. Mor TENsEN, T., 1930. — Some new Japanese echinoids. Annot. zool. jap. 12 (2) : 387-404. —— 1951. — A monograph of the Echinoidea 5 (2) , Spatangoidea II. Copenhagen: Reitzel. NicHois, D., 1959. — Changes in the Chalk heart-urchin Micraster interpreted in relation to living forms. Phil. Trans. R. Soc Lond. B, 242: 347-437. PomEL, A. 1869. — Revue des Echinodermes et de leur classification pour servir d’introduction a l’étude des fossiles. Paris: Deyrolle. STEPHENSON, W., Cook, S. D., and NEwLaAnps, S. J., 1978. — The macrobenthos of the Middle Banks area of Moreton Bay. Mem. Qd Mus. 18: 185-212. Proc. LINN. Soc. N.S.W., 104 (2), (1979) 1980 Cirral Activity and Feeding in the Lepadomorph Barnacle Lepas pectinata Spengler (Cirripedia) D. T. ANDERSON ANDERSON, D. T. Cirral activity and feeding in the lepadomorph barnacle Lepas pectinata Spengler (Cirripedia). Proc. Linn. Soc. N.S.W. 104 (2), (1979) 1980: 147-159. Among the lepadids, L. pectinata shows extreme adaptation to neustonic life, as a small species inhabiting fragile, ephemeral objects at or near the water surface. In addition to feeding by cirral extension on small macroplankton, L. pectznata employs rhythmic cirral beating in continuous feeding on microplankton. The form and setation of the cirri and mouthparts are adapted to these dual modes of feeding. The rhythmic cirral activity of L. pectznata is in the opposite mode to that of balanoids, the cirri being held extended between beats, and is similar in general to that of Verruca stroemza. All three patterns of cirral activity have evolved independently, those of L. pectinata and V. stroemza being convergent, associated with feeding on micro- plankton. Other features of adaptation of L. pectznata to its mode of life are discussed. They include, in addition to continuous versatile feeding on small food organisms in the top few centimetres of the water, a rapid growth rate, onset of sexual maturity and reproduction at a small size, insensitivity of the cirri to light, water movements or contact stimulation, production of specialized flotatory nauplii, settlement of cyprids gregariously on planktonic objects and a precocious post-settlement metamorphosis. D. T. Anderson, School of Biological Sciences, University of Sydney, Australia 2006; manuscript received 29 October 1979, accepted for publication 20 February 1980. INTRODUCTION Although lepadid barnacles are well known taxonomically (Darwin, 1851; Nilsson-Cantell, 1921; Stubbings, 1963; Zullo, 1963; Utinomi, 1968; Newman, 1972; Arnaud, 1973; Foster, 1978), only a few scattered reports have been given of their feeding activities. In general, these place emphasis on prolonged cirral extension and macrophagy (Gruvel, 1893; Howard and Scott, 1959; Patel, 1959; Bieri, 1966; Crisp, 1967; Jones, 1968; Lockwood, 1968; Cheng and Lewin, 1976), with some intimation of cooperative feeding on larger prey. The obvious and prolonged extension of the cirri in Lepas species is also attested by the many photographs in elementary textbooks and popular accounts of marine animals, showing Lepas with its cirri fully exposed. No other cirripede behaves so readily in this way. Lepas is often said to be a generalized thoracican genus, but all aspects of its biology are indicative of specialization for a neustonic mode of life. This specialization is nowhere more evident that in the small L. pectinata of tropical and warm temperate waters, a species whose cirral activity and feeding have hitherto been undescribed. L. pectinata preferentially attaches to a variety of small, fragile floating objects such as cuttle bones, feathers, sargassum, pumice and tar (Darwin, 1851; Horn, Teal and Backus, 1970; Lang, 1979). The present paper analyses the cirral activity of L. pectinata in relation to cirral and mouthpart anatomy and offers some comparisons with feeding in other species of the genus in the same neustonic habitat. MATERIALS AND METHODS Living specimens of L. pectznata attached to a cuttlefish shell were collected by Mr M. J. Moran at Cape Banks, Botany Bay, N.S.W. in October, 1978. The animals Proc. Linn. Soc. N.S.W., 104 (2), (1979) 1980 148 LEPAS PECTINATA were maintained in an aerated aquarium tank at the University of Sydney. Cinematographic records of cirral activity and details of anatomical structure were obtained by methods described in previous papers (Anderson, 1978, 1980a). Anatomical details were determined from specimens preserved in 5% formalin in sea water, dissected, and examined by both bright field and dark field microscopy of unstained material. Records of cirral movements were made _ by cinephotomacrography, using Kodak Ektachrome 160 super 8 mm film, and analysed using a Eumig R2000 analysing projector. No food was provided for the living L. pectinata during the two weeks that they were kept alive in the tank, but the water was renewed every three days. After 10 days in the tank, some of the animals released large numbers of nauplius larvae, on which the captive population proceeded to feed. It was notable, however, that the level and pattern of activity was no greater when nauplii were present than it had been in the absence of obvious food organisms. Since all of the animals in the tank retained their vigour throughout the two weeks of observation, it was presumed that they were able to feed microphagously on naturally occurring microscopic organisms in the water. As will be shown below, the cirral and mouthpart morphology, the mode of cirral activity and the gut contents bear out the fact that L. pectinata is both a microphagous and macrophagous feeder in the neuston. OBSERVATIONS General External Anatomy. The general external anatomy of L. pectznata is well known: (Darwin, 1851; Foster, 1978) and only certain aspects will be emphasized here. The species is the smallest in the genus Lepas, with individuals rarely exceeding 12 mm in length. The grey-coloured capitular plates (Fig. 1A) are thin and deeply cupped, with closely approximated margins. The distinctive ridging on the plates and Fig. 1. A. — The carapace plates of L. pectinata; interior view of the left scutum, left tergum and carina. B. — L. pectinata, viewed from the right side, with the right valve removed. ad, adductor scutorum; c, carina; fa, filamentary appendage; p, peduncle; pm, peduncular muscle; sc, scutum; te, tergum. Proc. Linn. Soc. N.S.W., 104 (2), (1979) 1980 D. T. ANDERSON 149 the positions of the umbones reveal the specialized growth pattern which yields the globose, lightweight valves. The capitulum is also large relative to the peduncle, which is short (Fig. 1B), cone shaped, thin walled and muscular. The yellowish covering of the peduncle is irregularly annulated but otherwise smooth and not setose. Longitudinal muscle strands are conspicuous beneath the peduncular cuticle in preserved specimens, fanning out into the mantle beneath the basal margin of the scutum of each side (Fig. 1B). Within the capitular valves, the body of the animal is relatively large, almost completely filling the mantle cavity when in the retracted position with the cirri curled (Fig. 1B). The prosoma is swollen and thin walled, with the musculature and other internal organs clearly visible through the cuticle. The oral cone is large and the thorax well developed. The cirri are of moderate length, but strongly formed for the size of the animal. The first pair is set quite close to the second pair on either side of the posterior end of the oral cone (see also Fig. 4A). In contrast to the relatively large size of the body, the adductor scutorum muscle is quite small (Figs 1A and 1B). It lies close to the occludent margins of the scuta, approximately at the midpoint of the length of these margins. The aperture, which lies apical to the adductor scutorum, thus occupies only the apical half of the rostral surface of the capitulum (Fig. 4B). When extended, the body and limb bases of the animal fill the aperture. When withdrawn, the coiled limbs are only just confined within the aperture. As will be shown below, the large body, small adductor, small aperture and restricted mantle cavity of L. pectznata are associated with a mode of life in which the animal spends most of its time with the body and limbs extended in the water and only occasionally retracts within the shell. The contrast between the bold exposure of the limbs in living L. pectznata and the fugitive retreat of most barnacles into the mantle cavity at the slightest provocation is perhaps the most striking indication of the adaptation of L. pectznata to a highly specialized mode of neustonic life. Anatomy of the Czrrz. As in all species of Lepas, cirrus I in L. pectiznata shows substantial modification as a maxilliped. Cirrus II is partially modified anatomically for this function and the remaining cirri (III-VI) show a more generalized form. In the following description, setal directions refer to the position of the limbs when the animal is withdrawn into the mantle cavity asin Fig. 1B. Cirrus I (Figs 2A and 2B) has moderately short, subequal rami, the exopod having 11 or 12 podomeres, the endopod 9. Apart from the terminal few, the podomeres of both rami are short and broad. Setation is sparse on the lateral surfaces, being confined to a few setae on the distal margins of the podomeres, but dense on the median surfaces of both rami. On the exopod, the median setae of the distal five podomeres arise at the distal margins of the podomeres, point distally and are simple setae. On the remaining podomeres, dense brushes of long, thin, serrate setae arise from the posteromedian surfaces and point posterodistally. On the endopod, dense brushes of similar long, thin serrate setae arise from the median surfaces of the podomeres and point anteriorly, intermeshing with the median setae of the exopod. Little setation occurs on the protopod except for a bunch of long, distally directed setae distally on the median surface. Cirrus II (Figs 2C and 2D) has longer, more cylindrical rami than cirrus I, the exopod and endopod being almost equal in length, with 12 and 14 podomeres respectively. As in cirrus I, lateral setation is sparse and median setation dense, especially on the proximal half of each ramus. These median setae are a mixture of simple and serrate, long, thin setae all pointing anteriorly and overlapping with the median setae of cirrus I. Proc. LINN. Soc. N.S.W., 104 (2), (1979) 1980 150 LEPAS PECTINATA \\ S a6 Ms AYN, \ aN AN RS te ZX \ EE PIES ff 2 a (NG Gage = KX) mm RO SS ce CBA \ WY AS ATS ee \ Ni VX ees li) aN jie Gal a Sey Se SSS i | lt ff fee ~ Fig. 2. L. pectenata. A. — Cirrus I, right lateral view. B. — Cirrus I, left, median view. C. — Cirrus II, right, lateral view. D. — cirrus II, left, median view. E. — Cirrus III, right, lateral view. F. — Podomere 10 of exopod of right cirrus III, lateral view. G. — Podomere 10 of exopod of left cirrus III, median view. Proc. LINN. Soc. N.S.W., 104 (2), (1979) 1980 D. T. ANDERSON 151 The remaining cirri, III-VI, all have long cylindrical rami. Podomere numbers for the exopod and endopod are 18/20, 19/21 and 22/19 respectively (Figs 2E and 3A). Each podomere carries 6 pairs of setae anteriorly, the distal 3 pairs being long (Figs 2F and 2G), and a group of short setae posteriorly on the distal margin. Most of the setae are simple, but serrate setae occur amongst them on the more proximal podomeres of the limbs. The long anterior setae of cirri III-VI are about 0.75 mm in length, but when the cirral rami are spread in the extended position shown in Fig. 4, the setae do not meet across the spaces between the distal parts of the rami. Anatomy of the Mouthparts. The oral cone of L. pectznata (Fig. 3B) is large and prominent. The bullate labrum is densely setose around the entrance of the preoral cavity, the setation being continued along the posteromedian margins of the mandibular palps (Fig. 3D). Mandibles, maxillules and maxillae are in the usual array, but their masticatory margins show prominent setation and only moderate Wa ON f} y Ky LK, | ay. TILL’ al aa’ Bur cam AWA " h \ \ Imm SS Ry as BH Me £2 tae wand Z|) LOE CTT Mf Why Yj jy Vor Ys Lif) ly Yi Fig. 3. L. pectinata. A. — Cirrus IV, left median view. B. — Oral cone, posterior view. Cue Right mandible, lateral view. D. — Right mandibular palp, lateral view. E. — Right maxillule, lateral view. F. — Right maxilla, lateral view. mb, mandible; mp, mandibular palp; mx, maxillule; mxa, maxilla. Proc. Linn. Soc. N.S.W., 104 (2), (1979) 1980 152 LEPAS PECTINATA spination. The mandible (Fig. 3C) has 5 teeth, but the incisor tooth is modest and the molar process is small. The maxillule (Fig. 3E) shows only vestigial stepping of the margin, small cutting blades on the lateral angle and short spines on the median angle. The maxilla (Fig. 3F) is a convex lobe with many fine, anteriorly directed setae on the free margin. These mouthparts, while retaining the capacity for maceration of small prey, are also indicative of an ability to retain and process fine particulate food (compare Semzbalanus balanotdes and Verruca stroemza; Stubbings, 1975; Anderson, 1980a). Cirral Activity. The most striking feature of the cirral activity of L. pectznata is that the animals are active continuously. The group of individuals observed in the present study showed no break in activity during two weeks. Even in the brief periods when the animals were removed from the aquarium in order to change the water, cirral exposure and movements of the peduncle continued. Activity was maintained in all conditions of illumination, being unaffected by bright light, darkness, or changes of illumination. No shadow reflex could be elicited. Activity was unaffected by water Fig. 4. L. pectinata, with cirri fully extended. A. — Ventral view. B. — Lateral view. Proc. Linn. Soc. N.S.W., 104 (2), (1979) 1980 D. T. ANDERSON 153 movements or by reversing the orientation of the animals relative to the water surface. Animals attached on both sides of the cuttle bone and around its margin continued their activity regardless of orientation. Activity was also unaffected by contact with the water surface. Submerged individuals swept the water with their cirri. Individuals at the water surface swept the surface, with some cirral rami projecting above the surface. A sharp percussive vibration of the aquarium caused the animals to react by sudden withdrawal into the shell, but only momentarily. The shell valves reopened and the cirri emerged again in a few seconds. In general, the activity of L. pectinata at or just under the water surface is one of continuous feeding and low sensitivity to environmental disturbance. The activity expressed by the animals involves two elements. One is swaying of the capitulum on the short peduncle, both from side to side and back and forth, slowly swinging the extended cirral net about in the water. This swaying action tends to be self sustaining within a group of individuals, in that movement of one causes contact with adjacent animals and elicits movement by them. The second and more vigorous element of activity in L. pectznata is rhythmic cirral extension and withdrawal. The extended position is the normal one for this species. In it, the body is straightened and protruded through the aperture to the level of the oral cone (Fig. 4). Cirri IV-VI stand upright as a fan at the carinal end of the aperture, with cirrus III adjacently upright on either side in a carinolateral position. Fig. 5. A - E. — Representative cirral positions during a typical sequence of limb extension and withdrawal in L. pectznata, seen in lateral view. The total sequence occupies 1.28 s. A. — Position at the beginning of the sequence B. — 0.28 s from the beginning of the sequence C. — 0.5s D. — 0.72s E. — 0.945 F. — 1.28s Proc. Linn. Soc. N.S.W., 104 (2), (1979) 1980 154 LEPAS PECTINATA Cirrus II on either side has its rami directed forwards above the oral cone, and cirrus I similarly projects forwards on either side of the oral cone. From the extended position, the animal makes a regular movement (Fig. 5) of withdrawal of the cirri followed by extension. In the withdrawal movement, the body swings downwards and forwards on the axis of the adductor muscle. The first two pairs of cirri are drawn down into the mantle cavity. Cirri III-VI are folded together and curled forwards, but not completely withdrawn into the mantle cavity. After a short pause, the cirri and body are extended again. The long cirri first uncurl, then extend and spread, accompanied by unfolding and protrusion of cirrus I and II on either side. Frame by frame analysis of cinematographic records (Fig. 6) shows that the timing of the withdrawal-extension sequence varies little among individuals. At 22 - 23°C,, observations of 3 individuals performing a total of 70 beats gave an average cirral withdrawal time of 0.28 - 0.30s, followed by a pause of 0.17 - 0.37 s and a cirral protrusion time of 0.36 - 0.40 s. The slight difference in duration between withdrawal and extension of the cirri reflects, as is usual with thoracican barnacles, the faster muscular contraction and slower hydraulic action of the two movements. The range of variation in the duration of the pause with the cirri withdrawn is correlated with the rate of cirral beating in different individuals. At higher rates of beat, the pause in the withdrawn position is of shorter duration, but it was not observed to be greater than 0.37 s even when the rate of beat was markedly slow. The factors determining the rate of beat are obscure. General observation showed that adjacent individuals in the group under study exhibited different rates of beat. Counts were made for 11 individuals recorded simultaneously on film. The number of beats performed per 10 s by these animals were 0.2, 0.8, 1.7, 2.0, 2.4, 4.75, 5.0, 5.0, 5.9, 7.25 and 7.6 respectively. The range was thus from one beat every 50 s to one every 1.3 s, with corresponding intervals of cirral extension of 49 s and 0.6 s respectively, slight differences in timing being evident from beat to beat. The two 1 2 3 4 5 6 7 8 9 10 1 12 13 TIME -SECONDS Fig. 6. Record of cirral extension and withdrawal in two individuals of L. pectinata in still water at 22- 23°C. Vertical axis: E. limbs extended, W. limbs withdrawn. A. — An individual beating at 5 per 10s. B. — An individual beating at 1.7 per 10s. Proc. Linn. Soc. N.S.W., 104 (2), (1979) 1980 D. T. ANDERSON 155 examples given in Fig. 6 show rates of 5.0 and 1.7 beats per 10 s, with average interbeat durations of 1.3 s and 8.4 s respectively. In spite of these variations in the rate of beat, the withdrawal - extension action is the same in all individuals. On withdrawal, the cirri curl down through the water, collecting suspended particulate matter. During the pause before re-extension, the coiled cirri show movements indicative of cleaning off by the maxillipeds and mouthparts. The cirri are then extended again, preparatory to the next sweep. When the cirri were extended in water containing nauplii, individual cirral rami were seen to curl forwards and down to be cleaned off by apposition of the second pair of cirri. These limbs were then bent downwards between the first pair of cirri, rubbed together and drawn back. Finally, the endopods of the first pair of cirri were brought together in the midline above the mouthparts and rubbed one upon the other. By this means, the small captured prey are presumably transferred to the mouthparts for ingestion. Contact of the extended cirri with a larger object such as the end of a pencil elicited a strong grasping action by all the cirri together. L. pectinata appears to be able to feed by the capture of larger prey, as well as on small prey and particulate matter. In order to determine the food intake resulting from these movements, the gut contents of five of the captive individuals were examined. Three categories of food were found in abundance, phytoplankton, nauplii and fragments of adult exuviae. It can be concluded that L. pectznata is able to feed, by its rhythmic cirral action, its individual ramal action and the grasping closure of the cirral net, on microplankton and small macroplankton. Little or no selective discrimination of food intake appears to occur, and feeding is continuous at or just below the water surface day and night, irrespective of water movements. DISCUSSION Feeding in Lepadids. Prior to the present study, information on cirral activity in Lepas was available for L. anatifera (Gruvel, 1893; Southward, 1957; Howard and Scott, 1959; Crisp and Southward, 1961; Crisp, 1967), L. anserifera, (Bieri, 1966; Jones, 1968), L. fasctcularts (Crisp, 1967; Cheng and Lewin, 1976) and L. pacifica (Cheng and Lewin, 1976). All accounts emphasize a number of common features of lepadid cirral activity. The cirri are held extended for long periods in either still or moving water and are swept through the water by vigorous muscular contractions of the peduncle. On contact with animal food and the stimulus of certain amino-acids and ions (Crisp, 1967), the cirri make two types of response. If the prey is small, contacting a single cirrus, the contacted cirrus curls down, capturing the prey and conveying it to the maxillipeds, thence to the mouthparts. If the prey is large, the cirral net curls as a whole to grasp the food and hold it against the mouthparts. Large prey grasped in this way may be held for up to two hours before the remains are released. As the present study has shown, L. pectznata retains these two feeding responses in spite of its small adult size. The responses are basically like those of scalpellids (Batham, 1946; Barnes and Reese, 1959; Howard and Scott, 1959) but are associated in lepadids with a number of specializations related to the floating neustonic habit. These include prolonged cirral extension in still water, active sweeping by peduncular contractions, and insensitivity to illuminations, water movements or contact stimulation, all of which combine to result in the vigorous capture of small or large planktonic prey. These feeding adaptations are further combined with lightweight, globose capitular valves, a specialized growth pattern, fast Proc. Linn. Soc. N.S.W., 104 (2), (1979) 1980 156 LEPAS PECTINATA rates of growth (Darwin, 1851; Annandale, 1909b; Evans, 1958; Skerman, 1958), rapid attainment of sexual maturity, flotatory specializations during naupliar development (Bainbridge and Roskell, 1966; Lang, 1979), planktonic searching for floating substrata by cyprids, highly gregarious settlement and, in L. pectinata (personal observation), a precocious development of the adult organization post- settlement. An account of the latter phenomenon will be given elsewhere. Without doubt, lepadids are highly specialized among the Lepadomorpha for the catch-as- catch-can inhabitation of floating objects in an opportunistic manner. The carnivorous propensities of lepadids in this environment are well documented in direct observations on their feeding habits. Howard and Scott (1959) fed L. anatifera on Artemza and Tigriopus, and observed polychaetes, amphipods, carids, gastropods, bivalves and pycnogonids in the guts of field-collected specimens. Patel (1959) and Crisp (1976) fed the same species on pieces of Mytzlus tissue, which were grasped by the cirral net and engulfed in the manner first described by Gruvel (1893). Bieri (1966) and Jones (1968) have shown that L. anserifera is even more active as a carnivore, feeding on whole Vellela, pieces of Physalia tentacle and pieces of fish and squid. Bieri gave evidence that this species can feed cooperatively, passing a Vellela from one individual to the next. L. fascicularis has also been observed to eat Vellela (Bieri, 1966) and pieces of Mytzlus tissue (Crisp, 1967). In the natural habitat, it is clear that macrozooplankton is the major food source for the larger Lepas species. Anatomical descriptions of the mouthparts of L. anatifera, L. anserifera and L. fascicularis support this conclusion. The comparative anatomy of the cirri and mouthparts further indicates a similar diet of macrozooplankton for other lepadids of the same oceanic habitat, L. testudznata, L. australis, L. pacifica, Conchoderma virgatum and C. auritum (e.g. Hoek, 1907; Nilsson-Cantell, 1921; Petriconi, 1969; Foster, 1978). Powerful mandibles with strong cutting teeth and a prominent molar process, heavily built maxillules with a large cutting spine on the lateral angle, a sequence of setose steps along the cutting edge and a group of strong spines in the median angle, and a strong spinose development of the maxillae, are features of these species. L. pectinata retains these features on a smaller scale, but the cutting masticatory processes of the mouthparts are relatively reduced and the mouthparts, mandibular palps and labrum carry many fine setae. This is indicative of an ability to collect and ingest particulate material gathered by the cirri, a fact confirmed by analysis of gut contents. L. pectinata feeds on small macroplankton by the usual two lepadid methods, but also takes in substantial quantities of microplankton. Rhythmic Cirral Activity in L. pectinata. It is in connection with particulate feeding that the rhythmic cirral activity of L. pectznata can be interpreted. Little reference has been made to such activity in other lepadid species. It has been mentioned as occurring occasionally in L. anatifera at a maximum rate of 2.85 contractions per 10 seconds (Southward, 1957) but the pattern and significance of the activity were not described. In L. anatzfera, the rami of cirrus I and the exopod of cirrus II carry dense setation on the median surface, arranged in a pattern similar to that of L. pectznata, but there is no evidence that L. anatifera feeds on particulate material. The maxilliped specialization in this species appears to be related to a grasping function. In L. pectenata, in which every individual maintains a rhythm of cirral contractions, albeit at a wide range of rates among individuals (from 1 per 50s to 1 per 1.3 s in the present study) , the cirral movements gather particulate material from the water and transfer it to the maxillipeds. In addition to the rami of cirrus I and the exopod of cirrus II, the endopod of cirrus II in L. pectznata carries dense, anteriorly pointing setation. Rhythmic feeding on microplankton can therefore be recognized as Proc. LINN. Soc. N.S.W., 104 (2), (1979) 1980 D. T. ANDERSON 157 a third feeding mechanism in this species, with correlated setose arrangements on the mouthparts and two pairs of maxillipeds. The continuous performance of this rhythmic activity, the amount of microscopic material in the gut and the ability of L. pectinata to remain active and healthy in water containing no macroplankton, confirm the importance of particulate feeding in this species. The pattern of rhythmic cirral activity is also different from that well known for various balanomorph species. In particular, the timing is reversed as compared with balanids, the cirri being held extended between beats, with only a brief pause in the contracted position during each beat. In balanids, the cirri are held in the contracted position between beats, with little or no pause in the extended position (Crisp and Southward, 1961; Anderson, 1980b). There is also no indication in L. pectznata that the rhythmic cirral activity drives a current of water through the mantle cavity, as it does in balanids. Indeed, there is very little free space for such a current in the mantle cavity of L. pectznata, though some movement of water across the Wee u amase internal surfaces of the mantle valves must occur at each beat. A comparison of the timing of events between the rhythms of L. pectinata and a representative balanoid, Balanus balanus, emphasizes this contrast and also reveals certain functional constraints in the cirripede cirral mechanism. B. balanus shows rhythmic extension and withdrawal at a rate of 2-5 beats per 10 seconds (Crisp and Southward, 1961). The average duration of the pause between beats, with the cirri withdrawn, is 0.8 - 1.74. During each beat, cirral extension takes 0.75 - 1.25 s and is immediately followed by a faster withdrawal, taking 0.5 - 1.0s. In L. pectznata, the cirri may be held extended up to 50 s between beats, but rates of 4-5 beats per 10 seconds are frequently observed. At this comparable rate, cirral extension in 0.38 - 0.40 is followed by a pause of 1.0 - 1.3 s with the cirri extended. Cirral withdrawal in 0.28 - 0.30 is then followed by a pause of 0.17 - 0.28 s before the cirri are extended again. In both species, cirral extension is slower than cirral withdrawal, a function of the similar hydraulic and muscular mechanisms involved in both cases. Other than this common factor, the rhythms of the two species are performed in entirely different ways. Extension and withdrawal are both faster in L. pectinata than B. balanus. Between extension and withdrawal, the cirri are held in the mantle cavity for a much shorter time in L. pectznata than in B. balanus. Following each extension, the cirri are held extended in L. pectinata for a period equal to or longer than the duration of a beat. In B. balanus, there is no pause in the extended mode. These differences indicate that the rhythmic cirral beating of L. pectznata has evolved independently of that of balanoids, lending further support to the view that it is a special feature of L. pectznata among lepadids. The recent description and analysis (Anderson, 1980a) of rhythmic cirral activity in the verrucid V. stroemza, again evolved independently of balanoid beating, provides a further opportunity for comparison with L. pectinata. In this comparison, the similarities are much greater. V. stroemia, like L. pectinata, performs rhythmic cirral beating at 4-9 beats per 10 seconds, with the cirri held extended between beats. In each beat, the average duration of the withdrawal movement is 0.34 s, little different from that of L. pectinata, and of the extension movement 0.57 s, intermediate between L. pectznata and B. balanus. The average duration of the pause between beats with the cirri extended is 0.90 s in V. stroemza, slightly less than in L. pectinata. On the other hand, there is no pause with the cirri in the withdrawn position in V. ,stroemia. Once withdrawn, they are immediately extended again. Another unique feature of the rhythmic cirral action of V. stroemza is that the long, posterior cirri do not curl forwards during the withdrawal movement. Thus in spite of the general similarity of the rhythmic cirral action of V. stroemza Proc. LINN. Soc. N.S.W., 104 (2), (1979) 1980 158 LEPAS PECTINATA and L. pectznata, the two patterns of action differ fundamentally in the lack of a pause in the withdrawn position in V. stroemza and in the lack of cirral bending. The maxillipeds also spread and close in different ways in the two species. Since all phylogenetic considerations point to the independent evolution of these rhythmic actions as specialized features of these species within their genera, the differences between them are not surprising. What is more remarkable is the convergent similarity that they show as modifications of the prolonged cirral extension with captorial feeding characteristic of lepadids and verrucids respectively. L. pectznata and V. stroemia are both small species adapted to unusual habitats as compared with other members of each genus. L. pectznata preferentially inhabits ephemeral objects at the water surface. V. stroemza is a shallow water species. Both retain captorial feeding on small macroplankton, but both also feed on microplankton. Both have finely setose mouthparts and maxillipeds. Both capture their microplankton by a rhythmic cirral action in which the cirri are held extended between beats. In view of this convergent evolution of similar rhythmic cirral activity in a lepadomorph and a verrucomorph, the possibility of convergent evolution of the balanoid pattern of rhythmic cirral activity on more than one occasion in the Balanomorpha must not be overlooked. ACKNOWLEDGEMENTS This investigation forms part of a study supported by the Australian Research Grants Committee and the University of Sydney. I wish to thank Mr M. J. Moran for the provision of animals and my wife, Joanne, for technical assistance. References ANDERSON, D. T., 1978. — Cirral activity and feeding in the coral-inhabiting barnacle Boscza anglicum (Cirripedia). J. mar. bzol. Ass. U.K. 58:607-626. — , 1980a. — Cirral activity and feeding in the verrucomorph barnacles Verruca recta Aurivillius and V. stroemia (O. F. Miller) (Cirripedia). J. mar. bzol. Ass. U.K. 60 (in press) . ——, 1980b. — Cirral activity and feeding in the balanoid barnacle Balanus perforatus Bruguiére (Cirripedia) (in preparation). ARNAUD, P. M., 1973. — Le genre Lepas Linné 1758, dans les Terres Australes et Antarctiques Frangaises (Cirripedia). Crustaceana 24: 157-162. BAINBRIDGE, V., and RoskELL, J., 1966. — A redescription of the larvae of Lepas fasczcularzs Ellis and Solander with observations on the distribution of Lepas nauplii in the Northeastern Atlantic. Pp. 67- 81 in H. Barnes (ed.), Some contemporary studies in Marine Science. London: Allen and Unwin. Barnes, H. S., and REEsE, E. S., 1959. — Feeding in the pedunculate cirripede, Polliczpes polymerus J. B. Sowerby. Proc. zool. Soc. Lond. 123, 569-585. BaTHaM, E. J., 1945. Pollicipes spinosus Quoy and Gaimard. I. Notes on biology and anatomy of the adult barnacle. Trans. R. Soc. N.Z. 74: 359-374. Bieri, R., 1966. — Feeding preferences and rates of the snail, Janthina prolongata, the barnacle, Lepas anatifera, the nudibranchs, Glaucus atlanticus and Fiona pinnata, and the food web in marine neuston. Publs. Seto mar. biol. Lab. 14: 161-170. CHENG, L., and Lewin, R. A., 1967. — Goose barnacles (Cirripedia: Thoracica) on flotsam beached at La Jolla, California. Feshery Bull. Fish. Wild. Serv. U.S. 74: 212-217. Crisp, D. J. 1967. — Chemoreception in cirripedes. Biol. Bull. mar. biol. Lab. Woods Hole 133: 128-140. ——, and SouTHwarbD, A. J., 1961. — Different types of cirral activity of barnacles. Phil. Trans. R. Soc. B243: 271-308. Darwin, C., 1851. — A monograph on the subclass Cirripedia. The Lepadidae or pedunculate cirripedes. London: Ray Society. Evans, F., 1958. — Growth and maturity of the barnacles Lepas hilli and Lepas anatifera. Nature 182: 1245-1246.9p Foster, B. A., 1978. — The marine fauna of New Zealand: barnacles (Cirripedia Thoracica). N.Z. Oceanogr. Inst. Memoir 69: 1-60. Gruve, A., 1893. — Contribution 4 l'étude des Cirrhipédes. Arch. Zool. exp. gén. 1:401-610. Horn, M. H., TEAL, J. M., and Backus, R. H., 1970. — Petrol lumps on the surface of the sea. Sczence 168: 245-246. Proc. LINN. Soc. N.S.W., 104 (2), (1979) 1980 D. T. ANDERSON 159 Howarp, G. K., and Scott, H. C., 1959. — Predacious feeding in two common gooseneck barnacles. Science 129: 717-718. Jones, E. C., 1968. — Lepas anserifera Linné (Cirripedia Lepadomorpha) feeding on fish and Physalza. Crustaceana 14: 312-313. Lanc, W. H., 1979. — Larval development of shallow water barnacles of the Carolinas (Cirri- pedia: Thoracica) with keys to naupliar stages. N.O.A.A. Tech. Rpt. N.M.F.S. Circular 421. U.S. Dept. Commerce, pp. 1-39. Lockwoop, A. P. M., 1968. — Aspects of the Physiology of Crustacea. Edinburgh: Oliver and Boyd. NEwMaAN W. A., 1972. — Lepadids from the Caroline Islands (Cirripedia Thoracica) . Crustaceana 22: 31- 38. NILssoN-CANTELL, C. A., 1921. — Cirripeden Studien. Zur Kenntnis der Biologie, Anatomie und Systematik dieser Gruppe. Zool. Bédrag, Uppsala 7: 75-395. PaTeEL, B., 1959. — The influence of temperature on the reproduction and moulting of Lepas anatifera L. under laboratory conditions. J. mar. bzol. Ass. U.K. 38: 589-597. PETRICONI, V., 1969. — Vergleichend anatomische Untersuchungen an Rankenfussern. I. Die mundwerkzuege von Lepas anatifera (L). Zool. Jb. Anat. Ont. 86: 67-83. SKERMAN, T. M., 1958. — Rates of growth in two species of Lepas (Cirripedia). N.Z. Ji. Scz. 1: 402-411. SOUTHWARD A. J., 1957. — On the behaviour of barnacles. III. Further observations on the influence of temperature and age on cirral activity. J. mar. bzol. Ass. U.K. 36: 323-334. SrupBincs, H. G., 1963. — Cirripedia of the tropical South Atlantic coast of Africa. Res. Scz. Exped. oceanogr. Belg. Eaux Cot. Afr. Atlant. Sud. 3(10) : 1-39. — , 1975. — Balanus balanotdes. L.M.B.C. Memoir No. 37. Liverpool: University Press. Utinomi, H. 1968. — Pelagic, shelf and shallow water Cirripedia from the Indo-West Pacific. Vidensk, Meddr. dansk. naturh. Foren. 131: 161-186. ZuLLO, V. A., 1963. — A preliminary report on systematics and distribution of barnacles (Cirripedia) the Cape Cod region. Publ. Maz. Biol. Lab. Woods Hole. 33pp. Proc. Linn. Soc. N.S.W., 104 (2), (1979) 1980 Annexure to Proceedings. Volume 104 THE LINNEAN SOCIETY OF NEW SOUTH WALES RECORD OF THE ANNUAL GENERAL MEETING, 1979 The one hundred and fourth Annual General Meeting was held in the Science Centre, 35 Clarence Street, Sydney on Wednesday, 28th March 1979 at 7.30p.m. The President, Mr J. T. Waterhouse, occupied the Chair. The minutes of the one hundred and third Annual General Meeting 29th March 1978 were read and confirmed. REPORT ON THE AFFAIRS OF THE SOCIETY FOR THE YEAR 1978-9 Publications Following advice in February 1978 from the Australasian Medical Publishing Company, our printer since 1925, that other commitments would prevent its handling the Proceedings beyond vol. 102, part 3, the Society was faced with an urgent need to find another printer. At this time also, we were seeking ways of improving the format of our Proceedzngs as well as reducing the burdensome costs of editing and printing. To give effect to our plans, Professor T. G. Vallance has taken over as Honorary Editor from Part 1 of Volume 103 and the changes forecast in last year’s Annual Report are being implemented. We are considerably in Professor Vallance’s debt. We are pleased to report that manuscripts are coming in at a steady rate and copy is now in the hands of our new printers, Southwood Press Pty Limited, of Marrickville. Volume 102, Part 3 of the Proceedings was published on July 5th. Membership During the year, 10 new members were elected to the Society, 6 resigned and one died. At 1st March, 1979 the membership was made up of 258 Ordinary Members, 26 Life Members and 6 Corresponding Members, making a total of 289. Council noted with regret the death in May of Mr H. K. Judd. Howard Judd was elected to the Society in 1960. At the time of his election he had just taken on the position of Custodian and Ranger of the Minnamurra Falls Forest Reserve, Jamberoo, a relict pocket of rain forest in the Illawarra that he himself had been the prime initiator in having conserved. Although this reserve is small it is extremely important floristically as a sample of the once more-widespread southern rain-forests, and natural historians will be forever indebted to Howard Judd for its conservation. He was by training a marine wireless operator and for some time was in charge of an army training school in this field. He became an amateur natural historian not only well-informed on his premier interest, the botany of rain-forests, but also knowledgeable on the local fauna and geology. Many of us have found him an enthusiastic and valued guide in the Jamberoo area and his loss will indeed be felt. In September, Emeritus Professor I. A: Watson was elected to Corresponding Membership of the Society in recognition of his distinguished contribution to Science and to the Society over many years. Council had decided to recognize a new category of membership to be known as “Associate Membership”, suitable for students and others who do not wish to be full members. Associate Members would be invited to participate in all activities and benefits of the Society except voting and receiving the Proceedings, and would be liable for a smaller fee than full members ($4.00 in 1979). Meetings Our activities during the year included one Special General Meeting of Members to discuss the Society’s financial position and relationship with Science House Pty Ltd, three Ordinary General Meetings and three Field Excursions. None of these meetings was as well attended as we should have liked, but all were very rewarding for those who did come. At the first of the Ordinary General Meetings in May, Dr D. H. Ashton of the School of Botany at Melbourne University spoke about “The Vegetation of Chile”. In June at a joint meeting with the Australian Museum Society, Professor Gordon Craig, James Hutton Professor of Geology at the University of Edinburgh, gave an address on “The Lost Illustrations of James Hutton for The Theory of the Earth (1795)”. On September 3rd a Field Day was held at the Kurnell Peninsula to visit the aboriginal middens and examine the vegetation and the mud flats. In October a Field Day was held at Agnes Banks to examine the Castlereagh State Forest and the effects of sand mining. Another Field Trip visited Lake Illawarra in November to explore problems involved in the management of the lake. More recently, on 14th March, 1979, we joined the Australian Systematic Botany Society to hear an address by Mr H. B. Carter (Hons. Banksian Archivist, British Museum (Nat. Hist.)) on “Sir Joseph Banks”. Newsletter The LINN SOC NEWS has continued to be printed quarterly, giving details of coming meetings, reports of resolutions from the Council meetings and other items of interest to members. Linnean Macleay Fellowship Mrs Jennifer Anderson completed her third and final year as a Linnean Macleay Fellow at the University of New South Wales, studying the biology of two species of Australian Coccinellidae, Scymnodes liudigaster (Mulsant) and Lepthothea galbula (Mulsant). During the year her experimental studies of the reproductive and diapause physiology of L. galbula and an ecological programme involving population monitoring, determination of voltinism, sex ratios and seasonal developmental cycles in both species, was completed. She is now a tutor in the School of Zoology, University of New South Wales, and writing her PhD thesis. Miss B. D. Porter is the Linnean Macleay Fellow for 1979. She is carrying out her research in the School of Biological Sciences at the University of New South Wales on the subject ‘The Structure and Function of Macropodid Salivary Glands”. Linnean Macleay Lectureship in Microbiology This appointment continues to be held by Dr K. Y. Cho. The research work this year concerns mainly the use of agricultural waste for the cultivation of edible fungi. Cotton seed hull has been found suitable for the cultivation of Vovariella volvuacea, Pleurotus ostreatus, Lentinus edodes, Pholiota nameko and Flammulina velutipes. Similar studies will be extended to other edible fungi. The study of the antegenecity of the outer and inner membranes of Azotabacter vinelandii is still in progress. Staff Appointments Mrs Pauline Mills was appointed the Society's Librarian on May 22nd following the resignation of Mrs Buttigieg. Office The Society’s office is on the 6th floor of the Science Centre. The Librarian is in attendance on Mondays and Wednesdays from 9 a.m. until 1 p.m. and the Secretary all day on Tuesdays. The office is closed on Thursdays and Fridays. The Society’s telephone number is 290 1612. Science Centre Professor N. G. Stephenson gave a detailed report on the Science Centre which was printed in full in Newsletter No. 13 issued in June 1979. Library Since the appointment of Mrs Pauline Mills the library has functioned normally. FINANCIAL REPORT This report was given by the Honorary Assistant Treasurer, Dr F. W. E. Rowe, in the absence overseas of the Honorary Treasurer, Dr D. A. Adamson. Following the resignation of Dr Vickery as Honorary Treasurer in August, Council appointed a Finance Committee consisting of Dr D. Adamson, Honorary Treasurer, with Drs F. W. E. Rowe and A. Ritchie assisting. The apparently healthier situation of the Society at the end of 1978 — with a credit balance of $2224, compared with the 1977 deficiency of $3516 — was the result of unusual factors and belies the true situation. Invested funds in the General Account have risen marginally to $94,175 from which we derived interest of $9,864. The remainder of our investments (totalling $403,004) is tied up in the loans to Science House Pty. Ltd. It still appears unlikely that we will receive any financial return from this source in the foreseeable future. Many of the expenditure items differed little from those of the previous year and will not be dealt with individually. Council continued to supplement the Linnean Macleay Fellowship Grant until the completion, in December, of MrsJ. Anderson’s term. The 1978 costs for cleaning and office rent considerably exceeded those of 1977 mainly because the former represented the first payment for a full year. wa Because of the problems encountered with the Proceedings following the printer’s abrupt termination of its long-standing association with the Society, issue of the Proceedings has been severely delayed. 1978 printing costs were only $2287 compared with $10,573 for 1977 for printing and illustrations. The Society can expect, therefore, to face severe financial problems when the cost of publishing the overdue issues and those of the following volume fall in the same financial year. We expect these costs to exceed $10,000. By a decision of Council referees’ fees were discontinued. The delay in publishing the Proceedzngs has also had an effect on the costs of postage and of reprints which were smaller than usual during 1978. Secretarial services cost $10,632 ($11,090 for 1977) which still included payment for editing work undertaken by Science House prior to the Council’s decision to appoint an Honorary Editor. Total expenditure for the year 1978 was $24,310 ($31,911 for 1977). Total income for 1978 in the General Account was $26,534 ($28,395 for 1977). The main sources of income for the General account fall into several categories : (a) Membership subscriptions (b) Subscriptions to Proceedings (c) Interest on General Account investments (d) Transfer of surplus income from the Fellowships Account (e) Donations to the Proceedings (f) Sales of sets of the Proceedzngs, back issues, etc. (g) Sale of valuable assets, e.g., Gould Humming Bzrds volumes. Of these (a) and (b) are unlikely to rise markedly; there is some scope for reinvestment of maturing funds at higher interest rates (c) and (d) ; (e) is likely to be minimal. This leaves (f) sale of Proceedings — these are “once only” items but if potential buyers for sets can be located they may also be expected to subscribe to future Proceedings. (g) Since Landsdowne Press has made facsimiles from other sources do we need to keep this item? The financial situation can also be improved by reduction of expenditure and the main categories where this might be achieved appear to be (a) the library — by relocation and reducing the costs of servicing it. (b) secretarial services currently carried out by Science House Pty. Ltd. Failing some determined action during the next 12 months the Linnean Society will be compelled to draw on investments as they mature instead of reinvesting them, a short-sighted and short-term policy which would solve nothing. In the Fellowships Account total investments of $129,861 produced an interest income of $10,726. $3,199 of this went to the Fellow during 1978 leaving $7,527 to be transferred to the General Account. This was similar to the situation in 1977. The Bacteriology Account involving total investments of $36,900 received interest of $2,398 (similar to 1977), allowing $2,400 to be donated to the University of Sydney towards the salary of the Linnean Macleay Lecturer in Microbiology. The Scientific Research Fund has been augmented by interest of $2,121 and by donations of $2,000 during 1978 bringing the balance to $21,895. Following the presentation of the Honorary Treasurer’s report and discussion a motion that the audited balance sheets for 1978 he adopted was passed unanimously by the members present. PRESIDENTIAL ADDRESS The President, Mr J. T. Waterhouse, delivered an address entitled “The Phylogenetic significance of Dracaena-type growth in Monocotyledons’, which he illustrated with slides. The Presidential Address will be published in full in a future issue of the Proceedings. DECLARATION OF ELECTIONS As the number of nominations did not exceed the number of vacancies on the Council, no election was " necessary. The Chairman declared the following members duly elected : President: Dr A. Ritchie Members of Council: Dr H. A. Martin, Mr E. J. Selby, Dr A. Ritchie, Dr J. W. Vickery, Mr J. T. Waterhouse and Dr A. J. T. Wright. Auditors: W. Sinclair & Co. Mr Waterhouse introduced Dr A. Ritchie as the President for 1979 and invited him to take the Chair. Dr Ritchie called on Professor D. J. Anderson to propose a vote of thanks to Mr Waterhouse for his Presidential Address and for his work for the Society during the year. This was carried by acclamation. Dr Ritchie expressed appreciation of the retiring President’s meticulous chairmanship of Council meetings during a difficult year. 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DREN CLC TOC DONO LOTO.-O LEMUR Oscar ROTI ee O. BOM Mace. O10 sono One suonex3snq yy LI¥'‘T 00°009 Hs G005p i080 O%De0 6 Cobo -Q8Ord 6 OlOo Goo oOo 0 0 6 queig drysmoyaq 009 90°189'L GL6‘G L6“LES ‘--sasuadxg [e12us OIF 90°L6L ‘9 0.090000 Oddo 0-00 05-4 016 0600-0 ooo Oo sSUIp2a001g L¥0‘G G0'02Z foo 0 0 00.0 0:0 076 6615 5 6-00 A ° AOU OOOFC ODDO OO GOO uonepaidag €0Z 00'F8F'I eM obfeMletoiteMellot slielicWel ai alielie(haliells (tsi slvsliet slilelelici > sioq Way 826 00861 Duele hei cltesis et offal silo allo ol elliot eine ifeutelfe ts Moli resigned 24 October 1979 ® deceased 29 May 1979 Cover motif: Fossdrus sydneyenszs Hedley Balmoral Beach, Sydney (Proc. Linn. Soc. N.S.W. 35, 1900:89) PROCEEDINGS of the LINNEAN SOCIETY NEW SOUTH WALES VOLUME 104 NUMBER 3 rs fag remit i Sporobolomycetaceae from Indooroopilly (Australia) and from Port Moresby (Papua New Guinea) DOROTHY E.SHAW and E. GWENDA CARTLEDGE SHaw, D. E., & CarTLEDGE, E. G. Sporobolomycetaceae from Indooroopilly (Australia) and from Port Moresby (Papua New Guinea). Proc. Linn. Soc. N.S.W. 104 (3), (1979) 1980:161-170. Sporobolomycetaceae were isolated following the spore fall method from 60 out of 89 mainly healthy, undamaged, samples from 51 of 58 plant species at Indooroopilly near Brisbane, Australia, and from 21 out of 66 samples from 21 of 51 plant species from eight sites around Port Moresby in Papua New Guinea. At Indooroopilly, positive records involved Sporobolomyces (58.3%), Tulletiopses (38.1%) and Bullera (3.6%), and at the Port Moresby sites, Tzlletzopszs (78.3%) and Sporobolomyces (21.7%), no Bullera being recorded. At Indooroopilly, some plant species were consistently positive with many colonies while five species were negative in two tests. In the Port Moresby area, ratios of positive to negative samples were 1: 1.4, 1: 3.2 and 1: 8.0 for three foliage zones (below 1 m, between 1 and 2 m and over 2 m, a.g.l., respectively) ; 1: 7.0 and 1: 0.2 for coastal versus inland sites, and 1: 1.8 and 1: 17.0 for sites with and without rain in the 24 h preceding sampling. Eighty isolates altogether from the temperate and tropical locations were lodged with Dr J. Fell, U.S.A., for biochemical studies and species identification. Dorothy E. Shaw, C/- Plant Pathology, Department of Primary Industries, Mezers Road, Indooroopilly, Australia 4068 and E. Gwenda Cartledge, 39 Greenways Road, Glen Waverley, Australia 3150 (both formerly, Department of Primary Industry, Konedobu, Papua New Guinea); manuscript received 14 June 1979, accepted in revised form 20 February 1980. INTRODUCTION Since the study of Derx (1930), Sporobolomycetaceae have been recorded on various plants in different parts of the world by workers including Nyland (1948, 1949, 1950) ; Tubaki (1952a, b; 1958); Last (1955 a, b; 1970); di Menna (1959) ; Brady (1960); Last and Deighton (1965) ; Hogg and Hudson (1966); Pady (1974) and Pugh and Lindsey (1975), and they have also been isolated from other situations (Phaff, 1971; Lindsey, 1976). Dickinson (1976) stated that although the majority of phylloplane studies have been carried out in temperate regions and on agricultural crops, the few studies which have been published on tropical plants suggest that many phylloplane fungi (which include the Sporobolomycetaceae) are cosmopolitan in their distribution. In January 1976, the spore fall method of Derx (1930) was used as a qualitative measure to determine whether members of the Sporobolomycetaceae were occurring on samples of plants from Indooroopilly, near Brisbane, a temperate site at 27°28 S latitude, and from around Port Moresby in Papua New Guinea (P.N.G.), a tropical area at 9° 27 S latitude. MATERIALS AND METHODS The average annual rainfall for Brisbane is 1158 mm with 60% occurring from December to April inclusive; average relative humidity for 0900 and 1500 h is 66% and 54% respectively, and mean annual temperature is 20.5°C, with average maximum and minimum of 25.4° and 15.5°C respectively. Proc. Linn. Soc. N.S.W., 104 (3), (1979) 1980 162 SPOROBOLOMYCETACEAE The average annual rainfall for Port Moresby is 1197 mm with 76% occurring from December to April inclusive; average relative humidity for 0900 and 1500 h is 77% and 67% respectively; mean annual temperature is 26.9°C with average maximum and minimum of 31.0° and 22.6°C respectively. At Indooroopilly One sample was taken at random from within the first 30 cm of foliage above ground level (a.g.l.) from each of 58 herbaceous and tree ornamentals, weeds, crop and pasture species* growing within an area of 0.5 ha about 20 km in direct line from the coast. Each sample consisted of a piece of healthy, undamaged leaf, or a small leaf, or phyllode, or several strap-like leaves, according to the plant species. Following the procedure of Derx (1930), samples were attached to the underside of Petri dish lids by adhesive tape at each end to expose an area of the adaxial surface of approximately 10 mm? for each species, and held over potato dextrose agar (PDA) in the bottom of the dishes for three to four days at 25°C. Colonies were then counted, or scored as ‘many’ if confluent. No attempt was made to express the number of colonies quantitatively per cm? of plant tissue because of the variability of the samples. Colonies on the plates, and isolates from the colonies, were examined for colour, ‘halo- ing’ by ejected ballistospores, type and size of spores, presence or absence of budding, mycelium and clamp connexions. Eighteen plant species negative in the first screening were retested a second time with fresh samples. Some of the repeat tests were carried out with the sample on one half of the lid and a fresh sample from Bzdens pilosa L. or Erigeron floribundus (H. B. and K.) Schultz (two species chosen at random from those whose samples gave ‘many’ colonies) on the other half for comparison. Two other species negative twice were retested using insect-damaged material. One other species (Rhychelytrum repens (Willd.) C. E. Hubbard) was sampled twice without and twice with rust (Puccenia levis (Sacc. and Bizz.) Magn. var. tricholaenae (H. Syd. and P. Syd.) Ramachar and Cumm.). Around Port Moresby Samples were taken from 51 plant species* at eight sites around Port Moresby: five sites near the coast and three further inland at 7, 15 and 31 km in direct line from the coast, with the last site on a plateau at about 600 m altitude. The sampling procedure differed slightly from that used at Indooroopilly. At two sites near the city, second samples were taken after rain when the first samples proved negative. In a few other cases, a second (and in two more cases, a third) sample was taken at another site or at another foliage height or both. The height a.g.l. of each sample was measured, and these are grouped arbitrarily into three foliage zones as (1) under 1 m, (2) between 1 and 2 m, and (3) over 2m a.g.l. The method of isolation followed the spore fall procedure of Derx (1930) as given in the previous section, except that quantities of colonies were not assessed. The meteorological data given previously apply to Site 6. Although no accurate figures are available for other sites, the five near the coast are generally slightly drier and warmer, and the other two inland sites slightly wetter and cooler, than Site 6. Rain was known to have fallen at all sites during the 24 h preceding sampling except at two coastal sites when the first screening followed a dry 24h, and at Site 7, where no information was available. *A complete list of species is available for any interested reader. Proc. Linn. Soc. N.S.W., 104 (3), (1979) 1980 D. E.SHAW AND E. G. CARTLEDGE 163 RESULTS At Indooroopilly Sixty (67.4%) out of the 89 samples, involving 51 (87.9%) out of 58 plant species, yielded Sporobolomycetaceae (Table 1, a andb). Three (5.2%) of the plant species sampled (Lantana montevidensis Briz., Trifolium repens L. and Wahlenbergia caryophyllordes B. Carolin) yielded three genera of the Sporobolomycetaceae, namely Sporobolomyces, Tulletiopsis and Bullera. One of the species was scored as having ‘many’ colonies of Tzlletzopsvs. TABLE 1 Summary of the number and percentage of samples and sampled plant species at Indooroopilly and around Port Moresby positive and negative for various genera of the Sporobolomycetaceae Item as under Indooroopilly Around Port Moresby No. % No. % a Samples positive 60 67.4 21 31.8 Samples negative DMT US Wey olay yy SURE 45 68.2 Total samples 89 100 66 100 b Plant species positive 51 87.9 21 41.2 Plant species negative 7 12.1 30 58.8 Total plant species 58 100 51 100 c Plant species with genera: Sporobolomyces, Tilletzopses and Bullera 3 5.2 0 0 Sporobolomyces, and Tilletzopszs 27 46.5 23 3.9 Sporobolomyces only 19 32.8 3 5.9 Tilletzopszs only 2 3.4 16 31.4 None 7 12.1 30 58.8 58 100 5 100 d Total records of genera, separately: Sporobolomyces 49 58.3 5 21.7 Tilletiopszs 32 38.1 18 78.3 Bullera 3 3.6 0 0 84 100 23 100 Twenty-seven (46.5%) of the plant species sampled yielded two genera, Sporobo- lomyces and Tilletiopsis. Of these species, seven were scored with ‘many’ colonies of both Sporobolomyces and Tulletiopsis. These included Bzdens pilosa and Erigeron flortbundus which were consistently positive with ‘many’ colonies of both genera in six and four successive samplings respectively. Five other plant species yielded only Sporobolomyces, one with ‘many’ colonies. Two (3.4%) of the species yielded only Tilletzopsis, one with ‘many’ colonies. Eleven of the plant species included above did not yield any Sporobolomycetaceae in their first tests, and were resampled, the second tests proving positive in all except two, viz., Acacia podalyrizfolia A. Cunn. ex G. Don and Eucalyptus sp. A third sample from each of these two species deliberately selected with insect damage proved positive. The two healthy samples of Rhynchelytrum repens were negative and the two rusted samples positive. Seven (12.1%) of the plant species (?Astridza sp., Chlorophytum capense (L.) Kuntze, Crotalaria mucronata Desv., Ctenanthe oppenheimeriana Schum., Hakea gibbosa (Sm.) Cav., Macroptylium lathyrotdes (L.) Urb and Pinus sp.) did not yield any Sporobolomycetaceae when tested twice. The above figures are summarized in Table 1, c. Total records of the genera Proc. LINN. Soc. N.S.W., 104 (3), (1979) 1980 164 SPOROBOLOMYCET ACEAE taken separately are Sporobolomyces 49 (58.3%), Tulletiops’s 32 (38.1%) and Bullera 3 (3.6%) (Table 1, d). The specific identities of the Sporobolomyces isolates were not determined as facilities for the biochemical studies were not available. The isolates of Tzlletzopszs had ballistospores with length before germination of 4.5-10.5 um; on the medium used (PDA) the colonies were at first white and glistening, then ‘frosted’, turning deep ivory in colour and still later deep tan; all the isolates produced tan pigment in the medium. The isolates are tentatively ascribed to T. minor Nyland. The size of the ballistospores of the Bullera isolates falls into the ‘B. alba’ group, but as it was not possible to carry out nitrogen assimilation tests, it is not known, for example, whether some or all were B. alba (Hanna) Derx, which does not assimilate nitrate, or B. tsugae Phaff and Do Carmo-Souza, which does (Phaff, 1971). Although colonies were carefully checked for the presence of clamp connexions, none was noted, so that in this preliminary survey no species of Sporzdiobolus or Itersonilia were recorded. Thirty-four isolates, consisting of one isolate of Bullera, 10 of Tilletzopszs and 20 of Sporobolomyces, as well as three isolates which were non-ejecting and are perhaps true yeasts, were lodged in 1976 with Dr J. Fell, U.S.A., for biochemical studies and species identification, the results of which will be published separately. Around Port Moresby Sixty-six samples were taken from 51 herbaceous and tree species. No sample yielded three genera of the Sporobolomycetaceae as at Indooroopilly. Twenty-one (31.8%) out of the 66 samples, involving 21 (41.2%) of 51 plant species, yielded Sporobolomycetaceae (Table 1, aandb). Two (3.9%) of the plant species sampled yielded both Sporobolomyces and Tilletcopsts: three (5.9%) only Sporobolomyces and 16 (31.4%) only Tulletzopszs. Thirty (58.8%) * of the species sampled did not yield any Sporobolomycetaceae at all, even the six tested twice. The results are summarized in Table 1, c. Total records of the genera taken separately are Tzlletzopszs 18 (78.3%) and Sporobolomyces 5 (21.7%) (Table 1, d). TABLE 2 Number, percentage and ratio of samples posztive and negative for Sporobolomycetaceae from three foliage zones sampled around Port Moresby Samples Foliage zones Yielding Not yielding Sporobolo- Sporobolo- Total mycetaceae mycetaceae Posi- Nega- (positive ) (negative) tive tive m (a.g.1.) No. % No. % No. % G% % Ratio Below 1 36 54.5 15 WoT 21 31.8 41.7 58.3 1:1.4 Between 1] and 2 21 31.9 5 7.6 16 24.3 23.8 76.2 1:3.2 Over 2 9 13.6 1 1.5 8 12.1 11.1 88.9 1:8.0 Total 66 100 21 31.8 45 68.2 *A complete list of species is available for any interested reader. p P y Proc. Linn. Soc. N.S.W., 104 (3), (1979) 1980 D. E. SHAW AND E. G. CARTLEDGE 165 Thirty-six (54.5%) of the samples came from the foliage zone below 1 m, 21 (31.9%) from between 1 and 2 m and 9 (13.6%) from the zone over 2 m a.g.]. The ratio of positives (yielding Sporobolomycetaceae) to negatives in the three zones is 1:1.4, 1:3.2 and 1:8.0 respectively (Table 2). Only 28.6% of the positive samples came from the five coastal sites, whereas 71.4% came from the three inland sites. The percentages of positives to negatives in the coastal area are 12.5% and 87.5%, giving a ratio of 1:7.0, compared with 83.7% and 16.7% for the inland area, giving a ratio of 1:0.2 (Table 3). TABLE 3 Number and percentage of samples positive for Sporobolomycetaceae at eight sites in two areas around Port Moresby and ratio of posztives to negatives Samples Location Per site Per area Positive for Sporobolo- Total Posi- Nega- Total mycetaceae Total positive tive tive No. No. oe No. No. % G % Ratio Coastal area 48 6 28.6 12.5 87.5 1:7.0 Site 1 18 2 9.5 2: 12 1 4.8 Ey oe) 6 0 0 od 6 1 4.8 Be 6 2 9.5 Inland area 18 15 71.4 83.3 16.7 1:0.2 Site 6 6 6 28.6 eal 6 5 23.8 BS 6 4 19.0 66 21 + 100.0 66 21 + 100.0 Some samples at Sites 1 and 2 had been collected when no rain had fallen in the previous 24 h, and others after rain had fallen during this period. The figures for these sites were one positive sample against 17 negatives without rain, giving a ratio of 1:17, compared with two positives against 10 negatives after rain, giving a ratio of 1:5. The figure for all sites (except Site 7 where no rainfall information was available) was one positive against 17 negatives without rain, a ratio of 1:17, compared with 15 positives against 27 negatives with rain, a ratio of 1:1.8 (Table 4). The specific identities of the Sporobolomyces isolates were not determined as facilities for the biochemical studies were not available. The Tvlletzopses isolates were all at first white and glistening, then ‘frosted’, turning deep ivory in colour and still later deep tan. The lengths of the isolates mainly fell into the T. mznor range, although eight of the 45 isolates measured had lengths over 12.5 ym and appeared nearer to T. washingtonensis Nyland; some widths were wider than those recorded for this species. Therefore all isolates are ascribed to Tilletiopsis sp. until further study. Forty-six isolates, consisting of nine isolates of Sporobolomyces, 36 of Tzlletzopszs from the present study, and one isolate of T. mznor isolated previously by Shaw (unpublished) were lodged in 1976 with Dr J. Fell, U.S.A., for biochemical studies and species identification, the results of which will be published separately. Proc. LInn. Soc. N.S.W., 104 (3), (1979) 1980 166 SPOROBOLOMYCETACEAE TABLE 4 Number and ratio of samples positive and negative for Sporobolomycetaceae with and without rain during the 24 h prior to collection around Port Moresby Samples Rainfall during 24 h prior to collection Positive Negative Positive: Negative No No Ratio No rain, sites 1 and 2 1 17 1:17.0 Rain, sites 1 and 2 2 10 1: 5.0 Rain, all sites (except Site 7*) 15 27 1: 1.8 *No rainfall information available. DISCUSSION The results of the studies in the two regions (as discussed in detail below) support the suggestion that members of the Sporobolomycetaceae are cosmopolitan in distribution. Locality occurrence As shown in Table 1, a and b, 67.4% of the samples at Indooroopilly were positive for Sporobolomycetaceae, and 31.8% of the samples were positive around Port Moresby; 87.9% of the plant species sampled at the former location were positive and 41.2% positive around Port Moresby. These figures for occurrence even from mainly healthy, undamaged samples indicate that members of the family are fairly common at the tropical location (Port Moresby) and common at the temperate site (Indooroopilly) . Relative abundance of genera and temperature relations Last and Deighton (1965) stated that Sporobolomyces is the best known genus of the Sporobolomycetaceae. Nyland (1950), Gandy (1966) and Flannigan and Campbell (1977) reported that Sporobolomyces predominated over Tulletzopszs. Last (1955a), however, found that Tzlletzopszs, when present, decreased the number of colonies of Sporobolomyces. From studies with spore traps in England, Last (1955b) found a predominance of Sporobolomyces per m> of air compared with Tulletzopszs, the position being reversed a month later, and Gregory and Sreeramulu (1958) found that numbers of Sporobolomyces reached a maximum of about one million per m°, about six times the peak concentration of Tzlletzopsis. Last (1955a) recorded T. mznor only in the warmer months of his study in England. In controlled experiments, the number of colonies of S. roseus reached a maximum about 20°C. Pady (1974) isolated Sporobolomyces throughout the year in Kansas, Bullera in autumn, winter and spring, and Tvlletzops¢s only in summer; T. minor was the only species to produce well at 27°C. Derx (1930) reported that some species of Sporobolomyces had no growth at 30°C while others had some growth sometimes or were positive. Dickinson (1976) concluded that Tulletzopses appeared to require a higher temperature for growth than Sporobolomyces. Species of Bullera have been recorded very occasionally, as summarized by Phaff (1971), and since then mentioned by various authors including di Menna (1971), Davenport (1976) and Dickinson (1976). Derx (1930) found that the maximum temperature of B. alba was 27°C and Phaff (1971) reported that B. alba gave no growth at 30°C. Proc. Linn. Soc. N.S.W., 104 (3), (1979) 1980 D. E. SHAW ANDE. G. CARTLEDGE 167 The lower temperature at Indooroopilly may have accounted for the predominance of Sporobolomyces (58.3%) over Tulletiopsis (38.1%) and for the occurrence of Bullera (3.6%) at that site, while the higher temperature at Port Moresby may have contributed to the predominance of Tulletzopsis (78.3%) over Sporobolomyces (21.7%) and Bullera (0%) in that area (Table 1, d). Whether a reversal of genus dominance occurs at higher altitudes (up to 4500 m) in P.N.G. has still to be determined. Hosts’ Last and Deighton (1965) and di Menna (1971) considered that colonizers of leaf surfaces (including Sporobolomycetaceae) were not host specific. Gandy (1966), however, found that Itersonzlza perplexans Derx occurred on some live and dead parts of some host and non-host species, but not on some other parts or some other species. It was rarely isolated from the hirsute leaves of a derivative of Chrysanthemum morifolium, but was commonly found on glabrous leaves of three other Chrysanthemum species. Last (1970) found that numbers of Tzlletzopszs colonies isolated from leaves of three herbs usually greatly exceeded those of Sporobolomyces, but the latter was usually more abundant on three deciduous tree species. Lamb and Brown (1970) isolated 10 times more colonies of S. roseus from leaves of Paspalum dilatatum than from Salix babylonica, and none at all from Eucalyptus stellulata. Davenport (1976) recorded S. roseus from certain parts of apple flowers and fruit but not from other parts, and Dennis (1976) isolated S. roseus from freshly harvested fruit of Rubus idaeus and R. ulmzfolius whereas none was recovered from the fruit of Fragaria ananassa. At Indooroopilly, although 87.9% of the plant species tested yielded Sporobolomycetaceae, including two species consistently positive in six and four tests each, 12.1% of the plant species were negative even when tested twice (Fig. 1, b). The limited number of repetitions precludes the drawing of any definite conclusions from the results. However, in view of the slight evidence presented, it is suggested that undamaged leaves of some species may be less acceptable habitats than others to even epiphytic phylloplane inhabitants such as the Sporobolomycetaceae. A similar opinion has already been expressed by Lamb and Brown (1970), Dickinson (1976) and Irvine etal. (1978). As yet, little information has accumulated in the literature on recovery or non- recovery of Sporobolomycetaceae from various plant species or parts of plants. In some cases where samples have been drawn from many hosts, the species names have not been published, no doubt because of space restrictions. It would seem that many more data are required from repeated screenings in order to determine consistent negatives. If confirmed, they could then be investigated in detail to determine the cause or causes of the inhospitality. This might involve aspects of gross morphology and structure orientation (affecting, for example, the deposition and liberation of propagules) ; glabrosity or hairiness and presence of glands and stomates; microscopic topography and surface wax crystals; nutrient status or inhibitory activity of leachates and possibly other factors intrinsic to the host. In colonization studies, methods apart from spore fall may need to be considered (Bashi and Fokkema, 1976). State of the host Derx (1930) considered that the Sporobolomycetaceae belong to the microflora which are nourished principally by exudations on plants produced by atmospheric or traumatic causes. Some workers have obtained the greatest number of colonies from actively growing leaves (Ruscoe, 1971), from leaves soon after unfolding and persisting for 18 months (Hog and Hudson, 1966), from living and dead leaves (Last, Proc. Linn. Soc. N.S.W., 104 (3), (1979) 1980 168 SPOROBOLOMYCET ACEAE 1955a; Gandy, 1966; Collins, 1976). Brady (1960) found that species of Tzlletzopszs were present on most leaves checked whether or not these were attacked by Entyloma, but Last and Deighton (1965), Pady (1974) and Last (1970) reported increase in numbers after fungal infection, leaf nematodes, mites and other damage. Burg (1974) suggested that Sporobolomyces only becomes established on Phragmites australis following honey dew deposition, but Dickinson (1976) reported growth on undamaged and unpolluted leaves of this host. In the present study, Sporobolomycetaceae were obtained from healthy, undamaged leaves of many plants. However, insect damaged leaves of Acacza podalyrifolia and Eucalyptus sp., and rusted leaves of Rhynchelytrum repens yielded colonies whereas healthy, undamaged ones did not, so that the former groups apparently afforded a more favourable habitat for sporulation than did the latter. Height of samples Last (1955a) found that the greatest concentration of Sporobolomyces spores in the air over wheat in England was near ground level. Lamb and Brown (1970) conceded that closeness to the ground may have contributed to the larger number of colonies of S. roseus isolated from a host sampled at 30 cm compared with two other hosts sampled at 2 ma.g.l. The ratios of samples positive to negative for Sporobolomycetaceae in the Port Moresby study were 1: 1.4 for the foliage zone below 1 m, 1:3.2 for the zone between 1 and 2 m, and 1:8.0 for the zone over 2 m a.g.l. (Table 2). While different plants were sampled in each zone, these figures indicate that the largest numbers of Sporobo- lomycetaceae were probably occurring in the lowest zone. Various factors may have been responsible for this, particularly humidity, which was probably highest in the zone closest to the ground. Coastal versus inland sites Pugh and Lindsey (1975) found that cell numbers of Sporobolomyces from plants growing in maritime areas were lower than those of inland plants and was caused by relatively high salt concentrations on leaf surfaces due to deposition and evaporation of salt spray. The ratio of samples positive for Sporobolomycetaceae to negative for the five coastal sites around Port Moresby was 1:7.0 whereas the ratio for the three more inland sites was 1:0.2 (Table 3) . Salt deposition may have had some part in reducing the populations on leaves at the coastal sites. These latter, however, are also in a drier and warmer zone than the sites further inland, and this may also have contributed to the reduction in numbers of their positive samples. Rainfall and humidity Various workers have discussed rainfall and humidity in relation to the Sporo- bolomycetaceae. Last (1955a) concluded that in wheat the spread of Sporobolomyces was probably restricted until the crop became dense enough to raise the humidity. Last (1955b) also found a tremendous increase in the number of spores per m* over cereal crops on a rainy day compared with a dry day. Zoberi (1964) reported that the rate of ballistospore discharge of S. roseus fell immediately on transfer from high to low humidity but recovered on return to relatively damp air, if the exposure to dry conditions was not too prolonged. Pugh and Lindsey (1975) reported that populations of Sporobolomyces on leaves of Halimione portulacotdes were removed by tidal washing and a similar effect was also obtained by washing leaves in the laboratory. Bashi and Fokkema (1977), however, found no evidence that rain could be either beneficial to yeast populations by providing free water or disadvantageous by washing cells from the leaves, although continuous rain may leach nutrients. Sporobolomyces Proc. Linn. Soc. N.S.W., 104 (3), (1979) 1980 D. E. SHAW ANDE. G. CARTLEDGE 169 could only profit from the nutrients if exposed to relative humidities of at least 90% during part of the day. Flannigan and Campbell (1977), however, noted increase in numbers of S. roseus populations on wheat despite dry weather, perhaps influenced by increased nutrient availability from ageing organs or pollen grains deposited on the surface. Dickinson and O’Donnell (1977) supported the suggestion that humidity is a prime factor in determining the extent of leaf colonization. At Port Moresby, fewer samples were positive when collected after a dry 24h (positives to negatives 1:17) than after rain at the same two sites (1:5) or at all sites (1:1.8) (Table 4). The last ratio may reflect higher annual rainfall at two of the sites, as well as rainfall during the 24 h prior to collection. Possible interactions with other microorganisms Di Menna (1962) recorded S. roseus as sensitive to some bacterial species from soil, to soil Streptomyces and a few soil fungi, while Smith (1967) found that isolates of Baczllus subtelis and Streptomyces from natural soil were antagonistic to J. pastinacae. A protostelid, Protostelium mycophaga var. major Olive, was found parasitizing Sporobolomyces sp. isolated from Solanum nodiflorum Jacq. at Indooroopilly (Shaw and Olive, 1977). However, it is not known whether the Indooroopilly samples differed from the Port Moresby samples regarding type and quantity of other phylloplane resident or transient microorganisms, or other objects such as pollen (Fokkema, 1976) which may have also contributed to the difference in numbers of colonies obtained between the temperate and tropical sites. ACKNOWLEDGEMENTS Grateful acknowledgement is made for the identifications of some plant species by Mr N. Byrnes of the Botany Branch, Department of Primary Industries (D.P.I.), Indooroopilly and Mr E. Henty, Department of Forests, Papua New Guinea, and to Mr G. S. Purss, Director of the Plant Pathology Branch, D.P.I., Indooroopilly, for making facilities available to the first author for the Queensland study. References BasHt, E., and FoKKEMA, N. J., 1976. — Scanning electron microscopy of Sporobolomyces roseus on wheat leaves. Trans. Brit. mycol. Soc. 67: 500-505. —, 1977. — Environmental factors limiting growth of Sporobolomyces roseus, an antagonist of Cochliobolus sativus, on wheat leaves. Trans. Brit. mycol. Soc., 68: 17-25. Brapy, B. L., 1960. — Occurrence of Itersonzlza and Tulletzopszs on lesions caused by Entyloma. Trans. Brit. mycol. Soc., 43: 31-50. BurG, A. van der, 1974. — The occurrence of Sporobolomyces roseus, a red yeast on leaves of Phragmites australis. Thesis, Free University of Amsterdam. (Cited by Dickinson, 1976.) Coins, M. A., 1976. — Colonisation of leaves by phylloplane saprophytes and their interactions in this environment. In Microbiology of aerzal plant surfaces, C.H. DickINsON and T. F. PREECE (eds), pp. 410-418. London: Academic Press. DAVENPORT, R. R., 1976. — Distribution of yeasts and yeast-like organisms from aerial surfaces of developing apples and grapes. In Microbiology of aerial plant surfaces, C. H. Dickinson and T. F. PREECE (eds), pp. 325-349. London: Academic Press. DENNIS, C., 1976. — The microflora on the surface of soft fruits. In Mzcrobzology of aerial plant surfaces, C. H. Dickinson and T. F. PREECE (eds), pp. 419-432. London: Academic Press. Derx, H. G., 1930. — Etude sur les Sporobolomycetes. Ann. Mycol, Berlin, 28: 1-23. Dickinson, C. H., 1976. — Fungi on aerial surfaces of higher plants. In Mzcrobzology of aerial plart surfaces, C. H. Dickinson and T. F. PREECE (eds), pp. 293-324. London: Academic Press. ——, and O’DonneELL, J., 1977. — Behaviour of phylloplane fungi on Phaseolus leaves. Trans. Brit. mycol. Soc., 68: 193-199. FLANNIGAN, B., and CAMPBELL, I., 1977. — Pre-harvest mould and yeast floras on the flag leaf, bracts and caryopsis of wheat. Trans. Brit. mycol. Soc., 69: 485-494. Proc. Linn. Soc. N.S.W., 104 (3), (1979) 1980 170 SPOROBOLOMYCETACEAE FokKEMA, H. J., 1976. — Antagonism between fungal saprophytes and pathogens on aerial plant surfaces. In Microbiology of aerzal plant surfaces, C. H. DickINson and T. F. PREECE (eds), pp. 487-506. London: Academic Press. Ganpy, D. G., 1966. — Itersonilia perplexans on chrysanthemums: alternative hosts and ways of overwintering. Trans. Brit. mycol. Soc., 49: 499-507. Grecory, P. H., and SREERAMULU, T., 1958. — Air spora of an estaury. Trans Brit. mycol. Soc., 41: 145- 156. Hocc, B. M., and Hupson, H. J., 1966. — Micro-fungi on leaves of Fagus sylvatica 1. The micro-fungal succession. Trans. Brit. mycol. Soc., 49: 185-192. IRVINE, J. A., Dix, N. J., and Warren, R. C., 1978. — Inhibitory substances in Acer platanozdes leaves: seasonal activity and effects on growth of phylloplane fungi. Trans. Brit. mycol. Soc., 70: 363-371. Lams, R.J., and Brown, J. F., 1970. — Non-parasitic microflora on leaf surfaces of Paspalum dilatatum, Salix babylonica and Eucalyptus stellulata. Trans. Brit. mycol. Soc., 55: 383-390. Last, F. T., 1955a. — Seasonal incidence of Sporobolomyces on cereal leaves. Trans. Brit. mycol. Soc., 38: 221-239. ——, 1955b. The spore content of air within and above mildew-infected cereal crops. Trans. Brit. mycol. Soc., 38: 453-464. ——, 1970. — Factors associated with the distribution of some phylloplane microbes. Nether J. Pl. Path., 76: 140-143. , and DEIGHTON, F. C., 1965. — The non-parasitic microflora on the surfaces of living leaves. Trans. Brit. mycol. Soc., 48: 83-99. LinpseEy, B. I., 1976. — Saprophytes on plant surfaces in maritime areas. In Microbiology of aerzal plant surfaces, C. H. Dickinson and T. F. PREECE (eds), pp. 391-399. London: Academic Press. MeEnnaA, M. E. di, 1959. — Yeast from the leaves of pasture plants. New Zealand J. agric. Res., 2: 394-405. —, 1962. — The antibiotic relationships of some yeasts from soil and leaves. J. Gen. Microbzol., 27: 249- 257. —— , 1971. — The microflora of leaves of pasture plants in New Zealand. In Ecology of leaf surface micro- organisms, T. F. PREECE and C. H. Dickinson (eds), pp. 159-174. London: Academic Press. NyLanp, G., 1948. — Preliminary observations on the morphology and cytology of an undescribed heterobasidiomycete from Washington State. Mycologza, 40: 478-481. ——, 1949. — Studies on some unusual heterobasidiomycetes from Washington State. Mycologza, 41: 686- 701. ——, 1950. — The genus Tulletiopss. Mycologia, 42: 487-496. Papy, S. M., 1974. — Sporobolomycetaceae in Kansas. Mycologia, 66: 333-338. PuarF, H. J., 1971. Discussion of the yeast-like genera belonging to the Sporobolomycetaceae. In The yeasts: a taxonomic study, J. LopDER (ed.), pp. 815-862. Amsterdam: North-Holland. Pucu, G. J. F., and Linpsey, B. I., 1975. — Studies of Sporobolomyces in a maritime habitat. Trans. Bret. mycol. Soc., 65: 201-209. RuscoE, Q. W., 1971. — Mycoflora of living and dead leaves of Nothofagus truncata. Trans. Brit. mycol. Soc., 56: 463-474. SHaw, D. E., and Otive, L. S., 1977. — A rare protostelid (Mycetozoa) recorded in Australia. Proc. Lznn. Soc. N.S.W., 102: 58-59. i Smit, P. R., 1967. — The survival in soil of Itersonilia pastinacae Channon, the cause of parsnip canker. Aust. J. Biol. Sct., 20: 647-660. Tusakl, K., 1952a. — Studies on the Sporobolomycetaceae in Japan: I. On Tulletzopszs. Nagaoa, 2: 26-31. ——., 1952b. — Studies on the Sporobolomycetaceae in Japan: II. On Itersonzlca. Nagaoa, 2: 62-66. ——, 1958. — Studies on the Japanese Hyphomycetes (IV). Miscellaneous group. Bot. Mag., Tokyo, 71: 133-137. ZoBERI, M.H., 1964. — Effect of temperature and humidity on ballistospore discharge. Trans. Brit. mycol. Soc., 47: 109-114. Proc. LINN. Soc. N.S.W., 104 (3), (1979) 1980 A Preliminary Report on the late Cainozoic Geology and Fossil Fauna of Bow, New South Wales C. G. SKILBECK SKILBECK, C. G. A preliminary report on the late Cainozoic geology and fossil fauna of Bow, New South Wales. Proc. Linn. Soc. N.S.W. 104 (3), (1979) 1980:171- 181. Fossil marsupials collected from Bow, New South Wales, since 1966 are here examined and identified for the first time. These fossils occur in unconsolidated riverine conglomerates that overlie Liverpool Range basalts of early Janjukian age. The fossil deposits are estimated to be about 4.5 million years old (early Pliocene). A comparison of species recovered from Bow with those of other Australian Tertiary mammal faunas indicates affinities with both the Bluff Downs and Chinchilla local faunas of Queensland. C. G. Skilbeck, Department of Geology and Geophysics, University of Sydney, Australia 2006; manuscript received 24 August 1979, accepted in revised form 20 February 1980. INTRODUCTION Excavations during relocation of the Merriwa-Cassilis Road at the site of the new bridge across Bow Creek led to a road cutting exposure (grid reference 323033 on 1:250,000 Geological Sheet for Singleton (No. S1-56-1), New South Wales, New South Wales Department of Mines, Sydney) of sediments containing a fossil mammal fauna. Although discovered in 1964, the palaeontological significance of this site remained unknown until 1966 when a local council gardener gathered surface specimens and forwarded them to the Australian Museum. The site was visited by J. A. Mahoney, of the University of Sydney, several times during 1966 at which time further specimens were collected. Between 1967 and 1970 a local banker, E. W. McDonald, made extensive collections at the site and donated these to the Australian Museum. A group that included A. Ritchie, of the Australian Museum, visited Bow in 1975 and with the aid of council earthmoving equipment collected further material. Further surface material was collected during research for the present study. Continued investigation of the site is being conducted by M. Archer of the University of New South Wales. GEOLOGICAL SETTING Bow is situated approximately 12 kilometres west of Merriwa on the Merriwa- Cassilis Road (Fig. 1). It lies on the ‘Merriwa Plateau’, a geomorphological sub- division of the Hunter Valley on the southern slopes of the Liverpool Ranges (Galloway, 1963b). Galloway, in his geomorphological study of the Hunter Valley (1963a, 1963b, 1967) concluded that the recent drainage pattern has been determined primarily by lithology and secondarily by the structure of Palaeozoic and Mesozoic rocks which crop out in the valley. The effects of widespread Tertiary volcanism have been considerable. The pre-Cainozoic geology of the Hunter Valley has been recorded by Packham et al. (1969); Branagan, Herbert and Langford-Smith (1976) and Proc. Linn. Soc. N.S.W., 104 (3), (1979) 1980 172 CAINOZOIC GEOLOGY AND FOSSIL FAUNA Galloway (1963a). The only recently published investigation of the Tertiary basalts of the Liverpool Ranges is that of Galloway (1967) who looked at the occurrence of the basalt and its effects on subsequent geomorphology. A detailed investigation of the petrology and geochemistry of these basalts is at present being undertaken by R. Schon of the University of Sydney. GEOLOGY OF THE BASALT Great flows of basalt were extruded over much of the Hunter Valley during the middle Tertiary (Galloway, 1967). These volcanics were erupted from two separate shield volcanoes and yield potassium/argon dates of 33.7 + 1.4 million years (lower Janjukian) and 39.0 + 1.4 million years (middle Aldigan) for the western and eastern provinces respectively (Wellman et al., 1969). These dates are further supported by those of Wellman and McDougall (1974). The remnants of this volcanic episode are manifest as the present Liverpool Ranges. The geology of the basalt is of particular importance in the development of Bow Creek since basalt forms its basement and provided a unique source of its sediment. Perpendicular jointing planes and the platy texture of weathered basalt which crops out around Bow indicate that the flows there dip slightly to the south. These near horizontal flows indicate a highly liquid lava capable of widespread occurrence. Petrologically, the basalts that crop out in the vicinity of Bow are olivine basalts. The texture is highly fluidal and amygdales occur in some flows. Although more than one flow can be recognized at Bow, a single volcanic episode is thought to have been their origin. The evidence for this single episode is the narrow range of modal compositions of six basalt samples from different stratigraphic levels. These compositions were derived by thin section point count. POST-BASALTIC DEVELOPMENT Since the termination of basalt eruption, the Hunter Valley has been subject to almost continual erosion. Removal of vast quantities of basalt and underlying sediments in some places has produced the lower-relief areas of the valley. Minor erosion in the thicker basalt areas has resulted in a remoulding of the geomorphology without any great topographical changes. The ‘Merriwa Plateau’ is an example of the latter part of this range of topographical expressions. Deep dissection of the basalt has not occurred; erosion has resulted in broad shallow valleys that are typified by the formation of alluvial terraces. THE GEOMORPHOLOGICAL DEVELOPMENT OF BOW CREEK The late Cainozoic deposition at Bow occurred in a depression, now occupied by a laterally restricted, slightly meandering stream. The earliest fluvial sediments in the Bow Creek Valley, deposited subsequent to the cessation of volcanism, have been partially eroded by the modern creek to form characteristic fluvial terraces. In some places, the terrace bank and/or river bed is defined by renewed incision of the basalt basement. Terrace delineation, within the scope of this report, has only been tentatively attempted for the Bow Creek Valley (Fig. 1). It is based on altitude correlations of plane table mapping data. Based on the definition of a terrace as an ‘abandoned flood plain’ (Leopold, Wolman and Miller, 1964) for the section of Bow Creek studied, four terraces are recognizable. An active flood plain with an associated low discharge level bench is also recognized. The abandonment of a flood plain can occur by three methods (Warner, 1972). Proc. Linn. Soc. N.S.W., 104 (3), (1979) 1980 C. G. SKILBECK FOSSIL LOCALITY K TI t CREE } > > > > >>>>>>>>>>>>>> > > > > > >>>>>>>>>>>>>>> >>>>>>>>>>>>>>>>>>>> >>>>>>>>>>>>>>>>>>> OR I ee ES >>> >>>>>>>>>>>>>> HSSSSSS SC SSO SS SRQSSSSS555 4 55555 D> >>> SOBSS SSS SASS >> ROS dd >5>4>>555> SoS ESE eee eee SS SS > RRP SSS 54> > >> o> \P2>>>>>8>> SSSSSS NS OSS 54555555 } SISAL Qo >>> 4 SFS555 H SS4SS55 55 H SSS555 ' WF >>555> 1 p>>>>>> H SSSS55 } £ 3 Ke >>- >> >>>>555> peak fanaa SSSSSSSStSsssss IE >>>>>>bSS>>>> SSSSSSSSISPSSSS oN) >>>>>>>>Pp>>>>>>- >>>>>>>> Op >>>yS>> Ue ete ere re 2>PPr>r>PArrrHr>>r>r>>>>e >>>>>>>>>—~ >>> >>>>>>H> >>> >>> SH > >> >> >>> >>>>>>>>>>>>>>>5 SSSSSSSSSBSSSE >> mY >>>>>>>>>>>>>>>>>>>>>>>>>>>>>> >> >>>>>>>/P >>> >>>>>>>>>>>>>>>>>>>>>>>>>>>>>> > >>>>>>>> > >>> >>> >>> >>>>>>>>>>>>>>>>>>>>>> eee >>>>>>>>f >>>>>>>>> >>> >>> >>>>>>>>>>>>>>>>>>: UsssX\\ >>>>>>>3fh PP >>> >>> >>> >>> >>> >> >>> >>> >>> >>>>>>>>>>>>>F >>>>>>> PPP >> >> rrr >>> >>>>>>>>>>>>>>>>>>>>>>>>>>>>% >>> >>>>HP>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>> i SESESEE PP >>> r>>>>>>> >>> >>> >>>>>>>>>>>>>>>>>>>>>> i f q f > >>>>>>H>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>> >>>>> B >> >>> >>> >> >>> >>> >> 5555555555555 555555555 >>>>>F ‘EEE ESSE ESESE SESE SESE EESEEESSESSS SS SS SS SESS >>>> YD SSS SSS SSS SSS SSS SSS SSS SSSSSSSSSSS P>>>As >>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>> >>>> (3 >>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>> P>>>An >>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>> >>>>>hc DS SSSSSSSS SSS SSS SSS SSS SSS SSS SSS SSM >>>>>4V > >>> >>> >>> >>> >>> >>> >>>>>>>>>>>>>>>>>>>>>>>>> >>>>>H P >>> > >>> >>> >>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>> 2>>>>>h D> >>>>>> FP >>> >>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>> D> >>>B ->>>>>>>5> >>> >>> >>> >>> >> >3 >> >>5>5 5555555555555 >>> >>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>> >>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>> >>> >>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>> >>> >>>>>>>>>>>>>>> >>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>>> PINNVVNVVVY > >> >> >> >> >> > H H H if { i i NAVIN VINNY VVVVV o1 a 173 Zz © & & “~o x 8 = KS ot 5 AQ aes — Z a oO = >Zuw = > O = N = — wu >>>>>>>>>>>>> >> 2P>>>>>>>>>>>>>>>>>> > 2>>>>>>>>>>>>>>>>>>>> a>> 2>>>>>>>>>>>>>>>>>>>>>> >> 2>>>>>>>>>>>>>>>>>>>>>>> >> >>>>>>>>>>>>>>>>>>>>>>>> >>> >>> >>> >>> >>>>>>>555>55555 >>> >>> >>> >>> >>> 5555555555555 >> >>>>>>>>>>>>>>>>>>>>>>>>>> >>> >> >>> >>> 5>>>>>>>>55555555 >>>>>>>>>>>>>>>>>>>>>>>>>>>> >>> >> >>> >>> >>>>>55>5>>>>>55>5 >>>>>>>>>>>>>>>>>>>>>>>>>>>> >>>>>>>>>>>>>>>>>>>>>>>>>>>> >>> >>> >> >> >S >>> >5 555555555555 >>>>>>>>>>>>>>>>>>>>>>>>>>>> >>> >>> >>> >>> >>> >> >>5>5555>55 >>>>>>>>>>>>>>>>>>>>>>>>>>>> >>>>>>>>>>>>>>>>>>>>>>>>>>>> >>>>>>>>>>>>>>>>>>>>>>>>>>>> >>>>>>>>>>>>>>>>>>>>>>>>>>>> >>>>>>>>>>>>>>>>>>>>>>>>>>>> >>> >>>>>>>>>>>>>>>>>>>>>>>>> >>>>>>>>>>>>>>>>>>>>>>>>>>>> >>>>>>5 AS S5555555555555555555 Lg >>>>>>>>>>>>> >>>>>>> >>>>>> 15 >>>>>>>>>>> >>>>>>>>>>> We >> >>>>>>° eS > SSS5 wee 13 12 GEOLOGICAL MAP OF BOW, NEW SOUTH WALES 1 KILOMETRE FIGURE 1 ° n= ° Proc. LINN. Soc. N.S.W., 104 (3), (1979) 1980 174 CAINOZOIC GEOLOGY AND FOSSIL FAUNA A combination of these three can be shown to have occurred at Bow (Fig. 2). The modern flood plain — designated A, — was formed by overlapping at least two previous flood plains during higher discharge levels or positive base level movements. This overlapping was caused by aggradation. These terraces — designated A, and A, — have a vertical stratigraphic relationship with the A, terrace and thus do not appear on Fig. 1. An older terrace, designated T,, is probably representative of a Pleistocene terrace no older than sixty thousand years (Warner, pers. comm.). It has been formed by the inset method (shown in Fig. 2), presumably accompanying a fall in the base level associated with the onset of glaciation. Poor preservation is due to weathering °09000000 00000009 KEY: Basalt basement. Channel lag conglomerate. [—_~=s«~Point bar and overbank deposits. Fog. 2. IDEALIZED DEVELOPMENT OF FLUVIAL GEOMORPHOLOGY ASSOCIATED WITH BOW CREEK. 1. Original flood plain; 2. Inset of A3 flood plain inside abandoned T1 flood plain; 3. Overlapping abandonment of A3 flood plain by A2 flood plain during river migration; 4. Overlapping abandonment of A2 flood plain by Al flood plain; 5. Renewed incision by river; 6. Present geomorphology. Incision has exposed older channel lag and flood plain sediments. Low discharge-level benches formed. Proc. Linn. Soc. N.S.W., 104 (3), (1979) 1980 Cc. G. SKILBECK 175 and the development of a soil cover. In some places, complete erosion of older fluvial deposits has resulted in renewed lateral incision of the basalt basement. The contemporary river regime is represented by the stream and its associated depositional and erosional activities. Deposition occurs on meander points, as lag in the channel and in times of flood, on the flood plain. Erosion occurs on the concave meander bank and where basement is exposed. Down-cutting through the older flood plains would indicate that erosion is the present dominant force. Channel sediment consists almost exclusively of well rounded pebbles and cobbles of basalt. The roundness of these pebbles is not indicative of transport mechanisms or distance, but is rather a feature of initial spheroidal weathering. Evidence for this can be seen in the basalts exposed in the road cutting below Bow Post Office (grid ref. 132016, Fig. 1). THE FOSSIL DEPOSITS AND THEIR RELATIONSHIP TO THE DEVELOPMENT OF BOW CREEK The deposits containing fragments of the fossil vertebrates crop out adjacent to Bow Post Office and occur within a slightly elevated region of weathered basalt. They occur as residual deposits (Warner, 1972, p. 10, fig. 3c), above the T, terrace. Out- crop in this road cutting is particularly sparse due to slumping and subsequent council efforts to reduce erosion by planting ‘pig face’ (Carpobrotus aequilaterus). A section of the southern bank of the road cutting is given in Fig. 3. The fossiliferous sediment is riverine and in section it is confined to channels, slightly convergent to the south with the modern creek. These channels may represent Pliocene perennial streams that did not develop laterally or that resulted from incised formation. However, evidence presented later does not favour the presence of a permanent body of water. The most probable interpretation of these sediments is that they represent ephemeral gully facies deposits. THE BOW FAUNAL ASSEMBLAGE The classification used herein follows those listed by Moore (ed.) (1957) for the Gastropoda and Bivalvia, Webb et al. (1975) for the Malacostraca, Romer (1971) for Idealized Section. Figure 3. ROAD CUTTING SECTION (SOUTHERN EXPOSURE) Map reference 132016 (figure 1). Horizontal scale —— Vertical X100. 100m Average slope of bank 41°. KEY: Basalt, weathered (in situ) [eo] Fossiliferous conglomerates, basalts weathered by transport. HH Soil profile. Proc. Linn. Soc. N.S.W., 104 (3), (1979) 1980 176 CAINOZOIC GEOLOGY AND FOSSIL FAUNA the Reptilia and Mahoney and Ride (1975) for the Marsupialia. Dental notation follows that used by Archer (1978). The sample number prefix ‘F’ denotes Australian Museum fossil specimens, while ‘QF’ applies to Queensland Museum fossil specimens. All measurements are in millimetres. The Bow fossil material, registered at the Australian Museum, can be summarized as follows: BIVALVIA HYRIINAE Ortman, 1911 Hydridella sp. cf. H. australis (Lamarck) CORBICULIDAE Gray 1847 Corbicula sp. GASTROPODA PLANORBIDAE Dybowski, 1903 Physastra sp. BITHYNIIDAE Gabbia sp. cf. G. australis, Tryon MALACOSTRACA DECAPODA Latreille, 1802 BRACHIURA Latreille Family indet. REPTILIA ANAPSIDA CHELONIA Family indet. MAMMALIA METATHERIA MARSUPICARNIVORA DASYURIDAE Waterhouse, 1838 Dasyurus sp. DIPROTODONTA VOMBATIDAE Iredale and Troughton, 1934 Phascolonus sp. THYLACOLEONIDAE Gill, 1872 Thylacoleo crassidentatus Bartholomai, 1962 DIPROTODONTIDAE Gill, 1872 PALORCHESTINAE Tate, 1948 Palorchestes sp. cf. P. parvus De Vis, 1895 NOTOTHERIINAE Stirton, Woodburne and Plane, 1967 Genus indet. MACROPODIDAE Owen, 1839 POTOROINAE Trouessart, 1898 Propleopus sp. MACROPODINAE Thomas, 1888 Macropus (Osphranter) sp. cf. M. (Osphranter) woodsi Bartholomai, 1975 Protemnodon chinchillaensis Bartholomai, 1973 Troposodon sp. cf. T. bluffensts Bartholomai, 1978 Genus indet. STHENURINAE Glauert, 1926 Sthenurus sp. The Bow fossil material consists largely of broken limb fragments with very rare Proc. Linn. Soc. N.S.W., 104 (3), (1979) 1980 C. G. SKILBECK 177 and always disassociated dentary and maxillary fragments. Recovery of fossil speciments is also difficult because of the clayey matrix of the sediment. Even after several washings the fossils are often still coated with fine sediment. DISCUSSION OF THE BOW FAUNAL ELEMENTS BIVALVIA and GASTROPODA Several entire and fragmentary shells have been recovered from the Bow fossil deposits. They also occur in the terrace deposits associated with the modern Bow Creek. Identification was made by Dr P. Colman of the Australian Museum. MALACOSTRACA Specimen F60120 represents brachiuran gastroliths. REPTILIA Fragments of tortoise shells (e.g. F60119) were among the most common fossils recovered. They cannot at present be referred to any particular genus although they do apparently represent relatively small chelonians. MAMMALIA MARSUPICARNIVORA DASYURIDAE Dasyurus sp. One specimen (F60112), a left dentary with M,-,, represents a species of Dasyurus. In molar morphology it resembles D. viverrinus, D. geoffrow (in Smith, 1972) and D. dunmalli (Bartholomai, 1971). The last named is known from the Pliocene Chinchilla Sand of Queensland and is distinguished by the presence of a single rooted P;. D. wverrinus and D. geoffrow are both only known from Pleistocene and modern deposits. The Bow Dasyurus is of the same size as all three of the above species, larger than D. hallucatus and smaller than D. maculatus. It also differs in molar morphology from the last two. Without information about the presence or absence of a P; the Bow specimen cannot be identified. DIPROTODONTA VOMBATIDAE Phascolonus sp. One specimen F59587 appears to represent a fragment of an upper incisor of a species of Phascolonus. Two species are known, P. gigas from the Pleistocene (and possibly Pliocene) and P. lemley: from the Pliocene (Archer zn Archer and Wade, 1976). At present lower incisors are required to distinguish the species and for this reason the Bow specimen cannot be more precisely assigned. THYLACOLEONIDAE Thylacoleo crassidentatus Bartholomai, 1962 This species is represented in the Bow fauna by F59593, a partial left mandibular ramus with roots of M;, alveoli for the posterior molar (s) , and an incomplete posterior root for P;. F59594, a left P;; and F59569, an incomplete right P;. Four genera and nine species of thylacoleonids have been named. Of these, four species, Mylodon australis, Thylacopardus australis, Thylacoleo owent and Thylacoleo robustus are Proc, Linn. Soc. N.S.W., 104 (3), (1979) 1980 178 CAINOZOIC GEOLOGY AND FOSSIL FAUNA generally considered to be synonyms of Thylacoleo carnifex. The status of the Pleistocene species of Thylacoleo is in doubt but a recent review by Archer (in preparation) suggests that on the basis of dental structure alone, all but one named Pleistocene species appear indistinguishable from T. carnifex. The only exception is T. hilli Pledge, which because of its very small size cannot be referred to any other known species. The age of T. hzllz is unknown, while T. crasstdentatus is Pliocene. The Bow thylacoleonid is not attributable to the genus Wakaleo, because of the more generalized structure of the cheektooth of species of Wakaleo, particularly the P;. Further, in Wakaleo the ratio of length of P; to M; is less than 1.5 (Clemens and Plane, 1974). In the Bow thylacoleonid this ratio is 2.8 which is in close accord with specimens of species of Thylacoleo. Bartholomai (1962) described Thylacoleo crassidentatus from the Pliocene Chinchilla fauna. He indicates that the most specifically useful diagnostic feature was the structure of P;. This tooth is much broader in T. crasstdentatus than it is in T. carnifex, particularly above the posterior root and the longitudinal convexity is much better developed in T. crasstdentatus than it is in T. carnifex. These features in F59594 and F59569 compare well only with T. crasstdentatus. The second lower molar in T. crassidentatus, although variably developed, is commonly proportionately larger than it isin T. carnzfex and the alveolus is partially divided in the former by a vertical ridge on the lateral wall (F59593 has the alveolus completely divided). Thylacoleo crassidentatus and T. carnifex appear to have had very similar dimensions, but it has been shown above that they have very distinct dental morphologies. The Bow thylacoleonid can only be referred to T. crass¢dentatus. DIPROTODONTIDAE PALORCHESTINAE ? Palorchestes sp. cf. P. parvus DeVis, 1895 A single, isolated right M,, F59595, recovered from Bow appears to represent a species of Palorchestes. Although the crown of this tooth is worn, it can definitely be placed in the subfamily. Woods (1958) described Palorchestes parvus as a smaller and more lightly built species than P. azael. The lower molars are morphologically similar, but the upper molars are distinct in detail. Upper molars are as yet unavailable from Bow and thus identification has been based on less diagnostically unique characters. The dimensions of the Bow palorchestid, 20.8 x 12.8 (Ms; length x width) place it within the range of P. parvus (Woods, 1958). However, the generic identification remains tentative because M; is not particularly diagnostic. It is even possible that it could represent P. painez which is otherwise only known from the Miocene Alcoota fauna of the Northern Territory (Woodburne, 1967). The age range of Palorchestes parvus is in some doubt. The Chinchilla fauna and its component of P. parvus are commonly regarded to be Pliocene in age (Archer and Bartholomai, 1978). However, Bartholomai (1977) has also reported this species from the Pleistocene Gore Cement Mills fauna of southeastern Queensland. NOTOTHERIINAE Several upper molars and a single incisor are referable to this subfamily. The characteristic ‘V’-shaped transverse valleys (Stirton et al., 1967) are best represented in F59596 and F59597. However, the most diagnostic tooth for both subfamilial and generic identification’is P;, and as yet, this tooth is unavailable from Bow. Molar structure alone has not enabled generic determination. Six nototheriine genera are currently recognized of which the generic status of ‘Euowenza’ is in doubt (Archer zn Archer and Wade, 1976). Proc. Linn. Soc. N.S.W., 104 (3), (1979) 1980 C. G. SKILBECK 179 MACROPODIDAE POTOROINAE Propleopus sp. A single, incomplete mandibular ramus recovered from Bow is referable to a small species of the genus Propleopus. It is referred to by Bartholomai (1972, p. 15, para. 4). A paper on this specimen is in preparation by J. A. Mahoney and W. D. L. Ride. MACROPODINAE Macropus (Osphranter) sp. cf. M. (Osphranter) woods Bartholomai, 1975 This macropodid is represented by many specimens (e.g. F59548 dentary and F59536 maxillary). Although definitely referable to the subgenus Osphranter (as described by Bartholomai, 1975) the Bow species differs from all members of the subgenus currently recognized. The anterior cingulum of M. (Osphranter) altus exhibits recurvature and the shape of the talonid is variable. M. (Osphranter) ferragus has differentially rotated lophids in the lower molars and M. (Osphranter) pan has accessory links in the talonid basin (Bartholomai, 1975). The Bow Osphranter is most comparable to M. (Osphranter) woods except that the Bow specimens are smaller than the average Chinchilla speciments described by Bartholomai (1975). Protemnodon chinchillaensis Bartholomai, 1973 This Pliocene species is represented by F59530, a left maxillary fragment with M?*; F59533, a left maxillary fragment with P?—M?; and F59540, an M®. Although the Bow material is very limited this material appears to be referable to Protemnodon chinchillaensis. This identification is based mainly on the morphology of P* (P* of Bartholomai 1973) which is proportionately very elongate, high crowned and has a very low lingual cingulum. Protemnodon chinchillaensts is the smallest member of the genus yet recovered in Australia and it is also a morphologically distinct species, having low cheektooth crown heights with more accessory ridging (Bartholomai, 1973) . All these features are present in the small Bow sample. Troposodon sp. cf. T. bluffensts Bartholomai, 1978 Numerous dentary specimens (e.g. F60108) represent a small species of Troposodon. In size and morphology it is clearly distinct from T. mznor and T. kentzz. It compares best with T. bluffenszs described recently by Bartholomai (1978) from the Pliocene Bluff Downs fauna of northeastern Queensland. Positive identification must await a more complete analysis of the as yet unassessed isolated upper molars from the Bow site. In addition, the isolated P, referred by Bartholomai to T. bluffenszs differs sufficiently from that tooth in a Bow dentary (F60108) to advise caution in referring the Bow material to this otherwise Queensland taxon. Genus indet. Several specimens (e.g. F59603) are not clearly referable to any known genus. They represent a form that exhibits some affinity with species of Wallabza, Troposodon and to a lesser extent, even Dorcopsis. At present it seems best to leave it unallocated at the generic level until more material has been collected. STHENURINAE Sthenurus sp. A single tooth appears to represent a right lower molar of a species of Sthenurus. In size it approximates with some of the S. (Sthenurus) species such as S. (Sthenurus) Proc. LINN. Soc. N.S.W., 104 (3), (1979) 1980 180 CAINOZOIC GEOLOGY AND FOSSIL FAUNA atlas but in morphology it suggests similarities to species of the subgenus Sitmosthenurus. More specimens must be found before it can be allocated confidently to a particular species. THE AGE OF THE BOW FAUNA Although the Bow faunal deposits occur in association with basalts (see above), an erosional hiatus of indeterminate span separates the basalts from the fossiliferous sediments. As a result, the estimate of Pliocene age for the Bow fauna is based on a faunal comparison with the Chinchilla and Bluff Downs faunas. The Bluff Downs fauna lies immediately below a basalt dated at about four and a half million years B.P. (Archer and Wade, 1976). Comparison of the Bluff Downs fauna with the Chinchilla fauna suggests a four to four and a half million year date for the Chinchilla fauna. Presence in the Bow fauna of Protemnodon chinchillaensts (Chinchilla), Troposodon sp. cf. T. bluffensts (Bluff Downs), Macropus (Osphranter) woodsi (Chinchilla), Thylacoleo crassidentatus (Chinchilla) and Palorchestes sp. cf. P. parvus (Chinchilla), and the apparent absence of forms only known from younger or older faunas, suggests that the Bow fauna is early to middle Pliocene in age. THE PALAEOENVIRONMENT While assessment of the palaeoenvironment is subject to the problems of extrapolation from the habitat requirements of related modern animals, some comment can be made in the light of evidence now available. Fish and crocodile remains are absent, to date, from the Bow deposits. These animals require a permanent aquatic habitat. An ephemeral body of water is indicated by freshwater invertebrate and tortoise remains. Tortoises can migrate subaerially and the invertebrates can invade the habitat temporarily from perennial streams. The majority of marsupial species so far identified from the Bow fauna are essentially browsing herbivores, such as Troposodon sp., Protemnodon chinchillaensts, Palorchestes parvus and Sthenurus sp. The apparent lack of many aboreal marsupials is probably the result of a sampling bias because most of the aboreal species are fairly small animals and, as yet, no sieving has been attempted at the site. The presence of Thylacoleo crassidentatus also may indicate that more work will reveal an aboreal component in the fauna because it may be inferred that this carnivore could have been aboreal (Wells and Nichol, 1977). ACKNOWLEDGEMENTS The work presented in this paper resulted from the author’s honours research at the University of Sydney during 1977. Special thanks are given to Mr Jack Mahoney for his suggestion of the topic and his supervision and encouragement throughout its duration. Gratitude is expressed to Dr Michael Archer of the University of New South Wales who assisted greatly in the preparation of this paper with his criticism of the content and identifications as well as in the drafting. Professor David Branagan assisted with the geology and also read the manuscript. Dr Alex Ritchie and Dr Phillip Colman of the Australian Museum allowed access to fossil collections and laboratory facilities and Dr Colman also identified the Invertebrate material. Finally, thanks are extended to Professor Graeme Philip of the Department of Geology and Geophysics at the University of Sydney for providing research facilities. Proc. LINN. Soc. N.S.W., 104 (3), (1979) 1980 Cc. G. SKILBECK 181 References ARCHER, M., 1978. — The nature of the molar-premolar boundary in marsupials and a reinterpretation of the homology of marsupial cheek-teeth. Mem. Qd Mus. 18:157-164. , and BARTHOLOMAI, A., 1978. — Tertiary mammals of Australia: A synoptic review. Alcheringa 2: 1- 19. ——, and Wank, M., 1976. — Results of the Ray E. Lemley Expeditions, Part 1. The Allingham Formation and a new Pleistocene vertebrate fauna from northern Queensland. Mem. Qd Mus. 17:379-397. BaRTHOLOMaI, A., 1962. — A new species of Thylacoleo and notes on some caudal vertebrae of Palorchestes azael. Mem. Qd Mus. 14:33-39. ——, 1971. — Dasyurus dunmalli, a new species of fossil marsupial (Dasyuridae) in the upper Cainozoic deposits of Queensland. Mem. Qd Mus. 16:19-26. ——, 1972. — Aspects of evolution of the Australian marsupials. Proc. R. Soc. Qd 82:v-xviil. ——, 1973. — The genus Protemnodon Owen (Marsupialia: Macropodidae) in the upper Cainozoic deposits of Queensland. Mem. Qd Mus. 16:309-363. ——, 1975. — The genus Macropus Shaw (Marsupialia: Macropodidae) in the upper Cainozoic deposits of Queensland. Mem. Qd Mus. 17:195-235. ——, 1977. — The fossil vertebrate fauna from Pleistocene deposits at Cement Mills, Gore, southeastern Queensland. Mem. Qd Mus. 18:41-50. ——, 1978. — The Macropodidae (Marsupialia) from the Allingham Formation, northern Queensland. Results of the Ray E. Lemley Expeditions, Part 2. Mem. Qd Mus. 18:127-144. BRANAGAN, D. F., HERBERT, C., and LaNGrorD-SmiTH, T., 1976. — An outline of the geology and geomorphology of the Sydney Basin. Marrickville (N.S.W.) : Science Press. CLEMENS, W. A. and PLANE, M. C., 1974. — Mid Tertiary Thylacoleonidae (Marsupialia: Mammalia). /. Paleont. 48 :652-660. GaLLoway, R. W., 1963a. — Geology of the Hunter Valley. C.S.J.R.O. Resources Series No. 8:81-89. ——, 1963b. — Geomorphology of the Hunter Valley. C.S.J.R.O. Resources Series. No. 8: 90-100. ——, 1967. — Pre-basalt, sub-basalt and post-basalt surfaces of the Hunter Valley, New South Wales. Pp. 239-314 zn JENNINGS, J. N., and MassutT, J. A. (eds), Landform studies from Australia and New Guinea. Canberra: A.N.U. Press. LEopoLD, L. B., WoLMAN, M. G., and MILLER, J. P., 1964. — Fluvial processes in geomorphology. San Francisco: W. H. Freeman. Manoney, J. A., and Ripe, W. D. L., 1975. — Index to the genera and species of fossil Mammalia described from Australia and New Guinea between 1838 and 1968. W. Aust. Mus. Spec. Publ. No. 6 Moore, R. C. (ed.), 1957. — Treatise on invertebrate paleontology. Vols J. & N. Lawrence, Kansas: University of Kansas Press. PackHaM, G.H. (ed.), 1969. — The geology of New South Wales. J. Geol. Soc. Aust. 16(1). Romer, A.S., 1971. — The Vertebrate Body (Shorter version) . 4th ed. Philadelphia: W. B. Saunders. SmitH, M. J., 1972. — Small fossil vertebrates from Victoria Cave, Naracoote, South Australia. II Peramelidae, Thylacinidae and Dasyuridae (Marsupialia). Trans. R. Soc. S. Aust. 96: 125-137. WARNER, R. F., 1972. — River terrace types in the coastal valleys of New South Wales. Aust. Geographer 12: 1-22. WEBB, J. E., WALLWoRK, J. A., and ELcoop, J. H., 1975. — A guide to invertebrate animals. London: Macmillan. WELLMAN, P., and McDouGcALt, I., 1974. — Potassium-Argon ages on the Cainozoic volcanic rocks of New South Wales. J. Geol. Soc. Aust. 21:247-272. —, McEtuinny, M. W. and McDouca tt, I., 1969. — On the polar wander path for Australia during the Cainozoic. Geophys. J. R. Astr. Soc. 18:371-395. WELLS, R. T., and NicHoL, B., 1977. — On the manus and pes of Thylacoleo carnifex Owen (Marsupialia). Trans. R. Soc. S. Aust. 101:139-146. WoopsurRn_E, M. O., 1967. — The Alcoota Fauna, central Australia. Bull. Bur. Miner. Resour. Geol. Geophys. Aust. No. 87. Woops, J. T., 1958. — The extinct marsupial genus Palorchestes Owen. Mem. Qd Mus. 13:177-193. Proc. Linn. Soc. N.S.W., 104 (3), (1979) 1980 The genus Razllzetza Trouessart in Australia (Acari: Dermanyssidae) ROBERT DOMROW Domrow, R. The genus Razllietza Trouessart in Australia (Acari: Dermanyssidae). Proc. Linn. Soc. N.S.W. 104 (3), (1979) 1980: 183-193. Razllietza, confined to the auditory meatus of mammals, is represented in Australia by three species. Supplementary descriptive notes are given for R. australis Domrow from a wombat, Vombatus ursinus (Shaw) (Marsupialia: Vombatidae) and R. auris (Leidy) from the cow, Bos taurus Linnaeus (Artiodactyla: Bovidae). R. manfredi, n. sp., is figured and described from the goat, Capra hzrcus Linnaeus (Bovidae: Caprinae). A key to the females of the five known species is given. R. Domrow, Queensland Institute of Medical Research, Bramston Tce, Herston, Australia 4006; manuscript received 9 November 1979, accepted 20 February 1980. INTRODUCTION Three species of Razllietca Trouessart are now known to occur in the ears of native and introduced mammals in Australia. The descriptions are completed of the somewhat atypical R. australis Domrow, both known series of which are from a marsupial, and of the widespread R. aurts (Leidy), a cause of otzt2s medza in cattle (Domrow, 1963; Ladds et al., 1972). A new species (R. manfredz) from the goat is yet another of the parasitic mites found only recently on domesticated animals [e.g. Trixacarus caviae Fain, Hovell and Hyatt, 1972 (Sarcoptidae) from the guinea-pig, and Lynxacarus radovskyt Tenorio, 1974 (Listrophoridae) from the cat]. The two other known species (R. hopkinsi Radford, 1938 and R. whartonz Potter and Johnston, 1978, both from African bovids) are beyond the scope of this paper, as is the genus Rhodacantha Domrow, 1979* from the ears of Australian dasyurid marsupials. The term ‘holotrichous’ refers to the setal condition in typical free-living dermanyssids (Evans and Till, 1965; Evans, 1969). The hosts’ names are given after Simpson (1945) and Ride (1970). Depositories are abbreviated: ANIC, Australian National Insect Collection, CSIRO, Canberra; BMNH, British Museum (Natural History), London; QIMR, Queensland Institute of Medical Research, Brisbane; RVL, Regional Veterinary Laboratory, Wollongbar. Genus RAILLIETIA Trouessart Raillietia Trouessart, 1902: 1335. Type-species Gamasus auris Leidy. The larval structures described below support Radovsky’s (1969) placement of the Raillietiinae in the Halarachninae. Evans and Till (1966) gave an extended diagnosis for Razlletza; additional characters may be culled from Zumpt and Till’s (1961) key. Key to females of Razllzetza Based in part on original descriptions. 1. Dorsal shield with 19 and 15 pairs of setae on *In this paper, read seta for setae at line 51, page 118; and Z,, for Z,_, at line 6, page 121. Proc. Linn. Soc. N.S.W., 104 (3), (1979) 1980 184 RAILLIETIA TROUESSART IN AUSTRALIA podonotal and opisthonotal portions, respectively. Trochanter I and femora I, III holotrichous. Tibia I with seta pv, added. From a vombatid (Miairs wpa) yt cr eee ec es eg rere australis Dorsal shield with 10 and at most seven pairs of setae on podonotal and opisthonotal portions, respectively. Trochanter I and femora I, III unideficient. Tibia I with seta pv, added or not. From: bovids (Artiodactyla) (727. (hy Gi kais He acres Ie aire Glen snl Sone yaaa 2 2. Dorsal shield with 17 pairs of setae. Tibiae — hypertrichouss Fromaacaprineiy cca erty lee cna cy etl manfredt Dorsal shield with at most 15 pairs of setae. Tibiae at most;holotrichous: Krom boOvids Gi sic oe eg rei 3 3. Dorsal shield with at least 13 pairs of setae. Tibia IV holotrichous. From species of Kobus Smith Dorsal shield with 12 pairs of setae. Tibia IV unideticient.“Fromiy Bos Wimnaeus ’: . 34680. ee i aera aurts 4. Dorsal shield with 15 pairs of setae. Genital setae on margin of genital shield. Setae on tarsus II 1X0) 60020 Lee Ar crs ee I NELGn yen eniny ome dem EMSA Ho a Narh ioe GTBNAVE iA Na el Arg .. hopkinst Dorsal shield with 13 pairs of setae. Genital setae free of margin of genital shield. Setae ad,_, on tarsus Ichypertrophied (yon a ia ee aes en Cananetiee whartoni Raillietza australis Domrow (Figs 13-14) Raillietia australis Domrow, 1961: 75; 1973: 79. Types. Holotype 2 and one paratype 2, in ears of common wombat, Vombatus ursinus (Shaw) (Marsupialia: Vombatidae), Brindabella Road, A.C.T.-N.S.W. border, 24.v.1960, J. H. Calaby. Holotype in ANIC, paratype in BMNH (both reexamined ). Other material. One 9, V. ursinus, near Taggerty, Vic., 26.vii.1971, R. C. H. Shepherd. In QIMR (reexamined) . Female. Add to original description [ Potter and Johnston’s (1978) setal counts for dorsal shield and tibia I are wrong]: Chelicerae, although still dorsoventrally orientated, now seen to be very similar to those of Mesolaelaps Hirst (see Tenorio and Radovsky, 1974) ; 270 um long overall, shaft 45 ym in diameter, with digits occupying 27% of total length; middle segment with distinct dorsal setule and lyriform pore (external lyriform pore not detected), and ventral corona; fixed digit with pilus dentilis short and stiff, outwardly directed, set between tip of digit (shaped to receive tip of movable digit) and single low tooth placed well beyond midlength of digit; movable digit subequal to fixed digit, 70-75 um long, with two low teeth placed just beyond midlength. Epistome lobate, with lightly serrate margin not reaching far beyond level of palpal trochanters; disc with extensive dendritic pattern. Labial cornicles ‘not very strong’ cf., say, the predatory Hypoaspis Canestrini, but actually well sclerotized ; internal malae a single triangle with fringed margin barely exceeding tips of labial cornicles; epipharynx minutely ciliated around marginal strip, longitudinally striate in midline; salivary stylets present; anteromedial extension [see Evans and Loots (1972, 1975); this is ‘labrum’ of Gorirossi Bourdeau (1956) | of Proc. LINN. Soc. N.S.W., 104 (3), (1979) 1980 R. DOMROW 185 Figs 1-5. Raillietia manfredi. 1. Capitulum 9, ventral (true right palp dorsal). 2. Epistome 9. 3. Chelicera 9, external. 4. Cheliceral digits J, ventrointernal. 5. Coxa III and insemination apparatus Q, dorsal. Scales = 100yum. subcheliceral shelf distinct, with tip variable [holotype with two blunt points, paratype with three blunt points ending at same level, cf. Mesolaelaps bandicoota (Womersley, 1956) and M. australzensts (Hirst) as figured by Tenorio and Radovsky (1974) ]. Palpi holotrichous: trochanter 2, femur 5, genu 6 (al,-, spatulate, al, absent on one side of paratype), tibia 14 (including two dorsodistal rods), tarsus 4 (plus terminal cluster of rods). All capitular setae, except the very shortest, barbulate along shaft (true also of setae on idiosoma and legs) . Dorsal shield [ Fig. 28 in Domrow (1961) represents paratype] 700-770 um long, 310-340 um wide, ratio length/width 2.26-2.30, distinctly granulate (except on muscle insertions), hypotrichous, probably with 34 pairs of setae in normal specimens; podonotal portion with 19 pairs (s,; absent on both sides of paratype and on one side of holotype, but present on both sides of Taggerty specimen) compared to normal 22 (i.e. lacking z3, s; and r, — if setae acquired at protonymphal, rather than at deutonymphal, stage are taken as more likely to be represented in a reduced species) ; opisthonotal portion with 15 pairs (S; absent on both sides of holotype, and S, on one side of Taggerty specimen) compared to normal 17 (i.e. lacking intercalary pX2-3) - Proc. LINN. Soc. N.S.W., 104 (3), (1979) 1980 186 RAILLIETIA TROUESSART IN AUSTRALIA Undivided portion of tritosternal laciniae lightly spiculate. Sternal shield of paratype with seta st, absent on one side. Insemination apparatus not detected. Metapodal shields in two pairs just behind basifemora IV, inner pair equalling accessory genital shieldlets in size, outer pair rather larger. Anterior portion of peritrematalia originally figured in dorsoventral orientation [Fig. 27 in Domrow (1961) represents holotype], but actually more flared, though free of vertex of dorsal shield. Leg setation holotrichous, with one exception: tibia I with fourth ventral seta (pur) added, i.e. 2-3/2.3/2.2 rather than 2-3/2.3/1-2 (pv,-2 absent on one side of paratype). Tarsus I with dorsodistal sensory islet occupying 20% of length of segment. Notes. It may be that this morphologically and zoogeographically distinct species (see key above) should be transferred from Razllietza (Halarachninae) to some laelapine genus near Mesolaelaps and Rhodacantha, whose hosts are also largely Australian marsupials rather than Old World artiodactyls. That is to say, in a complex so morphologically reduced and so little collected, the presence of seta pv, on tibia I, once believed peculiar to these two Australian genera but now known also to occur in Raillietta, may as well be an adaptation to a habitat merely shared by unrelated lines as an indication of real relationships. Fig. 6. Razllietia manfred 2. Idiosoma, dorsal. Scale = 100um. Proc. LINN. Soc. N.S.W., 104 (3), (1979) 1980 R. DOMROW 187 Raillietia aurts (Leidy) Gamasus auris Leidy, 1872: 138. Raillietia auris: Freund, 1910: 313; Tzimbal and Litvishko, 1955: 1229. Material. Eight 99, middle ear of domestic cattle, Bos taurus Linnaeus (Artiodactyla: Bovidae) , Townsville, Qld, 11.v.1972, D. B. Copeman. In QIMR. Female. Palpal trochanter-genu holotrichous, tibia bideficient (12, including two dorsodistal rods) . Insemination apparatus as in R. manfredz. Legs with following deviations from holotrichous condition — hypotrichous: trochanter I 1-0/3-1 (d lacking), femur I 2-5/3-2 (one pv lacking) , femur III 1-3/1-0 (pl lacking), tibia IV 2-4/2-1 (pl, lacking); hypertrichous: genu IV 2-5/1-2 (pl, added). Tarsus I with dorsodistal sensory islet occupying 25% of length of segment. Figs 7-14. Raillietia spp. (7-12, R. manfredi 9; 13-14, R. australis 9). 7. Idiosoma, ventral. 8. Peritrematalia. 9-10. Sternal shield, variants. 11. Genital shield, variant. 12. Anal shield. 13. Peritrematalia. 14. Anteromedial extension of subcheliceral shelf, variants. Scale = 100 um, except for Fig. 14 (25 um). Proc. Linn. Soc. N.S.W., 104 (3), (1979) 1980 188 RAILLIETIA TROUESSART IN AUSTRALIA Raillietia manfredi, n. sp. (Figs 1-12, 15-28) Types. Holotype 9, allotype db and five paratype 99, auditory meatus of domestic goat, Capra hircus Linnaeus (Artiodactyla: Bovidae), Lismore, N.S.W., vi.1978, R. W. Cook. Six paratype 99 and one paratype 0, auditory meatus of C. hzrcus, Byron Bay Lighthouse, N.S.W., vi.1978, R.W.C. One morphotype larva, auditory meatus of C. hircus, Tuncester, near Lismore, 17.viii.1979, R.W.C. In ANIC (holotype, allotype and morphotype) ; BMNH, QIMR, RVL (paratypes). Female. Chelicerae 175 yum long overall, with digits occupying 26% of total length; middle segment with distinct dorsal setule, dorsal and external lyriform pores, and ventral corona; fixed digit with only one distinct denticle in addition to tip, pilus dentilis apparently absent; movable digit 45 um long, with two external denticles at level of tip of fixed partner. Epistome hyaline, in shape of inverted U, barely reaching level of bases of palpal femora, with two or three small serrations distally. Basis capituli wider than long, with a few short lines of denticles in addition to eight stronger rows in deutosternum; setae c simple, slender, exceeding sides of basis (often broken off short, as are all setae on body and appendages, except the shortest). Hypostome with setae h,-3 subequal to c; cornicles not heavily sclerotized, but distinct (albeit somewhat irregular in outline) ; internal malae not clear; epipharynx as in R. australis; salivary stylets present; anteromedial extension of subcheliceral shelf not clearly seen (cf. R. australis above). Palpi strong; genu with lyriform pore dorsally, tarsus with bifid claw (n.b.: small seta immediately above claw is also tarsal) ; trochanter-genu holotrichous (al, on genu spatulate), tibia bideficient (two dorsodistal rods included), tarsus discrete, with usual few simple setae and terminal cluster of rods. Idiosoma saccate, size unavailable because of rupture during mounting procedure. Dorsal shield 585-640 ym long, 230-255 um wide (ratio L/B 2.51), poorly demarcated from investing strip of sclerotized cuticle, sides subparallel, ends broadly rounded; surface heavily marked by muscle insertions, otherwise granulate, with about 15 pairs of pores (anteriormost pair lyriform) ; podonotal portion hypotrichous, with 10 pairs of setae; opisthonotal portion hypotrichous, with seven pairs of setae (one J seta doubled on one side of one specimen). Dorsal cuticle largely hyaline, with about 12 pairs of setae and a few paired pores. Tritosternum fully formed, with ciliated laciniae just exceeding insertions of setae h; on capitulum. Presternal striae absent. Sternal shield longer than wide, with somewhat irregular margins (one specimen with small submedian fenestration at level of setae st,) ; surface minutely granulate, provided submarginally with three pairs of setae (st,;-3) and two pairs of pores (f;-2, P2 absent on one side of one specimen). Metasternal setae (mst) free in cuticle, without associated pores (p3) or shields. Genital shield small, drop-shaped; surface granulate, marked by muscle insertions, and with one pair of setae (g) touching on margins (well free of margin on one side of one specimen), but associated two pores and shieldlets free in cuticle; operculum shallow, but rayed, supported by two strong genital apodemes. Insemination apparatus visible as convoluted adductor canals arising from sclerotized prominences on posterior margins of coxae III. Ovum very large, 760-800 um long, 540-565 um wide, some containing fully developed larva. Anal shield terminal in engorged specimens, with cribrum encroaching onto dorsum; surface weakly granulate, with pair of pores laterally; anus and adanal setae (aa) well forward, postanal seta (pa) subequal to aa. Irregular endopodal and exopodal shieldlets present between and behind coxae. Metapodal shields present, but largely subcuticular. Ventral cuticle with about six pairs of setae and a few paired pores. Stigmata provided with stout Proc. Linn. Soc. N.S.W., 104 (3), (1979) 1980 R. DOMROW 1 ane SaaS Se al SES TT coll y as eS SS Y hl Py Figs 15-22. Raillietia manfredi @, legs. 15-16. 1, dorsal, and ventral and lateral setation. 17-22. I-IV, same presentation as I. Scale = Proc. LINN. Soc. N.S.W., 104 (3), (1979) 1980 189 190 RAILLIETIA TROUESSART IN AUSTRALIA peritremes that, while largely ventral, turn finally dorsad onto humeral promontories ; peritrematal shields anteriorly slightly expanded mesad, but free of dorsal shield and, posteriorly, of expodal shields IV. Legs slender, with following deviations from holotrichous condition — hypotrichous: trochanter I 1-0/3-1 (d lacking), femora I 2-3/1.2/2-2 (one pu lacking), III 1-2/1.1/0-0 (pl lacking) ; hypertrichous: genua III 2-3/1.2/1-1 (ad; added; individual variation: pl, at times also added), IV 2-3/1.3/0-2 (ad; and pl, added) ; tibiae I 2-3/2.3/2-2 (pu, added), II-IV 2-2/1.3/1-2 (II with pd; added; III with ad2, pd; and pl, added; IV with ad, added). Femora-genua I-II without any d seta unduly strengthened. Tarsus I with dorsodistal sensory islet occupying 25% of length of segment. Coxa II without spinose anterodorsal process in addition to usual two condyles. Ambulacra with two claws and pulvillus. Male. Capitulum as in 9, except for slightly stronger setae on palpal trochanter-tibia and secondary sexual characteristics of chelicerae. Shafts thicker and more heavily sclerotized, but proportions unavailable because of foreshortening; fixed digit Figs 23-25. Raillietia manfredi 3. 23. Idiosoma, ventral. 24-25. Leg II, dorsal and posterolateral, and ventral and anterolateral setation. Scales = 100 um. Proc. Linn. Soc. N.S.W., 104 (3), (1979) 1980 192 RAILLIETIA TROUESSART IN AUSTRALIA obsolescent, but dorsal setule and at least external lyriform pore present; spermatodactyl strongly bidentate, apart from tip, ca 85 um long. Idiosoma saccate, of uncertain size. Dorsum as in 9, except that dorsal shield is wider, 605-615 um long, 260-265 um wide (ratio L/B 2.33) (seta J, doubled on one side of one specimen) . Sternogenital shield with cornua slight, genital aperture in midanterior margin; strongly sclerotized laterally between coxae III-IV, otherwise granulate, except for weak reticulations on genital portion; with five pairs of setae and two pairs of pores as in 9 (one mst seta absent on one side of one specimen). Venter otherwise essentially as in 9. Legs with same setational formulae as in 9, with some individual variation: one specimen with femur III 1-2/1.2/0-0 (pd, added, pl lacking) on one side and tibia I 2- 3/2.3/1-2 (holotrichous) on both sides. Legs I, III-IV slender, II incrassate, with pv,-2 on femur, av and pv on genu-tibia, and (to varying extent) av,-3 on tarsus strengthened and set on prominences (av,-, on tarsus also strongly inflated basally) . Nymphs. Unknown. Larva. Chelicerae 100 um long overall, with digits occupying 25% of total length; middle segment with dorsal setule and external lyriform pore, but dorsal pore and corona not detected ; digits edentate, pilus dentilis apparently absent. Epistome as in Q, but margin almost smooth. Basis capituli as long as its maximum width, deutosternal details not clear. Hypostome with setae h,-, subequal; cornicles pale, but distinct; other hypostomatal structures not clear. Palpi strong, genu without lyriform pore dorsally, tarsus with bifid claw; trochanter-tibia holotrichous (a/, on genu slightly spatulate) , tarsus much as in 9. Idiosoma ovate, 650 wm long, 405 wm wide. No distinct shield evident, but dorsum with at least five pairs of pores; podonotal portion holotrichous, with 10 pairs of setae; opisthonotal portion hypotrichous, with four pairs of setae. Tritosternum fully formed. No distinct shields evident on venter. Setae st,-3 subequal. Setae aa flanking anus, only slightly shorter than pa, with strong tendency to elongation as in other halarachnine larvae, e.g. Halarachne Allman and Orthohalarachne Newell (see Domrow, 1962, 1974). Ventral cuticle with three pairs of lateral setae in addition to usual three pairs of midventrals and pair flanking anal complex ; with metapodal traces and duct-like structures seen in Orthohalarachne. Legs holotrichous, otherwise much as in 9. Notes. This is the first species of Razllzetza to be described from a caprine rather than a bovine member of the family Bovidae. ACKNOWLEDGEMENTS I thank Dr R. W. Cook, RVL, for the chance to study the new species; ANIC and BMNH for the loan of specimens; Mr D. C. Lee, South Australian Museum, Adelaide, for helpful comment; and Miss Cobie Rudd for pencilling the illustrations. References Domrow, R., 1961. — New and little-known Laelaptidae, Trombiculidae and Listrophoridae (Acarina) from Australasian mammals. Proc. Linn. Soc. N.S.W., 86: 60-95. ——, 1962. — Halarachne miroungae Ferris redescribed (Acarina: Laelaptidae). Paczf. Insects, 4: 859- 863. ——, 1963. — New records and species of Austromalayan laelapid mites. Proc. Linn. Soc. N.S.W., 88: 199-220. Proc. Linn. Soc. N.S.W., 104 (3), (1979) 1980 R. DOMROW 193 ——, 1973. — New records and species of Laelaps and allied genera from Australasia (Acari: Dermanyssidae). Proc. Linn. Soc. N.S.W., 98: 62-85. ——, 1974. — Notes on halarachnine larval morphology and a new species of Pneumonyssus Banks (Acari: Dermanyssidae). J. Aust. ent. Soc., 13: 17-26. ——, 1979. — New dermanyssid mites from the ear canal of Australian dasyurid marsupials. J. Aust. ent. Soc., 18: 115-121. Evans, G. O., 1969. — Observations on the ontogenetic development of the chaetotaxy of the tarsi of legs II-IV in the Mesostigmata (Acari). Proc. II int. Congr. Acar. (1967), 195-200. , and Loots, G. C., 1972. — Scanning electron microscopy in the study of the gnathosoma of the Acari. Wetensk. Bydr. Potchefstroom Univ. C.H.O., Reeks B, Natuurw., 49: 1-13. ——, 1975. — Scanning electron microscope study of the structure of the hypostome of Phityogamasus, Laelaps and Ornithonyssus (Acari: Mesostigmata).J. Zool., Lond., 176: 425-436. ——, and TILL, W. M., 1965. Studies on the British Dermanyssidae (Acari: Mesostigmata). Part I. External morphology. Bull. Br. Mus. nat. Hist., Zool., 13: 247-294. ——, 1966. — Studies on the British Dermanyssidae (Acari: Mesostigmata). Part II. Classification. Bull. Br. Mus. nat. Hist., Zool., 14: 107-370. Fain, A., Hove, G. J. R., and Hyatt, K. H., 1972. — A new sarcoptid mite producing mange in albino guinea-pigs. Acta zool. path. antverp., 56: 73-81. FREUND, L., 1910. — Zur Kenntnis der Ohrmilbe des Rindes. Zool. Jb., Syst., 313-332. GoriRoss! BOURDEAU, F., 1956. — The gnathosoma of Megalolaelaps ornata (Acarina-Mesostigmata- Gamasides). Am. Midl. Nat., 55: 357-362. Lapps, P. W., Copeman, D. B., Dantes, P., and TRuEMAN, K. F., 1972. — Razllietta auris and otitis media in cattle in northern Queensland. Aust. vet. J., 48: 532-533. Leipy, J., 1872. — Note on Gamasus of the ox. Proc. Acad. nat. Sct. Philad., (3) 2: 138. Potter, D. A., and JoHNsTON, D. E., 1978. — Razllietza whartoni sp. n. (Acari: Mesostigmata) from the Uganda kob. J. Paraszt., 64: 139-142. RaprorD, C. D., 1938. — Notes on some new species of parasitic mites. Parasztology, 30: 427-440. Rapovsky, F.J., 1969. — Adaptive radiation in the parasitic Mesostigmata. Acarologza, 11: 450-483. Ripe, W. D. L., with drawings by Fry, E., 1970. — A guide to the native mammals of Austrulza. Melbourne: Oxford University Press. Simpson, G. G., 1945. — The principles of classification and a classification of mammals. Bull. Am. Mus. nat. Htst., 85: 1-350. Tenorio, J. M., 1974. — A new species of Lynxacarus (Acarina: Astigmata: Listrophoridae) from Felzs catus in the Hawaiian Islands. J. med. Ent., 11: 599-604. , and Rapovsky, F. J., 1974. — The genus Mesolaelaps (Laelapidae: Mesolaelapinae, n. subfam.) with descriptions of two new species from New Guinea. /. met. Ent., 11: 211-222. TROUESSART, E. L., 1902. — Deuxiéme note sur le Gamasus auris, type d’un genre nouveau (Raillzetza). C. r. S€anc. Soc. Biol., 54: 1335-1337. TzimBAL, T.G., and LitvisHko, N. T., 1955. — [Acariasis of the ear in cattle]. Zool. Zh., 34: 1229-1241. WonmersLey, H., 1956. — On some new Acarina-Mesostigmata from Australia, New Zealand and New Guinea. Linn. Soc. J., Zool., 42: 505-599. ZumPT, F., and TiLL, W. M., 1961. — Suborder: Mesostigmata. Publs S. Afr. Inst. med. Res., 9: 17-91. Proc. Linn. Soc. N.S.W., 104 (3), (1979) 1980 Structural Relationships across the Lambian Unconformity in the Hervey Range-Parkes Area, N.S.W. C. MCA. POWELL, C. L. FERGUSSON and A. J. WILLIAMS PoweELL, C. MCA., Fercusson, C. L., & Wittiams, A. J. Structural relationships across the Lambian Unconformity in the Hervey Range-Parkes area, N.S.W. Proc. Linn. Soc. N.S. W. 104 (3), (1979) 1980: 195-210. Detailed mapping of the structural relationships in four areas on the flanks of the Hervey and Parkes Synclines shows that the angular discordance between ?Silurian and Lower Devonian rocks and the overlying Hervey Group is very low in the north and increases southward. Comparison of the structural style of the Hervey and Parkes synclines with synclines in rocks of similar facies from other areas in the northern Lachlan Fold Belt shows that the latest Devonian to Early Carboniferous folding is less intense in the Hervey Range-Parkes area than in the eastern Lachlan Fold Belt, but more marked than the gentle warping further west. Mid-Devonian folds in the Hervey Range-Parkes area, if present, were open to gentle, and trended north-northeast. C. McA. Powell, School of Earth Sciences, Macquarie University, North Ryde, Australia 2113, C. L. Fergusson, Department of Geology, University of New England, Armidale, Australia 2351 (formerly School of Earth Sciences, Macquarie University)and A. J. Willams, Agnew Mining Company, P.O. Box 22, Leinster, Australia 6437 (formerly Department of Geology, Australian National University, Canberra) ; manuscript received 21 March 1979, accepted in revised form 23 April 1980. INTRODUCTION The Lambian Unconformity (Powell and Edgecombe, 1978, p. 166) in the northern Lachlan Fold Belt separates an upper well-bedded, quartzose, terrestrial to shallow-marine succession of sandstone and conglomerate from a lower succession that varies from graded-bedded sandstone and shale to massive silicic volcaniclastics and granitic rocks. The lower parts of the quartzose upper succession, variously known as the Lambie, Catombal, Hervey, Cocoparra and Mulga Downs Groups in the northern Lachlan Fold Belt (Conolly, 1965, 1969) range in age from latest Early or early Middle Devonian in the basal Mulga Downs Group (Ritchie, 1973) to Late Devonian in the lower marine part of the Lambie Group (Roberts et al., 1972). The upper parts of the succession may well extend into the earliest Carboniferous. The underlying rocks vary in age depending on the lacuna across the unconformity; in places, they are Early Devonian and elsewhere are as old as Ordovician. The structural relationships across the Lambian Unconformity have been mapped to determine the relative importance of deformations before, and after, deposition of the quartzose succession (Powell and Edgecombe, 1978; Powell and Fergusson, 1979a,b). By considering areas where the underlying rocks are no older than earliest Devonian, or, if older, where they can be shown to be conformable into the earliest Devonian, the relative importance of mid-Devonian and latest Devonian to Early Carboniferous deformation across the Lachlan Fold Belt may be compared. Mechanically, the upper quartzose succession is less ductile, and has a higher ductility contrast, than most of the underlying rocks, with the exception of areas of granite and multiply-deformed volcanics that may act as rigid masses in subsequent deformations (e.g. the Ordovician Sofala Volcanics, Powell et al., 1978). The Proc. Linn. Soc. N.S.W., 104 (3), (1979) 1980 196. LAMBIAN UNCONFORMITY See J Pe Se LEGEND eal Hervey Group ~~~ Lambian Uncontormity Mid - Yeoval Devonian + granites Bee Bumberry Eugowra Di[v - Unit C r (86:9m) LIMESTONE 50 USGD 85219 Unit B AMu 60129 | FP Gat saseea mire AMu 60131 ® +30 USGD 85218 E AMu_ 69130 £F20 o = }10 oO 7) bana : O Unit A Fig. 2. Stratigraphic section through the Mount Frome Limestone showing location of specimens and informal faunal subdivisions of the Limestone. fasciculate species which should possibly be separated on the basis of growth form at the generic level. However, it is also possible that genus-level taxa in this group ought to include a wide variety of growth forms as many species-level taxa [e.g. P. (Pleurodictyum) cylindricum (Michelin): Stumm, 1964, pl. 71, figs 1-5] are themselves quite variable. In particular, it is far from clear whether flattened colonies are generically distinct from more upright colonies approaching hemispherical form. Jones (1944) has discussed the problems generated by differing preservation in relation to Michelinia and Pleurodictyum. Many Pleurodictyum, such as are common in the Rhenish facies, occur as moulds and are discoidal colonies; these seem distinct from erect forms such as Pleurodictyum bifidum Jones, 1944 and many of the forms described by Stumm (1964) , especially those which are many-celled colonies. The problems created by varied preservation take on two main aspects. Firstly we have the matter of comparison of observed overall shape of the corallum; secondly there is the problem of comparison of detailed structures, often obscured by silicification and largely absent in moulds (e.g. septal microstructure). We believe these are separate problems as their results are felt at different taxonomic levels. The problem of preservation is an acute problem exemplified by the contrast between ‘typical’ Rhenish Pleurodictyum (almost always preserved as moulds) and the abundant North American materials (e.g. Stumm, 1964) (generally calcareous or silicified) . One result is considerable doubt as to the generic and subgeneric status of the Pleurodictyum problematicum Goldfuss (and Pleurodictyum megastoma McCoy) Proc. Linn. Soc. N.S.W., 104 (3), (1979) 1980 214 EARLY DEVONIAN TABULATE CORAL group compared with larger colonial forms such as P. bifidum Jones, 1944, P. (Pleurodictyum) maximum (Troost) and some other forms described by Stumm (1964). It may be that mould material referred to Procterza by Plusquellec (1965) and Clezstopora by Plusquellec (1966) will be eventually referred to Pleurodictywm when the importance of fine morphological features can be evaluated. Some unfortunate results of poor and good preservation might finally be noted. Concerning the former, the literature is replete with instances of probably indeterminate, broadly ‘favositid’ material preserved as moulds and referred (we believe erroneously in many cases) to Pleurodictyum. Conversely, well-preserved calcareous material described as a new tetracoral genus Arazostrotion (Guo, 1965) is probably a Pleurodictyum (see also Weyer, 1973). Subfamily Holacanthoporinae Le Maitre, 1957 Holacanthopora Le Maitre, 1954, p. 1668 Type Species. Michelinia (Ethmoplax) fascialis Le Maitre, 1952, p. 80, pl. 4, figs 3-6. Diagnosis. Large-celled fasciculate and cerioid Tabulata with abundant acanthine septa ; tabular floors weakly convex to weakly concave; mural pores located at or near wall junctions (new diagnosis) . Remarks. In addition to the type species, Le Maitre (1959) also placed i in this genus H. gracilis Le Maitre, 1954 (nom. nud.) and H. erregularts Le Maitre, 1957 (nom. nud.). The genus ranges from Emsian to Givetian (Le Maitre, 1959 p. 147). H. trregularts is known from the Emsian (Le Maitre, 1959, p. 203) and H. fascialis is known from the early Couvinian (Le Maitre, 1952, 1954, 1959). H. graczls ranges from the early Couvinian to early Givetian (Le Maitre, 1959, ps 203) Michelinia and Holacanthopora differ as the former lacks acanthine septa. Only in Michelinza varia Pickett (1967, p. 34) have ‘. . . very short septal spines . . .’ been described, projecting into the lumen; it remains to be seen whether truly acanthine septa are widespread in European Michelinia. Some similarities may be noted between Holacanthopora and Pseudoroemeria Chekhovich, 1960. The type species, P. atbashiensts Chekhovich, 1960, is partly cerioid and has mostly horizontal or oblique tabulae which Hill and Jell (1970, p. 185) consider favositoid. P. pulchra (Dubatolov, 1969, pl. X, figs 2a-b; 1971, pl. 5, figs la- b) has thickened walls (as in Roemertpora) and prominent mural pores which profoundly affect the tabulae. In this latter feature the Russian species differs markedly from the North African and Australian species. Holacanthopora clarke: Wright & Flory, sp. nov. ‘Fig. 3A-F; Fig. 4A Diagnosis. Wholly cerioid Holacanthopora with corallites up to 6.5 mm in diameter; up to about 10 acanthine septa on each wall; calical floors more or less horizontal, consisting of globose tabulae. Etymology. The species is named after Rev. W. B. Clarke who was apparently the first to record the Devonian age of the limestones at Mount Frome (Clarke, 1878, p. 16), Fig. 3. Holacanthopora clarkei Wright & Flory, sp. nov. Mount Frome Limestone, Early Devonian, near Mudgee, New South Wales. A, B, C, holotype USGD 85218; A, transverse section, x2.5. B, longitudinal section, x1.5. C, longitudinal section showing mural pores, x4. D, AMu 60131, longitudinal section, x2. E, F, USGD 85219; E, transverse section, x2.5. F, longitudinal section, x3.5. Both E and F show the abundant septal spines. Specimens bearing USGD are in the collections of the Department of Geology and Geophysics, University of Sydney; AMu denotes specimens in the Australian Museum collections. Proc. LINN. Soc. N.S.W., 104 (3), (1979) 1980 A.J. WRIGHT ANDR. A. FLORY 215 > Proc. Linn. Soc. N.S.W., 104 (3), (1979) 1980 216 EARLY DEVONIAN TABULATE CORAL probably based on fossils (especially Catceola) collected by Professor A. M. Thomson (Taylor, 1879). Material. 6 specimens, whose stratigraphic distribution is shown in Fig. 2. Holotype USGD 85218 (slides WW 190-191) ; paratypes USGD 85220 (slides W 220-221-222) ; USGD 85219 (slides W 497-498); AMu 60131 (slides WW 1-5 _ inclusive) ; AMu 60129 (slide WW 192) ; AMu 60130 (slides WW 193-194), all from the Mount Frome Limestone. Description. Colony cerioid, approximately spherical and up to at least 12 cm in diameter. Even at colony rim, corallites polygonal, although walls often curved; corallites up to 6.5 mm in maximum diagonal diameter. Walls up to 0.8 mm in total thickness with thin dark median structure (presumably primary) which bifurcates in places but elsewhere has beaded, discontinuous appearance (presumably recrystallization) . Stereozone contains up to 10 (usually about 7) septa on each wall. Mural pores about 0.5 mm in diameter mostly located at or near wall junctions; their vertical arrangement apparently in single series. Calices about 5 mm in depth, with subhorizontal floors. Increase intermural (Fig. 4A), at junctions of 3 or more corallites. At inner edge, stereozone denticulate, with short (up to 1 mm in length) septa with rounded or angular axial ends in transverse section which are weakly distally concave and distally inclined at low angle. Septa contain slender holacanths set in lamellar calcite and extend to median axial structure of wall. Longitudinal sections show acanthine septa (Fig. 3F). Tabular floors weakly convex to weakly depressed (with no sign of syrinx), formed by weakly convex to weakly concave, subhorizontal to gently inclined incomplete plates (tabellae) . Spacing often up to 1 mm. Rarely septal spines on these plates. Comparisons. Le Maitre (1957, 1959) assigns three species to Holacanthopora, viz. H. fasczalis Le Maitre, 1952; H. crregularis Le Maitre, 1957 (nom. nud.) and H. gracilis Le Maitre, 1954 (nom. nud.). Of the three Northern Hemisphere species placed in this genus, only H. fasczalzs can be usefully compared (and then only in its size and internal morphology) with H. clarket. A major difference is that, whereas clarkez is cerioid, fasctalis 1 is fasciculate (Le Maitre, 1952, p. 80). In addition, corallite increase in clarkez is intermural but in fascialis is lateral. Le Maitre (1957) states that H. gracilis and H. irregularis are cerioid species. In graczlzs the colony diameter is 7 mm (Le Maitre, 1954, p. 1668) and in zrregularts the corallite diameter is 4 mm (Le Maitre, 1957). Some general similarity with Michelinza is evident, but Holacanthopora is distinguished from Michelznia in possessing acanthine septa (see above). Devonian tabulate corals from many parts of the world have been assigned to Michelznza, but these reports probably require reassessment ; a noteworthy occurrence in this regard is the cerioid M. transttoria (Knod, 1908) from the Lower Devonian of Bolivia (Barthel and Barth, 1972). Sokolov (1962, p. 226) gives the range of the genus as Lower, Middle and Upper Devonian as well as Carboniferous. Remarks. The only similarly large-celled cerioid tabulate coral common in earlier Devonian limestones in New South Wales is Roemeripora progenitor (Chapman) Fig. 4. A, Holacanthopora clarkei Wright & Flory, sp. nov. Mount Frome Limestone, Early Devonian, near Mudgee, New South Wales; USGD 85219, transverse section, x6, showing wall structure, septal spines and mural pores. B, C, Roemeripora progenitor (Chapman), USGD 88216, Jesse Limestone, Limekilns, New South Wales, Early Devonian; B, transverse section, x3. C, longitudinal section, x3. D, E, Pleurodzctyum bifidum Jones, holotype USGD 6251, ‘Garra Beds’, near Wellington, New South Wales, Early Devonian; D, transverse section, x5. E, longitudinal section, x5. Proc. Linn. Soc. N.S.W., 104 (3), (1979) 1980 217 A.J. WRIGHT AND R. A. FLORY (1979) 1980 ’ Soc. N.S.W., 104 (3) Proc. LINN. 218 EARLY DEVONIAN TABULATE CORAL (Hill and Jell, 1970), clearly a roemeriporid (syringoporid) (Fig. 4B-C). Despite the similar wall structure, the nature of the tabulae argues against any phylogenetic relationship between progenztor and clarket. The rare Pleurodictyum bifidum Jones, 1944, from New South Wales differs from H. clarkez in possessing distant, complete and flattish tabulae (Fig. 4D-E), but probably should be placed in Holacanthopora and could be ancestral to clarkez; both species have abundant septal spines. ACKNOWLEDGEMENTS This work is part of a continuing study of Devonian biostratigraphy generously supported by ARGC grants to A. J. Wright. References BARTHEL, K. W., and BaRTH, W., 1972. — Palecologic specimens from the Devonian of Bolivia. Neues Jb. Geol. Paldont. Mh. : 573-581. CHEKHOVICH, V. D., 1960. — Pseudoroemeria, a new genus of the family Syringolitidae (Tabulata). Paleont. Zh., 1960, 4: 43-47 [Russian ]. CLARKE, W. B., 1878. — Remarks on the Sedimentary Formations of New South Wales (4th ed.) . Sydney: Government Printer. DuBaToLov, V.N., 1969. — Tabulata and biostratigraphy of the early Devonian of North-eastern S.S.S.R. Trudy Inst. Geol. Geoftz. sib. Otd., 70: 1-176 [ Russian ]. ——, 1971. — Taxonomic significance of the microstructure of the skeletal parts of Tabulata, p. 12-33 zn DusaToLov, V.N. (ed.) Paleozoic Tabulate and Heliolitocdea of the U.S.S.R. Papers of the I All- Union Symposium on fossil corals in the U.S.S.R., vol. 1 [ Russian ]. Guo, Sheng-Zhe, 1965. — Notes on a new genus of rugose coral — Arazostrotion from the Silurian of Dongwu-Qi region, Inner Mongolia. Acta palaeont. sin., 13: 650-653. [Chinese, English version 653-654. | Hit, D., and JeLi, J. S., 1970. — The tabulate coral families Syringolitidae Hinde, Roemeriidae Po€ta, Neoroemeriidae Radugin and Chonostegidae Lecompte, and Australian species of Roemeripora Kraicz. Proc. R. Soc. Vict., 83: 171-190. Jones, O. A., 1944. — Tabulata and Heliolitida from the Wellington district, N.S.W. J. Proc. R. Soc. N.S.W., 77: 33-38. Knop, R., 1908. — Beitrage zur Geologie und Palaontologie von Sudamerika. XIV. Devonische Faunen Boliviens. Neues Jb. Miner. Geol. Palaont. Beil. Bd., 25: 495-600. LE Maitre, D., 1952. — La faune du Dévonien inférieur et moyen de la Souara et des abords de |’Erg el Djemel (Sud-Oranais). Matériaux pour la Carte géologique de l’Algérie. 1'* Série. Paléontologie. Nr. 12: 1-170. ——, 1954. — Présence d’une microstructure du type Acanthiné chez des Tabulés dévoniens du Sud- Oranais: Holacanthopora, nov. gen. C.r. hebd. Séanc. Acad. Sct., Paris, 238: 1668-1670. —, 1957. — Polypiers tabulés dévoniens & structure Acanthinée. C.r. hebd. Séanc. Acad. Sct., Paris, 244; 369-371. —— , 1959. — Remarques sur trois genres de Tabulés: Holacanthopora, Pleurodictyum et Roemeria. C.r. somm. Séanc. Soc. géol. Fr., 1959, 6: 147-148. [Errata p. 203]. Puitip, G. M., 1974. — Biostratigraphic procedures and correlations in the Tasman Geosynclinal Zone, zn DENMEAD, A. K., TWEEDALE, G. W., and Witson, A. F. (eds) The Tasman Geosyncline — A Symposium, pp. 295-310. Geol. Soc. Aust. : Queensland Division, Brisbane. PicKETT, J., 1967. — Lower Carboniferous coral faunas from the New England district of New South Wales. Mem. geol. Surv. N.S.W. (Palaeont.) 15: 1-38. ——, 1978. — Conodont faunas from the Mount Frome Limestone (Emsian/Eifelian) , New South Wales. Bull. Bur. Miner. Resour. Geol. Geophys. Aust., 192: 97-107. PLUSQUELLEC, Y., 1965. — Le genre Pleurodictyum Goldfuss et genres morphologiquement voisins du Dévonien du synclinorium médian amoricain. Trav. Lab. Géol. Coll. Sct. Univ. Brest (Paléontologze) : 1-90. ——, 1966. — Le genre Cleistopora Nicholson 1888 dans le Dévonien du Finistére. Trav. Lab. Géol. Coll. Sct. Univ. Brest. (Paléontologie) : 1-14. Proc. LINN. Soc. N.S.W., 104 (3), (1979) 1980 A.J. WRIGHT ANDR. A. FLORY 219 SoxoLov, B. S. (ed.), 1962. — Fundamentals of Paleontology. Vol. II. Porifera, Archaeocyatha, Coelenterata, Vermes. 1-485 [Russian ]. StumM, E. C., 1964. — Silurian and Devonian corals of the Falls of the Ohio. Mem. geol. Soc. Amer., 93: 1-184. Taytor, N., 1879. — On the Cudgegong diamond field, New South Wales. Geol. Mag. dec. II, 6: 399-412, 444-458. WeyER, D., 1973. — Uber den Ursprung der Calostylidae ZiTrEL 1879 (Anthozoa Rugosa, Ordoviz-Silur) . Freiberger ForschHft. (Reihe C) 282: 23-87. WricHT, A. J., 1966. — Cerioid Stringophyllidae (Tetracoralla) from Devonian strata in the Mudgee district, New South Wales. Proc. Linn .Soc. N.S.W., 90: 263-273. Proc. Linn. Soc. N.S.W., 104 (3), (1979) 1980 PROCEEDINGS of the LINNEAN SOCIETY NEW SOUTH WALES VOLUME 104 NUMBER 4 A new species of the ulysses group, genus Haemolaelaps Berlese (Acari: Dermanyssidae) ROBERT DOMROW Domrow, R. A new species of the ulysses group, genus Haemolaelaps Berlese (Acari: Dermanyssidae). Proc. Linn. Soc. N.S.W. 104 (4), (1979) 1980 :221-227. Haemolaelaps sisyphus, n. sp., a much reduced member of the Australian wlysses group, is figured and described from the nasal passages of the brush-tailed possum, Trichosurus vulpecula (Kerr) (Marsupialia: Phalangeridae) , in New South Wales. A key to the eight known species is given. R. Domrow, Queensland Institute of Medical Research, Herston, Australia 4006; manuscript recerved 8 January 1980, accepted 23 April 1980. The distinctive new species of Haemolaelaps Berlese now described is the eighth member of the peculiarly Australian wlysses group, the history and host relationships of which can be gleaned from the following key. Two further references are Domrow (1979, 1981). In brief, four of the species (those with seta pl, added on genu IV, as often in Haemolaelaps) are from non-petaurid hosts, while the holotrichous four (those lacking pl,) are all from petaurids. The latter four comprise two pairs, each pair from a non-gliding host and its gliding equivalent (Ride, 1970). Terminology is after Evans and Till (1965), except for tarsi II-IV (Evans, 1969), the word ‘holotrichous’ referring to the setal condition in free-living dermanyssids. Measurements are in micrometres. Genus HAEMOLAELAPS Berlese Haemolaelaps Berlese, 1910: 261. Type-species Laelaps (Haemolaelaps) marsuptalis Berlese. Key to females of species of ulysses group, Haemolaelaps 1. Genu IV with seta pl, added (if pl, lacking, Goaalsolacking): From: non-petaunds 2... 294 fos ess ee 2 Genu IV holotrichous (pd; present). From petaurids 2. Dorsal shield with setae z;. Sternal shield with distinct cornua between coxae I-II. Metapodal shields enlarged. From Rattus fuscipes (Waterhouse) (Rodentia: INA UTA FY) AAR ERT EAS SP ee RM ater rs sre RIE Tea laertes Domrow, 1972a Dorsal shield lacking setae z3. Sternal shield without exaggerated cornua. Metapodal shields normal 3. Dorsal shield with minute setae; holotrichous at J, (and elsewhere, except at Z3). From Antechinus flavipes (Waterhouse) and A. stuartzi Macleay (Marsupialia: 1 DEES ADING KES). SMe OE rn an aN An os a) arse OR telemachus Domrow, 1964 Proc. Linn. Soc. N.S.W., 104 (4), (1979) 1980 222 ; A NEW SPECIES OF HAEMOLAELAPS Dorsal shield with normal setae; hypertrichous at J, (if holotrichous, both podonotal and opisthonotal portions markedly hypotrichouselsewhere)) 325-4 oo soca ee ree 4 4. Palpal tibia holotrichous. Dorsal shield hypertrichous at J,; podonotal portion holotrichous, except at z3; opisthonotal portion with px2-;. Genu IV with pl, added; tibia IV holotrichous. From Trichosurus caninus (Ogilby) (Marsupialia: Phalangenidae) sion cla neice ett a niacannasanayr penelope Domrow, 1964 Palpal tibia bideficient. Dorsal shield holotrichous at J,; podonotal portion markedly hypotrichous; opisthonotal portion lacking px2-3. Genu IV lacking pd;; tibia IV lacking pd; and pl,. From Trichosurus vulpecula (Kerr) (Marsupialia: Phalangertdae) 006. yos sea ae es a oe inci Mage neie yee stsyphus, n. sp. 52s Dorsalshield“with: setae 25 025.5 ae A et oa ee 6 Dorsalishield lacking, setaeiz4.c:00 2. cj) se ieee ty ee ios aes ale a earsir anes 7 6. Dorsal shield hypertrichous at J,. Coxae II- III with seta av simple. From Gymnobelideus leadbeatert McCoy (Marsupialia:Petauridae)) 2.033) ao eo ye ee anticlea Domrow, 1972b Dorsal shield holotrichous at J,. Coxae II-III with seta av blade-like. From Petaurus breviceps Waterhouse and P. norfolcenszs (Kerr) (Marsupialia: Petauridae) ................ calypso Domrow, 1966 7. Sternal shield with anterior margin eroded outside setae st,. Terminal pair of ventral setae barely half as long as anal shield. From Pseudocheirus peregrinus (Boddaert) (Marsupialia:) Petauridae)) is 5c.4 jo ese elas ulysses Domrow, 1961 Sternal shield with anterior margin not eroded outside setae st,. Terminal pair of ventral setae as long as anal shield. From Schoinobates volans (Kerr) (Marsupialia: Petauridae) aca cs hey Sei era A SC tae aaa ulixes Domrow, 1972a Haemolaelaps sisyphus, n. sp. (Figs 1-14) Material. Holotype @, allotype d, five paratype 99 and two paratype dd, nasal passages of a brush-tailed possum, Trichosurus vulpecula (Kerr) (Marsupialia: Phalangeridae), Timbillica State Forest, N.S.W., 26.11.1979, D. M. Spratt and P. Haycock. Holotype, allotype and one paratype 9 in Australian National Insect Collection, CSIRO, Canberra; remainder in my institute. Female. Basis capituli (Fig. 4) slightly wider than long, with setae c short, failing to reach either deutosternum or sides of basis; deutosternal denticles six, mostly single (occasionally double, rarely triple). Hypostome with h, > h, > hz, hs slightly exceeding sides of basis; cornicles well sclerotized ; internal malae with ciliations Proc. Linn. Soc. N.S.W., 104 (4), (1979) 1980 R. DOMROW 223 almost as long as inner edge of cornicles, but not clearly seen; epipharynx spiculate; salivary stylets almost reaching tips of cornicles; anteromedial extension of subcheliceral shelf present (as it is in all members of group), short, hastate. Epistome (Fig. 8) reaching apices of palpal femora, pointed, with a few serrations and submarginal dendritic pattern. Palpal trochanter-genu holotrichous (2.5.6) ; trochanter with v, only slightly expanded basally; genu with al,-, spatulate, dorsobasal pore present; tibia bideficient (12, including two dorsodistal rods) ; tarsus with a few slender ventral setae and terminal cluster of rods (figured diagram- matically), claw bifid. Chelicerae (Fig. 9) 190 long overall, with stout, strongly sclerotized shafts 35 in diameter (in dorsoventral view) ; basal segment 65 long; dorsal setule short (length not available because of refraction of light) , not inflated basally, dorsal and external pores both present; coronal ciliations short; fixed digit with two denticles, divided tip and short, setiform pilus dentilis; movable digit 50 long, occupying 26% of overall length, with two denticles and simple tip. Idiosoma a little broader posteriorly, but not expanded more than in Fig. 1 even when fed or gravid. Dorsal shield similarly wider posteriorly, 655-665 long, 385-405 wide (maximum) ; surface lightly reticulate, with paired muscle insertions and all 22 pairs of pores (lyriform behind setae j;, distinctively sclerotized near Z; and Ss) ; podonotal portion hypotrichous, with 14 pairs of setae (excluding 13, always present, but on cuticle) compared to usual 22 (i.e. 21,3, 51-3 and 72,4 lacking — actually, only on one side of one specimen, left-hand side of Fig. 1, is entire complement of 14 present; all other counts are 13 or 12, due to absence of 72, right-hand side of Fig. 1, or z., or both) ; opisthonotal portion also hypotrichous, with 14 pairs, left-hand side of Fig. 1, Figs 1-2. Haemolaelaps sisyphus, idiosoma, dorsal. 1. 9.2. 5. (Allscales = 100 um). Proc. Linn. Soc. N.S.W., 104 (4), (1979) 1980 224 A NEW SPECIES OF HAEMOLAELAPS cjr Figs 3-4. Haemolaelaps sisyphus 9 . 3. Idiosoma, ventral. 4. Capitulum, ventral (true right palp dorsal) . compared to usual 17 (i.e. S, and px2-3 lacking; S; absent on one side of one specimen and J, on one side of another two, right-hand side of Fig. 1) . Dorsal cuticle continuous posteriorly, with about eight pairs of setae (including rs) . Tritosternal base unarmed (Fig. 3), laciniae well ciliated. Sternal shield 105-110 long in midline, 130-135 wide at setae st,; anterior margin flatly convex, merged almost imperceptibly with presternal striae; posterior margin irregularly concave; surface reticulate only anterolaterally, with two pairs of lyriform pores; setae st,-3 short, subequal. Metasternal shields not taking in setae mst (of which one is absent on one side of four specimens) and associated pores. Genital shield 145-160 long behind setae g, 145-175 wide (maximum) ; expanded and sharply truncate behind coxae IV; surface reticulate, with paired muscle insertions and leaving genital pores free in cuticle (though not on right-hand side of Fig. 3) ; setae g short; operculum reaching over posterior margin of sternal shield, rayed and supported by apodemes between coxae IV; insemination apparatus visible only as pale, narrow adductor canals running in from between coxae III-IV. Anal shield 125-130 long (including cribrum), 140-145 wide, only narrowly separated from genital shield; surface reticulate, with paired muscle insertions and two pores on margin; anus set forward of centre, flanked | by setae aa and followed by longer pa. Metapodal shields in two elongate elements, Proc. Linn. Soc. N.S.W., 104 (4), (1979) 1980 R. DOMROW 225 outer one much the larger. Ventral cuticle with one or two pairs of shieldlets flanking genital shield, some paired pores and about 11 pairs of setae of increasing length posteriorly (including two pairs flanking genital shield). Peritremes reaching forward almost to anterior margins of coxae I; peritrematal shields fused very narrowly to vertex of dorsal shield, with two narrow expansions (the more posterior with a pore) along dorsal margins and variably free posteriorly of crescentic exopodal shields IV. Legs slender, but II a little thicker; holotrichous, with two exceptions: genu IV lacking pd;, tibia IV lacking pd, and pl, (Figs 13-14). Seta av on coxae II-III somewhat expanded ; ad, on femora I-IV strengthened and bifid at very tip, but other d setae on femora (and genua) undistinguished; pd; on tarsus IV not long and outstanding. Individual variations noted once (twice for genu IV) include unideficiencies: pd; on genu I, av on genua III-IV and ad; on tarsus IV; and doubled setae: ad, on femur III (anterior seta normal, bifid, posterior seta short, simple, each in its own alveolus) and pl, on tarsus IV (setae subequal, in contiguous alveoli). Dorsodistal sensory islet on tarsus I (Figs 11-12) including a forked seta and occupying 19% of length (of the seatae on this segment, four distals and two laterals are longer, and one middorsal long and outstanding, cf. H. n.sp. Domrow, 1981). Coxae II with anterodorsal process small; II-IV with posterointernal apodemes. All tarsi with stalked ambulacrum and two claws. Male. As @, except as follows. Deutosternum at times with seven denticles. Seta v, on palpal trochanter not expanded basally. Chelicerae (Fig. 10) 165-170 long overall; setule, pores and corona not seen clearly; fixed and movable digits with one denticle and simple tip; spermatodactyl 55 long, occupying 32% of overall length, sharply upcurved at tip. Dorsal shield fuller, 520-525 long, 280-290 wide (maximum) ; podonotal portion hypotrichous, with 14 pairs of setae (though not same 14 pairs as in 9 since 73, always present, is on shield, except on one side of one specimen, and 2z, is lacking — notwithstanding this, the regularity with which one or both z, are absent in 2 suggests this signature will also be found in & when more material becomes available) compared to usual 22 (actually, only on one side of two specimens is entire complement of 14 present; all other counts are 13 or 12, due to absence of 72, left- hand side of Fig. 2, or 7, and r; in one case or r; in another, right-hand side of Fig. 2) ; opisthonotal portion also hypotrichous, with 14 pairs compared to usual 17. Dorsal cuticle interrupted posteriorly, with about four setae to each side. Holoventral shield (Fig. 5) with genital aperture on convex anterior margin; 445-450 long overall, 155-175 wide behind coxae IV where ventral portion is irregularly expanded to usurp two (in one case, Fig. 6, one plus an alveolar remnant too imperfect ever to have housed a seta) or three pairs of ventral setae (one specimen with one mst seta, another with both mst and one g absent, Fig. 7). Metapodal shields likewise irregular, the larger divided posteriorly on one side of one specimen. Ventral cuticle with about five pairs of setae of increasing length posteriorly. Peritrematal shields fused broadly, wa more anterior of two expansions of their dorsal margins, to dorsal shield. Individual variations in leg setation (all unideficiences) even more common than in 2: pl on femur IV, av on genu III and av, on tibia I (all noted once); av on trochanter I and ad; on femur I (on same side of one specimen) ; and av on genu IV (on both sides of two specimens) . Etymology. Named after Sisyphus, said to have been Ulysses’ father. ACKNOWLEDGEMENTS I am grateful to Dr D. M. Spratt, Division of Wildlife Research, CSIRO, Lyneham, for this fine species, and to Miss Cobie Rudd for the drawings. Proc. Linn. Soc. N.S.W., 104 (4), (1979) 1980 226 A NEW SPECIES OF HAEMOLAELAPS Figs 5-14. Haemolaelaps sisyphus. 5. \diosoma G, ventral. 6-7. Variants of ventrianal portion of holoventral shield 5. 8. Epistome 9. 9. Cheliceral digits 9, ventral. 10. Cheliceral digits 6, ventral. 11-12. Trochanter- tarsus IV Q, dorsal and ventral. 13-14. Tarsus I 2, dorsal and ventral. Proc. LINN. Soc. N.S.W., 104 (4), (1979) 1980 R. DOMROW 227 References BERLESE, A., 1910. — Lista di nuove specie e nuovi generi di Acari. Redza, 6: 242-271. Domrow, R., 1961. — New and little-known Laelaptidae, Trombiculidae and Listrophoridae (Acarina) from Australasian mammals. Proc. Linn. Soc. N.S.W., 86: 60-95. ——, 1964. — The ulysses species-group, genus Haemolaelaps (Acarina, Laelapidae). Proc. Linn. Soc. N.S.W., 89: 155-162. ———, 1966. — Some laelapid mites of syndactylous marsupials. Proc. Linn. Soc. N.S.W., 90: 164-175. ——, 1972a. — Eight Australian species of Andreacarus Radford and Haemolaelaps Berlese (Acari: Dermanyssidae). J. Aust. ent. Soc., 11: 105-113. ——, 1972b. — Two new species of Haemolaelaps Berlese (Acari: Dermanyssidae) from Leadbeater’s possum. J. Aust. ent. Soc., 11: 290-294. ——, 1977. — New records and species of Laelaps and allied genera from Australasia (Acari: Dermanyssidae). Part 2. Proc. Linn. Soc. N.S.W., 101: 185-217. ——, 1979. — Some dermanyssid mites (Acari), mostly from Australasian rodents. Proc. Linn. Soc. N.S.W., 103: 189-208. ——, 1981. — Oriental Mesostigmata (Acari). 6. A Malesian member of the mesopicos group (Haemolaelaps). Acarologia, 22 (in press) . Evans, G. O., 1969. — Observations on the ontogenetic development of the chaetotaxy of the tarsi of legs II-IV in the Mesostigmata (Acari). Proc. I[int. Congr. Acar. (1967) : 195-200. , and TILL, W. M., 1965. — Studies on the British Dermanyssidae (Acari: Mesostigmata). Part I. External morphology. Bull. Br. Mus. nat. Hist., Zool., 13: 247-294. Rive, W. D. L., 1970. — A guide to the native mammals of Australia. Melbourne: Oxford University Press. Proc. Linn. Soc. N.S.W., 104 (4), (1979) 1980 ante! Renita AB ih eS CS cates The Geology of the Bungonia District, New South Wales P. F. CARR, B. G. JONES, A. J. KANTSLER, P. S. MOORE and A. C. COOK. Carr, P. F., Jones, B. G., KANTSLER, A. J., Moore, P.S. & Cook, A. C. The geology of the Bungonia district, New South Wales. Proc. Linn. Soc. N.S.W. 104 (4), (1979) 1980 : 229-244. Detailed geological mapping has provided stratigraphic and structural evidence for reinterpreting the geological history of the Bungonia area in the eastern Lachlan Fold Belt, New South Wales. The oldest rocks consist of a Late Ordovician distal flysch sequence (Tallong Beds) which shows isoclinal folding. The Tallong Beds are unconformably overlain by the Late Silurian shallow marine limestone — shale sequence of the Bungonia Limestone. Carbonate deposition ceased in the Late Silurian or Early Devonian when deposition of the Tangerang volcanics commenced. The latter sequence consists of lensoidal dacite flows interbedded with shallow marine volcaniclastic and tuffaceous sedimentary rocks. Emplacement of the southern part of the Marulan Batholith in the Early Devonian was probably coincident with a phase of broad folding. Erosional remnants of Permian and post-Permian sedimentary and volcanic rocks overlie parts of the older sequence. P. F. Carr, B. G. Jones, A. J. Kantsler and A. C. Cook, Department of Geology, University of Wollongong, P.O. Box 1144, Wollongong, Australia 2500 and P. S. Moore, Delhi Petroleum, G.P.O., Box 2364, Adelaide, Australia 5001; manuscript received 14 March 1980, accepted 23 April 1980. INTRODUCTION The area mapped at Bungonia (Fig. 1) abuts the western margin of the southern Sydney Basin and includes a sequence of Ordovician to Devonian sedimentary and volcanic rocks. This sequence occurs in the eastern part of the Lachlan Fold Belt and has been intruded by the Marulan Batholith. Erosional remnants of younger sedimentary and volcanic rocks overlie part of the area. The first detailed geological study of the Bungonia area was carried out by Woolnough (1909) and further references to the regional geology were made by Naylor (1935, 1936, 1939, 1950) and Garretty (1937). Aspects of the limestones were studied by Carne and Jones (1919), Pratt (1964), Ellis et al. (1972) and Pickett (1972), and descriptions of the Marulan Batholith were published by Osborne (1931, 1949) and Osborne and Lovering (1953). The district has been the subject of several unpublished honours theses. The aim of the present study was to remap the area from Bungonia Gorge to Inverary Park (Fig. 1) to elucidate the stratigraphy, structure and tectonic development of the region. TALLONG BEDS Distribution and Petrography. The Ordovician Tallong Beds (Wass and Gould, 1969) are well exposed along the Shoalhaven River between Tallong and Bungonia, and form part of a much larger meridional belt of Ordovician rocks extending southwards to the coast between Bermagui and Tathra (Packham, 1969; Crook et al., 1973). In the Bungonia area, the Tallong Beds consist of micaceous, fine-grained, quartz-rich sandstone with shale, slate, siltstone, phyllite and chert interbeds (Table Proc. Linn. Soc. N.S.W., 104 (4), (1979) 1980 0861 (6461) ‘(%) FOI ‘““M‘S'N 90S ‘NNIT ‘004g 0861 (6461) ‘(%) FOL ““M'S'N 90S ‘NNIT ‘004g TO SYDNEY GOULBURN xx IVvVvVv t+ +++ t+ tet ++ t+ t+ $+ +t t+ N+ Ne ents WN x Ps t S yr ; x t XXX KK XXX KX DK x la < Springponds x = Ix x x x xX TN (* < m. x fx xxgeoTy WF 4K x x eV vy USS Se HP I-y > 7 Lf LH / Brisbane misoant Meadows sg /% DEVONIAN ?PERM. TERT. EARLY LATE SILURIAN 1000 =o => 2000 Fa Se REEVESDALE BASALT INVERARY TONALITE PORPHYRY LUMLEY ADAMELLITE WYLORA QUARTZ GABBRO SPRINGPONDS GRANODIORITE | TANGERANG VOLCANICS BUNGONIA LIMESTONE TALLONG BEDS Fig. 1. Geology of the Bungonia area, New South Wales. metres Road Creek Unconformity ult ction line Geological boundary quartzarenite tourmaline-quartz rock tonalite adamellite quartz gabbro granodiorite silcrete, sand basalt hornblende dacite tuffaceous arenite dacite upper limestone upper shale middle limestone lower shale lower limestone shale, chert, arenite 0&2 VINOONNE JO ADOTOAD WOOO '0'V CNV AUYOOW 'S‘d ‘UAISLNVY fv ‘SaNOl’9'd ‘wWAVvo a‘a 18Z 232 Rock Type GEOLOGY OF BUNGONIA TABLE 1 Petrography of the Tallong Beds Composition ee Quartz-rich arenite Carbonaceous shale and slate Non-carbonaceous Fine-grained, poorly to moderately sorted, immature sublitharenite. Quartz (to 80%), feldspar (0-5%), sandstone and chert rock fragments (7%), muscovite (0-5%); minor epidote, amphibole, biotite, chlorite; rare zircon, rutile, tourmaline and iron-titanium oxides. Framework grains subangular to subrounded. Matrix (5-20%) of sericite, clay, quartz and carbon- aceous material. Minor quartz cement and secondary chlorite. Very fine-grained quartz, muscovite, chlorite, clay, pyrite (to 15%) and organic matter (>10%). Reflect- ivity of graptolites in the range Romax 8.35% to 10.01%. Well sorted siltstone with quartz (75-95%); minor Other Features Most prominent in northeast. Massive to flat bedded. Symmetrical and asymmetrical ripples. Bouma sequences include erosional base, sole marks, load casts, flame structures, graded beds, ripple cross-beds and small slumps. Arenite interbedded with siltstone and shale in 0.1-1lm units. Generally show medium to large scale isoclinal folds. Occur as interbeds in arenite or as massive shale with lenses of chert, siltstone and very fine grained sandstone. Abundant graptolites. Some small isoclinal folds. Most prominent in south and east. Lithologies siltstone, shale, slate and phyllite sodic plagioclase, chert, muscovite; rare biotite, pyrite and hematite. Remaining lithologies very fine © grained with quartz, sericite and clay. Slate and phyllite have mica and chlorite (to 30%) defining bedding plane cleavage. interbedded. Tops of Bouma sequences common. Ripple cross-beds. Some chert lenses. Show small and large scale isoclinal folds. Chert Microcrystalline quartz; minor sericite, clay; rare Occurs as interbeds in sandstone and shale. graphite and iron-titanium oxides. Some secondary chert. 1). An axial plane cleavage is weakly to moderately developed. The stratigraphy of the Tallong Beds is poorly resolved because of faulting and isoclinal folding with meridional axes (Fig. 2). Environment of Deposition. Sandy units in the Tallong Beds typically exhibit Bouma sequences and a variety of sedimentary structures characteristic of deposition from turbidity currents (Table 1). A thick, predominantly graded-bedded sandstone containing only minor argillaceous interbeds crops out in the northeast of the study area and is interpreted as proximal flysch. Sequences comprising thin alternations of sandstone and slate probably represent distal flysch, whereas the extensive, uniformly <= facing of bed |/Bungonia || — Gorge \ 4 Lst Fig. 2. Structure of Tallong Beds exposed along the lower portion of Bungonia Creek. Proc. Linn. Soc. N.S.W., 104 (4), (1979) 1980 P. F. CARR, B. G. JONES, A.J. KANTSLER, P.S. MOORE AND A. C. COOK 233 thin-bedded, black slate — chert association indicates deposition under moderately quiet water with reducing conditions at the sediment-water interface. A low initial Eh in the black slate facies would favour the preservation of abundant organic matter, including graptolites, and lead to the development of early diagenetic pyrite. The quartz-rich arenite — slate — chert association conforms to the greywacke — slate suite of Packham (1969) and Unit B of Crook et al. (1973) and Scheibner (1973). The source of the sediment was to the south and southwest (current direction to 030° assuming simplest structural interpretation) and may have come from the Canberra-Molong Volcanic Rise and possibly a distant continental mass. Fauna and Age. The carbonaceous black slates of the Tallong Beds contain graptolite faunas of Late Ordovician age (Sherrard 1949, 1954, 1962; Sherwin, 1972). Ten new Late Ordovician graptolite localities have been recorded in the Bungonia area but most of these have poorly preserved faunas because of surface weathering. ORDOVICIAN-SILURIAN BOUNDARY Considerable disagreement has existed over the nature of the boundary between the Tallong Beds and the overlying Bungonia Limestone. A marked angular discordance between the two formations in Bungonia Creek was described as an angular unconformity by Woolnough (1909) and Osborne (1949). However, Naylor (1950) attributed the angular discordance entirely to faulting and suggested that the Bungonia Limestone has a disconformable relationship with the Late Ordovician sequence. Gould (1966), Baker (1971) and Kantsler (1973) have indicated that the isoclinally folded Late Ordovician sequence was deformed at least once prior to the deposition of the Bungonia Limestone and have suggested a faulted contact. Counsell (1973) considered the boundary to be an unconformity and this has been confirmed by the present study. The base of the Bungonia Limestone between Bungonia Gorge and the southern nose of the plunging syncline northeast of Carne (Fig. 1) is a sharply defined slightly undulating plane which shows no evidence of faulting. This syncline accounts for the very extensive limestone outcrops in the lower part of Bungonia Gorge. Rare clasts of shale from the Tallong Beds occur in the basal 2 m of the limestone just south of Bungonia Creek. Furthermore, the presence of Ordovician graptolitic shale in the core of a small anticline south of Brisbane Meadows is additional evidence for the unconformable nature of the basal contact. In the central part of the area (Fig. 1) the eastern contact of the Bungonia Limestone is faulted. BUNGONIA LIMESTONE The Bungonia Limestone was first described by Woolnough (1909), named by Carne and Jones (1919) and has subsequently been mentioned by several authors. It is subdivided here into five informal units (lower limestone, lower shale, middle limestone, upper shale and upper limestone) which are not of uniform lateral extent. The three limestone units are composed of five interdigitating lithotypes whereas the lower and upper shales are composed of four lithotypes (Table 2) . Lower Limestone. The lower limestone forms the basal unit of the formation except on the western limb of the syncline northeast of Carne where it is underlain by a thin lensoidal fossiliferous sandstone. The lower limestone varies in thickness from 280 m in the north and south, to 90 m northeast of Carne (Fig. 1). Either the original depositional surface was undulating or the transition from limestone to shale was controlled by localized terrigenous sediment input. Proc. LINN. Soc. N.S.W., 104 (4), (1979) 1980 234 GEOLOGY OF BUNGONIA TABLE 2 Petrography of the Bungonia Limestone Unit Rock Type Composition Other features Fauna Shale Illite, chlorite; some sericite, muscovite, Poorly bedded. Bryozoans, graptolites, biotite, quartz, brown organic matter and trilobites, brachiopods, fossil fragments. Some shale calcareous or Nautiloids, gastropods siliceous. Reflectivity of organic matter and crinoid ossicles. a in the range Romax 2.7% to 6./%. <= a Siltstone Quartz; minor feldspar; rare rock fragments, Poorly to moderately Crinoid ossicles. ice organic matter, pyrite, zircon, tourmaline bedded. o and muscovite. Matrix of illite and chlorite. > Some siltstone calcareous with fossil fragments. (=) z Sandstone- Fine-grained and immature. Subrounded quartz; Laminated and ripple Crinoid ossicles and = sublitharenite minor feldspar, chert and lithic fragments, cross-bedded. Graded corals. S muscovite, biotite, zircon and iron-titanium bedding. 4 oxides. Matrix of sericite. Very minor calcite and quartz cement. Chert Microcrystalline quartz. Some silty chert. Thin beds. Crinoid ossicles, corals, brachiopods and bryozoans. Biosparudite Rounded fossil fragments (to 35cm) and some Massive and biostromes. Brachipods, crinoid angular to subangular limestone intraclasts ossicles, corals, 1 (to 20cm). Clasts mainly 5-10cm. Minor 6tromatoporoids and 2 detrital quartz and clay. Spar calcite stromatolites. iA cement. w 5 ZA Biosparite Fossil fragments (approximately 15%) and 5-25cm thick beds inter- Brachiopods, corals, = rounded intraclasts Accessory ilmenite, leucoxene and zircon. Matrix of = chert, chlorite, sericite and clay. Cement includes = quartz, calcite, secondary amphibole and pyrite. = aw = Fine arenite Poorly to inoderately sorted and immature. Very angular Most abundant lithology in south (approx- & (quartzarenite, to well rounded quartz and minor weathered feldspar imately 75%). Flat laminated to lenticular 2) sublitharenite (<5%). Rock fragments include siltstone, shale, chert beds. Small to medium tabular and trough and litharenite) and dacite. Accessory iron-titanium oxides, zircon, cross-beds inainly <15cm, few to lm. Small ‘tourmaline, anatase and sphene. Matrix of sericite, slumps. Cut and fill structures. Some clay; minor chert and calcite. Cements include quartz chert and shale interbeds. Rare bryozoans, and rare calcite especially in the north. corals and crinoid ossicles. Chert and Very fine-grained chert, chloritic chert and shale. Thin beds. Massive to poorly bedded, some shale Shales include detrital quartz, mica and clay. with undulose laminae. Cherty shale more abundant in south and at top of fomnation. EASTERN Porphyritic Phenocrysts of embayed quartz and greenish plagioclase Extensively altered — devitrification of DACITES dacite (Ang 9 45)" Very fine-grained groundinass of quartz, volcanic glass gives abundant chlorite, =f i pies icite and kaolinite. plagioclase, K-feldspar and minor hornblende, biotite, aay hypersthene and iron-titanium oxides. WESTERN Porphyritic Phenocrysts of embayed quartz, hornblende, plagioclase As above. HORNBLENDE hornblende (Angy_q7) and hypersthene. Groundmass and accessories as DACITE dacite above. Bungonia Limestone is Late Ludlovian (Carr et al., 1980) , which is in agreement with earlier age determinations by Pickett (1967, 1972). BUNGONIA LIMESTONE- TANGERANG VOLCANICS BOUNDARY The boundary between the Bungonia Limestone and the Tangerang volcanics is not exposed in the study area. Although the limestone and volcanics have similar dips, the contact between the units south of Adams Lookout is probably faulted since the basal unit of the Tangerang volcanics overlies several different units of the Bungonia Limestone (Fig. 1). In the Marulan South area the equivalent boundary is considered conformable (Wass and Gould, 1969). TANGERANG VOLCANICS The sequence of igneous and volcanogenic sedimentary rocks which overlies the Bungonia Limestone can be equated with the Tangerang volcanics (Wass and Gould, 1969) in the Marulan South region. In the Bungonia area these rocks can be subdivided into (i) the eastern dacites which are interbedded with tuff, tuffaceous to quartzose arenite and shale; and (ii) the western hornblende dacite. Eastern Dacites. The eastern dacites (Table 3) crop out as elongate lenses parallel to the regional strike in the central and northern parts of the study area. Sedimentary rocks interbedded with the eastern dacites show a wide range in grain-size and mineralogical composition but characteristically contain angular grains of plagioclase, $-quartz and volcanic rock fragments in a chloritic and cherty matrix. The rocks are texturally and mineralogically immature and the mineralogical composition is strongly grain-size dependent. They grade from very coarse-grained, poorly-sorted crystal tuff and tuffaceous sandstone to well-sorted, fine-grained quartz- rich arenite with minor cherty shale (Table 3, Fig. 3). The arenite tends to become finer and more quartz-rich towards the south. Western Hornblende Dacite. The hornblende dacite (Table 3) of the Tangerang Proc. Linn. Soc. N.S.W., 104 (4), (1979) 1980 P. F. CARR, B.G. JONES, A.J. KANTSLER, P.S. MOORE AND A. C. COOK 237 QUARTZ quartzarenite subarkose Lx sublitharenite 4 Crystal tuff = Coarse arenite Fine arenite lithic feldspathic arkose litharenite ROCK FELDSPAR FRAGMENTS Fig. 3. Mineralogical composition and classification of sedimentary units of the Tangerang volcanics. arkose litharenite volcanics is restricted to the central-western portion of the study area (Fig. 1). Thickness. Preserved thicknesses of the Tangerang volcanics in the Bungonia area vary from 450 m in the north to 1600 m in the south. The original thickness is indeterminate because the western margin of the formation is an intrusive contact with the Marulan Batholith. Mode of Emplacement of Igneous Rocks. The dacites and hornblende dacite within the Tangerang volcanics are considered extrusive in origin. The reasons are as follows: (1) the eastern dacites occur as a series of lensoidal bodies parallel to the regional strike ; (ii) there is no evidence of contact metamorphism along the margins of the igneous rocks ; (iii) possible pillow structures occur at the base of a thin dacite north of Carne; (iv) microscopic flow-layering is present in some dacites ; (v) B-quartz occurs in all units; (vi) the dacites are interbedded with tuff and tuffaceous sedimentary units; and (vii) some of the very fine-grained cherty groundmass of the sedimentary rocks probably originated from devitrification of volcanic glass. Fauna and Age. Sporadic occurrences of crinoid ossicles, bryozoans and solitary corals have been found in sedimentary units in the lower and middle parts of the Tangerang volcanics but the poorly preserved fossils do not permit an accurate age determination. In the Bungonia area, the Tangerang volcanics are Early Devonian (possibly latest Silurian) in age based on faunas from the Bungonia Limestone and K-Ar dating of the southern part of the Marulan Batholith (Carr et al., 1980). Enuironment of Deposition. The Tangerang volcanics represent an accumulation of shallow marine, flat- and cross-bedded arenite interbedded with submarine dacitic lavas and associated pyroclastic rocks. Devitrification of volcanic glass and primary precipitation of silica from marine waters supersaturated by volcanic emanations could account for the high proportion of chert in much of the tuffaceous arenite. Proc. Linn. Soc. N.S.W., 104 (4), (1979) 1980 238 GEOLOGY OF BUNGONIA A dacitic volcanic source must have been located to the north of Bungonia since the proportion of dacite and volcanic detritus in the Tangerang volcanics decreases south of the township. At the same time a sedimentary source, probably an exposed block of the Tallong Beds, was contributing fine-grained quartzose detritus to the depositional area. MARULAN BATHOLITH The Marulan Batholith is a composite body which crops out east and northeast of Goulburn and includes granite, granodiorite, contaminated and hybrid rocks (Woolnough, 1909; Osborne, 1949; Osborne and Lovering, 1953). O’Reilly (1972) considered that the ‘hybrid zones’ of Osborne and Lovering (1953) correspond to zones of progressive metamorphism of silicic volcanics intruded by magmas forming the batholith complex. Four separate phases of the batholith have been mapped in the Bungonia area (Fig. 1) and K-Ar dating of three of these phases indicates an Early Devonian age of emplacement (Carr et al., 1980). Springponds Granodiorite (new name). The Springponds Granodiorite crops out extensively in the Bungonia area and is named after the property Springponds (type locality GR701407 — Bungonia 1: 25,000 Topographic Sheet). The rock is holocrystalline, medium- to coarse-grained with a hypidiomorphic granular texture. It contains plagioclase, K-feldspar, quartz, hornblende, biotite and iron-titanium oxides with minor amounts of diopside, hypersthene, chlorite, uralite, prehnite, epidote, apatite, zircon and kaolinite. Plagioclase shows normal and oscillatory zoning from andesine (Amys) to oligoclase (An,.). The K-feldspar is perthitic and extensively kaolinized. Wylora Quartz Gabbro (new name). The Wylora Quartz Gabbro has an elongate outcrop to the north and east of Bungonia township and is named after the property Wylora (type locality GR695394 — Bungonia 1: 25,000 Topographic Sheet) . The quartz gabbro is a holocrystalline, medium- to coarse-grained rock with a hypidiomorphic granular texture. Plagioclase, augite, biotite, hornblende, hypersthene, iron-titanium oxides, interstitial quartz and accessory apatite occur in addition to traces of K-feldspar, sericite, carbonate, fibrous amphibole, prehnite and pyrite. The plagioclase shows normal and oscillatory zoning from cores of bytownite (Ang;) to rims of labradorite (Ans3). Lumley Adamellite (new name). The Lumley Adamellite crops out to the south and west of the township of Bungonia and is named after Lumley Creek (type locality GR689385 — Bungonia 1: 25,000 Topographic Sheet) . The adamellite is holocrystalline, medium- to coarse-grained with an allotriomorphic granular texture. Primary minerals are K-feldspar, plagioclase, quartz, biotite, hornblende, apatite, zircon, sphene and iron-titanium oxides. Alteration has produced chlorite, sericite, epidote and prehnite. The K-feldspar is microperthite and the plagioclase is zoned from andesine (An,;) to oligoclase (An,3) . Inverary Tonalite (new name). Brunker and Offenberg (1968) mapped a number of porphyritic tonalite intrusions on the southeastern portion of the Goulburn 1: 250,000 Geological Sheet. The northernmost tonalite intrusion crops out southeast of Bungonia and is dissected by and named after Inverary Creek (type locality GR711380 — Bungonia 1: 25,000 topographic Sheet) . The eastern contact between the intrusion and the Tangerang volcanics is sharp and dips towards the west at approximately 45° (Fig. 4D). The tonalite is holocrystalline and porphyritic with phenocrysts of plagioclase and subordinate hornblende, biotite and quartz in a fine-grained groundmass of plagioclase, quartz, biotite, hornblende, iron-titanium oxides and minor apatite and zircon. Extensive Proc. Linn. Soc. N.S.W., 104 (4), (1979) 1980 P. F. CARR, B. G. JONES, A. J. KANTSLER, P.S. MOORE AND A. C. COOK 239 secondary alteration has produced chlorite, sericite, sphene and leucoxene. Tourmaline-Quartz Rock. Three separate outcrops of tourmaline-quartz rock have been mapped in the Tangerang volcanics (Fig. 1). Two of the outcrops occur at the margins of intrusions whereas the northern outcrop does not have any obvious field relationship with intrusions. The rocks consist of fine-grained ferrian tourmaline and quartz with minor secondary hematite. CONTACT METAMORPHISM The Marulan Batholith has produced a narrow (<200 m) aureole within the Tangerang volcanics which is recognized by a slight recrystallization of the dacite groundmass. Contact metamorphism has produced the mineral assemblage albite- epidote-chlorite-actinolite typical of the albite-epidote hornfels facies. At some localities within 10 m of the intrusions the metamorphic grade reaches the hornblende hornfels facies. O’Reilly (1972) has described similar grades of contact metamorphism of silicic volcanic and associated sedimentary rocks around the Marulan Batholith in an area 15 km northwest of Marulan. METAMORPHISM OF ORGANIC COMPONENTS , Reflectance measurements on coalified graptolites from the Tallong Beds in Bungonia Creek (Table 1) indicate a metamorphic grade equivalent to the lower greenschist facies (chlorite zone). In contrast, vitrinite-like organic matter from the lower shale of the Bungonia Limestone (Table 2) is considered to represent a regional metamorphic grade equivalent to the upper zeolite facies. The differences in metamorphic grade between the Tallong Beds and the Bungonia Limestone could indicate that the Tallong Beds underwent low grade regional metamorphism prior to the deposition of the Bungonia Limestone. Alternatively the Tallong Beds may have been affected by contact metamorphism from a buried intrusion of the Marulan Batholith, although there is no evidence of this in the topographically equivalent portion of the Bungonia Limestone. ?PERMIAN SEDIMENTARY ROCKS Small outliers of ?Permian quartzarenite unconformably overlie the Bungonia Limestone and Tangerang volcanics and are commonly silicified or ferruginized. Some are cross-stratified (mean foreset azimuth to 340°). The arenite is typically medium- to coarse-grained, poorly sorted and consists of subangular to rounded quartz, lithic chert and rare sericitized K-feldspar, iron-titanium oxides and zircon. Quartz overgrowths and chert cement are present. Some of the arenite contains subrounded to well-rounded pebbles of quartz and quartzite. These outliers are tentatively correlated with the Permian sequence of the Sydney Basin. They are lithologically similar to a fossiliferous Permian outlier at Marulan South described by Wass and Gould (1969). REEVESDALE BASALT (new name ) The northernmost flow of the Late Eocene Nerriga Province (Wellman and McDougall, 1974) crops out to the south of Bungonia (Fig. 1) and is named after the property Reevesdale (type locality GR720336 — Bungonia 1: 25,000 Topographic Sheet). Maximum thickness is approximately 8 m but the original thickness and extent are unknown. The rock is an alkali olivine basalt consisting of a fine- to medium-grained assemblage of plagioclase (An,2-4,), olivine, titaniferous augite, iron-titanium oxides and accessory apatite. Proc. Linn. Soc. N.S.W., 104 (4), (1979) 1980 240 GEOLOGY OF BUNGONIA DYKES Numerous basalt and dolerite dykes occur in the Bungonia area but are too thin to be shown in Fig. 1. The dykes are medium- to fine-grained, have an ophitic texture and consist of plagioclase (Ang;-60), titaniferous augite, serpentine pseudomorphs after olivine, iron-titanium oxides and minor apatite. The rocks are extensively altered with the development of abundant serpentine, calcite and chlorite. The age of the dykes is uncertain but their emplacement may be related to the extrusion of the Eocene Reevesdale Basalt. TERTIARY SEDIMENTARY ROCKS Poorly-consolidated quartz sandstone and minor conglomerate occur sporadically beneath the Reevesdale Basalt. The age of most other surficial sediments cannot be defined except for the occurrence of Cznnamomum spp. leaves (Tertiary) in a ferruginous sandstone southeast of Adams Lookout (Pratt, 1964). Only the major ?Tertiary deposits are shown in Figure | and they consist of poorly-consolidated sand, gravel, ferruginous shale and manganiferous grit. PEDOGENIC DEPOSITS (i) Ferruginous surficial deposits, laterite and ferricrete occur as isolated patches over much of the study area. Iron (and manganese) oxides replace the matrix and minerals of the host rock to a variable degree. Ferruginous shale breccias also occur, especially along fault planes. (ii) Deep red bauxite with a pisolitic texture formed by intense weathering of the Eocene basalt in the Reevesdale area. (iii) Silcrete occurs on many low hills and ridges throughout the area. It consists of angular to rounded quartz grains with pitted or etched grain boundaries set in a cherty matrix. The silcrete is underlain by a pallid or mottled zone which suggests an origin due to deep weathering (cf. Hutton et al., 1972). The silcrete in this area has been described in detail by Callander (1978). (iv) Kaolinite deposits of variable quality occur beneath the silcrete. STRUCTURAL HISTORY Schematic geological cross-sections which show the major structural features of the Bungonia area are given in Figure 4. Folding. Two scales of folding have been recognized in the Tallong Beds. Large scale isoclinal folds (F,) have been mapped in the almost continuous exposures along the lower reaches of Bungonia Creek (Fig. 2). Shale which occurs between the more competent sandstone and chert units shows medium- to small-scale isoclinal folding. These smaller folds are generally not persistent along strike and the fold axes plunge gently (approx. 15°) towards the north-northeast. The shale beds show crenulation cleavage and a marked thickening in many of the fold hinges. Axial planes of the smaller folds have similar orientations to those of the larger folds, suggesting that all these folds were produced concurrently. Open, gently-plunging concentric folds (F,) occur in the Bungonia Limestone and the northeastern part of the Tangerang volcanics (Figs 1 and 4). The limestone beds and the Tangerang volcanics act as competent units whereas the interbedded shale is more deformed, shows the development of a weak bedding- plane cleavage and thickening along fold hinges. The meridional F, axial planes dip east at approximately 70°. The Tangerang volcanics south of Carne show consistent westerly dips between 35° and 55°. Proc. Linn. Soc. N.S.W., 104 (4), (1979) 1980 P. F. CARR, B. G. JONES, A.J. KANTSLER, P.S. MOORE AND A. C. COOK 241 Fig. 4. Idealized geological sections for the Bungonia region. Locations of sections are indicated on Fig. 1. Between the eastern edge of the Bungonia Limestone and the Shoalhaven River, the mesoscopic F, folds in the Tallong Beds are generally symmetrical with almost vertical axial planes, whereas east of the river they become asymmetrical with axial planes dipping at a moderate angle to the east (Baker, 1971). Thus, the Tallong Beds in the study area could represent the eastern limb of a broad F, syncline. Late Devonian strata which crop out about 1 km west of the study area in Lumley Creek and near Oak Valley homestead dip at approximately 15° to 20° towards the west and unconformably overlie more steeply dipping Early Devonian rocks. This post- Devonian tilting could explain the steep easterly dips of the F, axial planes. Faulting. The Bungonia Limestone is cut by two major normal strike faults which both dip 65° to 70° west (Figs 1 and 4). These faults are exposed in Bungonia Gorge as 1 to 3 m wide crush zones. The eastern fault is clearly recognizable from the northern side of Bungonia Gorge by a 30° discordance in dip within the Bungonia Limestone. The strike faults were later cut by a series of oblique faults which show lateral, vertical and slight rotational movement. Only the major faults are indicated in Figure 1. DISCUSSION During the Late Ordovician deep marine, quartz-greywacke distal flysch spread throughout the southern Lachlan Geosyncline south and east of Yass (unit B of Crook et al., 1973). The Tallong Beds at Bungonia form a northward extension of this facies and accumulated on the Monaro Slope and Basin near the subduction zone on the eastern edge of the Lachlan Pre-Cratonic Province. The F, fold style in the Bungonia area is similar to the isoclinal recumbent folding produced by the Benambran Orogeny in the southeastern part of the Lachlan Fold Belt (Late Bolindian to Late Proc. Linn. Soc. N.S.W., 104 (4), (1979) 1980 242 GEOLOGY OF BUNGONIA Llandoverian; Stauffer and Rickard, 1966; Crook et al., 1973). At the time of deposition of the basal part of the Bungonia Limestone (Late Silurian) the axial planes of the F, folds probably dipped towards the west at 30°. The Bungonia region remained deeply submerged after the Benambran Orogeny. Early Silurian graptolitic distal flysch strata (Jerrara Series of Naylor, 1935; 1936; 1950) 6 km west of Bungonia appear to be faulted against the Late Ordovician sequence. The Early Silurian strata show upright isoclinal folding (Naylor, 1936) probably resulting from the Wenlockian Quidongan Orogeny (Crook et al., 1973) but there is no evidence of this fold style at Bungonia. The Quidongan Orogeny encompassed a major period of uplift in the Quidong-Canberra region (Crook e¢ al., 1973) which is extended to the Bungonia area to account for the change from distal flysch facies in the Early Silurian to a shallow marine environment in the Late Silurian. The Quidongan Orogeny also led to the formation of the Capertee Rise and the Hill End Trough by splitting off from the Molong Volcanic Rise (Scheibner, 1973). Deformation and uplift of Late Ordovician (Powell and Fergusson, 1979) and Late Ordovician to Early Silurian (Powell et al., 1976) sequences prior to Late Silurian deposition has also been recognized in the Cookbundoon Syncline 60 km northwest of Bungonia. The southern part of the Capertee Rise was submerged during the Late Ludlovian and the shallow marine Bungonia Limestone was deposited unconformably on the Tallong Beds. Limestone deposition alternated with periods of greater input of fine-grained clastic detritus and was terminated by eruption of calc-alkaline acid volcanics on the Bungonia portion of the Capertee Volcanic Arch in the earliest Devonian or latest Silurian (Carr et al., 1980). Volcanic activity was presumably related to the high level intrusion of orogenic granitic rocks. Scheibner (1973) implied that these magmas were associated with a zone of secondary subduction. The phase of F, folding almost certainly accompanied the east-west compression associated with the intrusion of the southern part of the Marulan Batholith in the Early Devonian and is therefore associated with the Bowning Orogeny. At the close of this phase of folding, the axial planes of the F, folds probably would have dipped west at a high angle (about 75°). Northwest of Bungonia in the Murruin Creek area of the Cookbundoon Syncline, Powell et al. (1976, figs 4 and 5) have noted a low angle unconformity between Late Silurian strata and Early to Middle Devonian sandstone and conglomerate. Further south in the Taralga area a post-Late Silurian pre-Late Devonian fold episode produced upright open folds (Powell and Fergusson, 1979, fig. 7). The folding in the latter area is similar in style to the phase of F, folding at Bungonia and could therefore be related to the Early Devonian Bowning Orogeny rather than a Middle Devonian event as suggested by Powell and Fergusson (1979). The age of the faulting in the Bungonia area is difficult to ascertain but at least some of the faults are younger than the F, folding and may be related to a tensional phase of the Bowning Orogeny. Most of the oblique faults post-date the strike faults. The effects of the Bowning Orogeny increase in intensity south and west of the Bungonia area towards Wyangala, Breadalbane, Tarago and Bowning (Packham, 1969, 1978). The Ordovician to middle-Early Devonian stratigraphic succession and deformational history of the Tarago area (Felton and Huleatt, 1977; Gilligan et al., 1979) is similar to that of the Bungonia area some 70 km to the northeast although the open fold style produced during the Bowning Orogeny at Tarago has an associated axial plane slaty cleavage. Cratonization of the Lachlan Fold Belt occurred during the Mid-Devonian Tabberabberan Orogeny (Scheibner, 1973) but there is little or no evidence of this Proc. Linn. Soc. N.S.W., 104 (4), (1979) 1980 P. F. CARR, B. G. JONES, A.J. KANTSLER, P.S. MOORE AND A. C. COOK 243 orogenic episode in the Bungonia area. From studies in the northeastern part of the Lachlan Fold Belt, Powell and Edgecombe (1978) concluded that uplift, tilting and erosion occurred during the Middle Devonian but that there was no evidence of an intense orogenic episode beneath the Late Devonian Lambie and Catombal Groups. The Bungonia region was covered by shallow marine and terrestrial sediments of the Late Devonian Lambian Transitional Province. The folding of these beds must have occurred between the latest Devonian and Middle Permian and is probably related to the Carboniferous Kanimblan Orogeny. The sequence of deformational events recorded at Bungonia therefore can be related to the widespread orogenic episodes recognized in the southeastern Lachlan Fold Belt (e.g. Packham, 1969, 1978). The intrusion of the Early Devonian Marulan Batholith across the F, fold structures in the Late Silurian to earliest Devonian strata precludes the possibility that all the deformation occurred as a single latest Devonian to Early Carboniferous regional deformational phase as suggested by Powell et al. (1976). Remnants of flat-lying Middle Permian (Wass and Gould, 1969) Sydney Basin sedimentary rocks and Cainozoic volcanic rocks, sediments and pedogenic deposits complete the regional history. ACKNOWLEDGEMENTS We acknowledge with gratitude Dr A. J. Wright, Dr R. A. Facer and Dr R. E. Wass for discussions and comments on the manuscript. We thank R. L. Cooper, G. N. Burkitt, S. G. Jones (deceased) and all property owners in the Bungonia area for their assistance and co-operation. References Baker, C. J., 1971. — General geology of the Tolwong mines district, Shoalhaven Gorge, N.S.W. Sydney: University of Sydney, B.Sc. (Hons) thesis, unpubl. BRUNKER, R. L., and OrFENBERG, A. C., (Compilers), 1968. — Goulburn 1: 250,000 geological sheet SI 55-12. Geol. Surv. N.S.W., Sydney. CALLANDER, J. H., 1978. — A study of the silcretes near Marulan and Milton, New South Wales. In LANGFORD-SMITH, T. (ed.) Sélcrete in Australia. Armidale: Dept. Geog., Univ. New England. Carne, J. E., and Jones, L. J., 1919. — The limestone deposits of New South Wales. Min. Resour. geol. Surv. N.S.W., 25. Carr, P. F., Jones, B. G., and WricuT, A. J., 1980. — Dating of rocks from the Bungonia district, New South Wales. Proc. Linn. Soc. N.S.W., 104: 111-117. CounsELL, W. J., 1973. — The resources of the Bungonia Caves area, N.S.W. Sydney: University of Sydney, B.Sc (Hons) thesis, unpubl. Crook, K. A. W., Bein, J., Hucues, R. J., and Scott, P. A., 1973. — Ordovician and Silurian history of the southeastern part of the Lachlan Geosyncline. J. geol. Soc. Aust., 20: 113-138. E.uis, R., Hawkins, L., Hawkins, R., JAMES, J., MIDDLETON, G., Nurse, B., and WELLINGs, G., (eds), 1972. — Bungonia Caves. Sydney: Sydney Speleological Society. Fe_Ton, E. A., and HuteatrT, M.B., 1977. — Geology of the Braidwood 1: 100,000 sheet 8827. Geol. Surv. N.S.W., Sydney. GarreTty, M. D., 1987. — Geological notes on the country between the Yass and Shoalhaven Rivers. J. Proc. R. Soc. N.S.W., 70: 364-374. GiticaN, L. B., Fe_ton, E. A., and Oxcrrs, F., 1979. — The regional setting of the Woodlawn deposit. /. geol. Soc. Aust., 26; 135-140. GouLp, I. G., 1966. — The general geology of an area south of Marulan, New South Wales. Sydney: University of Sydney, B.Sc. (Hons) thesis, unpubl. Proc. Linn. Soc. N.S.W., 104 (4), (1979) 1980 244 GEOLOGY OF BUNGONIA Hutton, T. J., Twibae, C. R., Mitnes, A. R., and Rosser, H., 1972. — Composition and genesis of silcretes and silcrete skins from the Beda Valley, southern Arcoona Plateau, South Australia. J. geol. Soc. Aust., 19: 31-39. KanTSLER, A. J., 1973. — The geology of an area near Bungonia, New South Wales. Wollongong: Wollongong University College, B.Sc. (Hons) thesis, unpubl. Moore, P.S., 1976. — Silurian sediments at Bungonia, New South Wales. Sedzmentological Newsletter, 7: 21-22. —, 1979. — The stratigraphy of the Early Cambrian Edeowie Limestone Member, Flinders Ranges, South Australia. Trans. R. Soc. S. Aust., 103: 101-111. NayLor, G. F. K., 1935. — Note on the geology of the Goulburn district, with special reference to Palaeozoic stratigraphy. J. Proc. R. Soc. N.S.W., 69: 75-85. ——, 1936. — The Palaeozoic sediments near Bungonia: their field relations and graptolite fauna. J. Proc. R. Soc. N.S.W., 69: 123-134. ——, 1939. — The age of the Marulan Batholith. J. Proc. R. Soc. N.S.W., 73: 82-85. ——, 1950. — A further contribution to the geology of the Goulburn district, N.S.W. J. Proc. R. Soc. N.S.W., 83: 279-287. O’ReILLy, S. Y., 1972. — Petrology and stratigraphy of the Brayton district, New South Wales. Proc. Linn. Soc. N.S.W., 96: 282-296. OsporNnE, G. D., 1931. — The contact metamorphism and related phenomena in the neighbourhood of Marulan, New South Wales. Part I: The quartz-monzonite — limestone contact. Geol. Mag., 69: 289-314. ——, 1949. — Contributions to the study of the Marulan Batholith. Part I. The contaminated granodiorites of South Marulan and Marulan Creek. J. Proc. R. Soc. N.S.W., 82: 116-128. ——, and Loverinc, J. F., 1953. — Contributions to a study of the Marulan Batholith. Part II. The granodiorite-quartz porphyrite hybrids. J. Proc. R. Soc. N.S.W., 86: 108-118. PAcKHAM, G.H., (ed.), 1969. — The geology of New South Wales. J. geol. Soc. Aust., 16: 1-654. ——, 1978. — Timing of regional deformation in the Hill End Trough (Discussion). J. geol. Soc. Aust., 25: 361-364. PICKETT, J. W., 1967. — Report on fossils from the Goulburn district. N.S.W. Geol. Surv. Pal. Rep. No. 67/4 [ unpubl. ]. ——., 1972. — Fossils from the limestone near Bungonia Caves. N.S.W. Geol. Surv. Pal. Rep. No. 72/1 [ unpubl. ]. PoweELL, C. McA., EpGEcomBE, D. R., Henry, N. M., and Jones, J. G., 1976. — Timing of regional deformation of the Hill End Trough: a reassessment. J. geol. Soc. Aust., 23: 407-421. , and , 1978. — Mid-Devonian movements in the northeastern Lachlan Fold Belt. J. geol. Soc. Aust., 25: 165-184. ——, and Fercusson, C. L., 1979. — The relationship of structures across the Lambian unconformity near Taralga, New South Wales. J. geol. Soc. Aust., 26: 209-219. PraTT, B. T., 1964. — The origin of Bungonia Caves. J. Mining geol. Soc. Uni. N.S.W., 2: 44-51. SCHEIBNER, E., 1973. — A plate tectonic model for the Palaeozoic history of New South Wales. J. geol. Soc. Aust., 20: 405-426. SHERRARD, K., 1949. — Graptolites from Tallong and the Shoalhaven Gorge, New South Wales. Proc. Linn. Soc. N.S.W., 74: 62-68. ——, 1954. — The assemblages of graptolites in New South Wales. J. Proc. R. Soc. N.S.W., 87: 73-101. ——, 1962. — Further notes on assemblages of graptolites in New South Wales. J. Proc. R. Soc. N.S.W., 95: 167-178. SHERWIN, L., 1972. — Ordovician graptolite — conodont associations from the Goulburn district. Quart. Notes Geol. Surv. N.S.W., 6: 3-5. STAUFFER, M. R., and RickarD, M. J., 1966. — The establishment of recumbent folds in the Lower Palaeozoic near Queanbeyan, New South Wales. J. geol. Soc. Aust., 13: 419-438. Wass, R. E., and Goutp, I. G., 1969. — Permian faunas and sediments from the South Marulan district, New South Wales. Proc. Linn. Soc. N.S.W., 93: 212-226. WELLMAN, P., and McDoucaLt, I., 1974. — Potassium-argon ages on the Cainozoic volcanic rocks of New South Wales. J. geol. Soc. Aust., 21: 247-272. Woo.noucH, W. G., 1909. — The general geology of Marulan and Tallong. Proc. Linn. Soc. N.S.W., 34: 546-553. Youncs, B. C., 1978. — The petrology and depositional environments of the Middle Cambrian Wirrealpa and Aroona Creek Limestones (South Australia) . J. sed?m. Petrol., 48: 63-74. Proc. Linn. Soc. N.S.W., 104 (4), (1979) 1980 New Records of Zygnemaphyceae and Oedogoniophyceae (Chlorophyta) from northern New South Wales STEPHEN SKINNER SKINNER, S. New records of Zygnemaphyceae and Oedogoniophyceae (Chlorophyta) from northern New South Wales. Proc. Linn. Soc. N.S.W. 104 (4), (1979) 1980: 245-263. Records are given of 70 taxa from the Zygnemaphyceae and 9 taxa, including a new species Oedogonzum wissmani sp. nov., from the Oedogoniophyceae from collections of freshwater algae made in 1974. Most collections were made in the New England Tableland with two from the Clarence River Valley. They constitute the first report on the algal flora of northeastern New South Wales since Playfair’s (1914, 1915) records of algae from Lismore and the Richmond River. Stephen Skinner, 1 Monarch Ave, Parafield Gardens, Australia 5107 (formerly Department of Botany, University of Adelaide, earlier at University of New England) ; manuscript received 23 March 1979, accepted in revised form 21 May 1980. INTRODUCTION Papers on freshwater algae from Australia have been few and, with the exception of Playfair’s various papers, scattered in coverage, both of the collections and the algae. Most of the earliest records, which record algae from Tasmania and Victoria, contain no illustrations, few descriptions and no authorities for the names. There are also papers by Nordstedt (1887, 1888) and Raciborski (1892) derived from collections made by scientific travellers to Australia and New Zealand. Bailey (1893, 1895, 1898) gave much information on the Queensland algal flora including desmids and Oedogonium species. These papers are little more than compilations from the papers of the various authorities including Borge (1897, 1911), Schmidle (1896) and Moebius (1892, 1894) to whom Bailey sent specimens for determination. Hardy (1904, 1905, 1906, 1913), with the help of G. S. West, produced a series of checklists of freshwater algae, excluding diatoms, for Victoria which included original drawings and descriptions by West. West himself (1905, 1909) described the algal flora of the Yan Yean reservoir on the Yarra River, near Melbourne. Playfair, in a series of papers from 1907 to 1923, described the freshwater algal and animalcules of the Sydney and Lismore districts. He made numerous descriptions and illustrations of many desmids and allied algae but made almost no reference to Oedogoniophyceae. Although his concepts of the limits of species, especially desmids, were broad (Playfair, 1910, 1911), nevertheless he described and named numerous morphological varieties within his species which have led to subsequent nomenclatural difficulties for more recent collectors. His Supplement I (1917) to Maiden and Betche’s Census of New South Wales Plants is marred by a complete lack of localities for taxa listed. Prescott and Scott examined collections of desmids from South Australia (Prescott and Scott, 1952) and collections of freshwater algae from Arnhem Land made by the American-Australian Expedition 1948 (Scott and Prescott, 1958) which contain many new taxa. Croasdale has since completed the desmid records from the latter collections (Croasdale and Scott, 1976). More recently Tyler, in Tasmania, has Proc. Linn. Soc. N.S.W., 104 (4), (1979) 1980 246 ZYGNEMAPHYCEAE AND OEDOGONIOPHYCEAE led an upsurge in interest in freshwater algal (Tyler 1970; Thomasson and Tyler, 1971) with a return to the problem of polymorphism in desmid species (Ling and Tyler, 1972, 1974, 1976). DESCRIPTION OF THE AREA OF COLLECTION The geography and geology of the northeastern quarter of New South Wales are rather complex. The tablelands, which rise to 1600 m, consist largely of a much faulted granitic batholith and associated metamorphic rocks. Much of the area shows traces of extensive volcanic capping during the Tertiary. The Clarence River system, draining the northeast of the tableland and following the escarpment for about half the river’s length, traverses a sedimentary basin of Jurassic to Cretaceous age in its run to the sea. In the tablelands the water bodies are shallow lagoons or weed-choked but swiftly flowing streams; on the coastal plain, billabongs and lagoons frequently occur in association with the middle river. Both the coastal and montane shallow lagoons (Baldersleigh Lagoon; Dangar’s Lagoon, Uralla; the Mother of Ducks Lagoon system, Guyra; and the swamp billabong at Deep Creek, near Baryulgil on the Clarence) are species-rich, as are the various creeks and small rivers. The richest algal floras have developed in the swamps and sluggish creeks of old mining sites especially where the country rock is granitic (gold mines on the Ann River, Backwater; the tin mines on Majors Ck, Howell near Tinga). Comparable floristic variety is found in the alpine bogs near Round Mountain and Point Lookout. The deeper bodies of water, on basalt-derived sediments (Llangothlin Lagoon system) are species-poor, although often highly productive. Author citations, except for a few more recently published taxa, have been limited to the author’s name and date of publication only. The major references used have been Krieger (1937-1944) and Krieger and Gerloff (1962-1969) for the desmids, Kolkwitz and Krieger (1944) and Randhawa (1959) for the filamentous Zygnemaphyceae, and Tiffany (1930) and Gauthier-Liévre (1963-1964) for the Oedogoniophyceae. Further references for species are mostly restricted to those published on Australian collections. L = length of cell; W = width of cell; WM = median width; WP = polar width; T = thickness; I = isthmus; D = diameter of zygospore. The higher order classification used here follows Ruzicka (1979) for the desmids, with the orders and families arranged to follow Mix (1972) who based her rearrangement on the wall ultrastructure common to each group. The name Zygnemaphyceae of Round (1971) is preferred to Conjugatophyceae of Fott (1959) as it incorporates the name of the type genus and family. The filamentous taxa are classified according to the families designated by Randhawa (1959), and the ordinal status of the Mesotaeniales is retained. Specimens have been deposited in the Herbarium of the Botany Department, University of New England. Type material of Oedogonium wissmani sp. nov. is stored at the National Herbarium, Royal Botanical Gardens, Sydney. ZYGNEMAPHYCEAE ZYGNEMALES Mougeotiaceae: Although vegetative and reproductive filaments of taxa in this family were often encountered in collections, no fully mature zygospores were found. Proc. Linn. Soc. N.S.W., 104 (4), (1979) 1980 S. SKINNER 247 Zygnemaceae: Zygnema coeruleum Czurda 1932. Kolkwitz and Krieger, 1941: 227, figs 237, 238. Gauthier-Liévre, 1965: 50, pl. 12, fig. 6. Randhawa, 1959: 227, fig. 163, a, b. Cells L/B 3-4, 20-25 um in diameter, wall ends lenticular. Zygospores 30-35 um in diameter, mesospore wall blue with ellipsoid depressions forming a pattern over the surface. Majors Creek, Howell near Tinga (Garrard, July 1974). Spirogyra submaxima Transeau 1914. Kolkwitz and Kneger, 1941: 141, figs 637, 638. Individual filaments discernible with the naked eye, or low magnification. Cells large, L/B 2-3(—5), 80-120 um wide, end wall lenticular, chloroplasts 7-10, each with 1 to 2 turns. Conjugation scalariform; conjugation tube of two cups, median to cells; receiving cells all in one filament; zygospore round to slightly ovoid in outline, mesospore smooth, golden brown; diameter 90-115 ym. Gwydir River, Bundarra, with zygospores (Schnezder, March 1974) ; Aberfoyle River (Skznner, March 1974); Falconers Creek, Guyra (Skinner Dec. 1974) ; Mother of Ducks Lagoon, Guyra (Skznner, Dec. 1974). Spirogyra westii Transeau 1934. Kolkwitz and Krieger, 1941: 381, fig. 558, 559. Gauthier-Liévre, 1965: 167, pl. 63, fig. A, a-4. Randhawa, 1959: 310, fig. 279. Cells narrow, 20-25 um wide, L/B 4-5, end wall lenticular; chloroplast single, with 4-7 turns, with numerous pyrenoids. Conjugation scalariform; conjugation tube of two cups, towards one end of both donor and receiver cells, a little more terminally in the slightly inflated receiving cell, all receiving cells in the one filament. Zygospore ellipsoid, 65-70 x 30-35 um, suture line median, mesospores golden brown. Majors Creek, Howell, near Tinga (Garrard, April-July 1974) ; Sandy Creek, near the dog-gate, Armidale-Dorrigo Road (Skinner, Dec. 1974). Sirocladiaceae: Strogonium sticticum (Eng. Bot.) Kutzing 1849. Bailey, 1898: 10, pl. 4. Gauthier- Liévre, 1965: 186, pl. 72, B, b-é. Randhawa, 1959: 424, pl. 508 (after Jao). Schmidle, 1896: 303. Spirogyra stictica (Eng. Bot.) Wille. Kolkwitz and Krieger 1941: 429. L 130- 160 um; W 60-65 um; D 65x70 um. Aberfoyle River (Skinner, March, July, Oct. 1974); Falconers Ck; (Skznner, Dec. 1974); Little Guyra Lagoon (Skinner, Dec. 1974); Cooney Ck, near Hillgrove (Skznner, Dec. 1974). MESOTAENIALES Mesotaeniaceae: Spirotaenia condensata Bréb. in Ralfs 1848. Krieger, 1937: 181, pl. 2, fig. 1. L 160- 165 wm; W 22-25 um. Backwater (Wzssman, Feb. 1974) ; Baldersleigh, near Kingston (Wzssman, Oct. 1974) ; Howell, near Tinga (Garrard, July 1974). Spirotaenza obscura Ralfs 1848. Krieger 1937: 180, pl. 1, fig. 5, 6. Playfair 1907: 170, pl. 3, fig. 2. This taxon was found in pairs in gelatinous sheaths, otherwise it agrees with Krieger (1937). L. 75-80 um; WM 10 wm; WP 5-7 um. Fig. 1, 1. Sandy Ck, near the dog-gate, Armidale-Dorrigo Road (Skinner, Dec. 1974). Netrium digitus var. lamellosum (Bréb.) Gronblad 1920. Krieger, 1937: 219, pl. 7, fig. 6. Netrzum lamellosum Krieger, 1932: 158, pl. 3, fig. 5. A form which differs from N. digitus var. digitus by having straight cell walls in Proc. Linn. Soc. N.S.W., 104 (4), (1979) 1980 248 ZY GNEMAPHYCEAE AND OEDOGONIOPHYCEAE the middle of the cell; very common. L 200-350 wm; WM 75-85 um; WP 30 um. Backwater (Skinner, March 1974); Baldersleigh (Wzssman, Oct. 1974) ; Bullock Ck, Point Lookout (Skznner, Dec. 1974); Cooney Ck, near Hillgrove (Skinner, Dec. 1974) ; Deep Ck, near Baryulgil, swamp (Skznner, Nov. 1974). Netrium digitus var. rhomboideum Gronblad 1920. Krieger, 1937: 218, pl. 7, fig. 5. A variety which is smaller and more rhomboidal than the type. L 150-170 um; WM 30-35 wm; WP 20-25 um. Backwater, fen (Skinner, March, Dec. 1974); Llangothlin Lagoon (Skznner, Sept. 1974) ; Majors Ck, Howell (Garrard, June 1974; Wissman, August 1974). Gonatozygaceae: Gonatozygon monotaenium var. pilosellum Norst. 1886. Scott and Prescott, 1958: 22, fig. 3.14. Playfair, 1915: 317. Gonatozygon kinahanw var. monotaentum Playfair, 1912: 506, pl. 54, fig. 4. L 140-150 um; WM 10 pm; WP 12 um. Dumaresgq Creek, University of New England, Armidale (Skznner, Feb. 1974). Genicularia spirotaenza de Bary 1858. With two spiral, ribbon-like chloroplasts; cells often bent or curved. L 200- 230 um; W 12 um. Howell, near Tinga (Garrard, April 1974); Sandy Creek, near the dog-gate, Armidale-Dorrigo Road (Skinner, Dec. 1974). Peniaceae: Pentium cylindrus (Ehrenb.) Brébisson in Ralfs 1848. Krieger, 1937: 234, pl. 9, fig. 9- 12. Scott and Prescott, 1958: 22, pl. 1, fig. 20; 1961: 9, pl. 1, fig. 11. Cells with 3-5 or more sutures; L 20-45 um; W 6-8 pm. Backwater, swamp (Skznner, March, June, Dec. 1974). Penium margaritaceum (Ehrenb.) Bréb. in Ralfs 1848. Krieger 1937: 230, pl. 10, figs 2-4. 1150-190 um; W 20 pm. Styx River state forest, soakage pool (Skznner and Wissman, Feb. 1974) ; Dumaresq Ck, U.N.E., Armidale (Skznner, Feb. 1974). Penium phymatosporum Nordst. 1876. Krieger, 1937: pl. 11, figs 14-17. Small cells with smooth walls, L/B 3, 7-10 um in diameter. Zygospore irregularly mamillate, D 20-30 um. Fig. 1, 2. Baldersleigh, near Kingston, lagoon (Wzssman, Oct. 1974). Pentium spirostriolatum Barker 1869. Krieger, 1937: 227, pl. 9, figs 1-6. Playfair, 1908: 607, pl. 11, fig. 5; 1910: 490, pl. 13, fig. 24. I 140-160 um; W 10-15 um. Backwater (Wissman, Feb. 1974; Skinner, March 1974); Little Styx River, Point Lookout (Skinner and Wissman, Feb. 1974); Howell (Garrard, April- July 1974) ; Bullock Ck, Point Lookout, bog (Skznner, Dec. 1974). Closteriaceae : Clostertum cuspidatum Bailey in Ralfs 1848. Spinoclostertum curvatum Bernard, 1909: 31, pl. 2, fig. 35. Spinoclostertum cuspidatum (Bail.) Hirano. Scott and Prescott, 1958: 24, pl. 1, fig. 17. Spinoclosterium curvatum var. spinosa Prescott, 1940: 99. L 200-230 um WM 40 um; WP 15 um. Backwater, swamp (Skznner, March, June 1974). Proc. Linn. Soc. N.S.W., 104 (4), (1979) 1980 S. SKINNER 249 Clostertum ehrenbergu Menegh. 1840. Krieger, 1937: 285, pl. 17, fig. 1. pl. 18, fig. 1. Bailey, 1893: 42. Hardy, 1905: 66. Moebius, 1892: 441. Prescott and Scott, 1952: 56. Playfair, 1914: 100. L 200-250 um; W max 45 um. Little Styx River, Point Lookout, bog (Skinner and Wissman, Feb. 1974). Closterium tdiosporum West and West 1900. Krieger, 1937: 271, pl. 15, fig. 1, 2. L 150-160 ym; MW 15 um. Zygospore ovoid, densely papillose with a brown mesopore, held tightly between the four semicells, D 20 x 45 um. Fig. 1, 3a, b. Sandy Ck, near the dog-gate, Armidale-Dorrigo Road (Skznner, Dec. 1974). Closterrum kutzingw Bréb. 1856. Krieger, 1937: 351, pl. 32, fig. 8, 9. Bailey, 1893: 42, 1898: 33. Hardy, 1905: 66; 1906: 41. Moebius, 1892: 441. Prescott and Scott, 1952: 57, pl. 1, fig. 8. Schmidle, 1896: 304. Scott and Prescott, 1958: 23, pl. 1, fig. 14. Thomasson, 1973: 392. West, 1909: 14. A very variable species; L 180-250 um; WM 8-20 um. Backwater (Wzssman, Feb. 1974; Skinner, March, June 1974); Round Mountain, drain in bog (Wzssman, Nov. 1974); Deep Ck, near Baruylgil, swamp (Skinner, Nov. 1974). Clostertum ltbellula var. interruptum (West and West) Donat 1926. Krieger, 1937: 256, pl. 12, fig. 6. Scott and Prescott, 1958: 24, pl. 1, fig. 6. As noted by Scott and Prescott (1958), this species has distinctive terminal vacuoles with gypsum statoliths, thus distinguishing it from either Penzuwm or Netrium. L 145-170 um; WM 20-25 um. Styx River state forest, soakage pool (Skinner and Wissman, Feb. 1974) ; Backwater, fen (Skznner, March, Dec. 1974) ; Majors Ck, Howell near Tinga (Garrard, June 1974) ; Mother of Ducks Lagoon, Guyra (Skznner, Dec. 1974) ; Sandy Ck, near the dog-gate, Armidale-Dorrigo Road (Skinner, Dec. 1974) ; Bullock Ck, Point Lookout, bog (Skznner, Dec. 1974). Clostertum lunula (Mull.) Nitzsch 1817. Krieger, 1937: 301, pl. 21, fig. 1, pl. 22, fig. 1. Hardy, 1906: 36. Closterrum lunula forma giganteum (Bernard) Playfair, 1908: 605, pl. 11, fig.2. This very large species is often readily visible to the naked eye. L 800-1100 um; W 90-120 um. Little Styx River, bog (Skinner and Wissman, Feb. 1974); Backwater (Wissman, Feb. 1974; Skznner, March 1974) ; Aberfoyle River (Skznner, June 1974); Llangothlin Lagoon (Skznner, Sept. 1974); Sandy Ck, near the dog- gate, Armidale-Dorrigo Road (Skznner, Dec. 1974) ; Cooney Ck, near Hillgrove (Skinner, Dec. 1974). Closterium moniliferum (de Bary) Ehrenb. 1838. Krieger, 1937: 289, pl. 18, figs 6, 7 L 180-230 uml W: max 40 pm. Llangothlin Lagoon (Skinner, Sept. 1974) ; Dangars Lagoon, Uralla (Skznner, Dec. 1974) ; Pyes Ck, near Tenterfield (Skznner, Jan. 1975). Clostertum nematozdes Joshua 1886. Krieger, 1937: 370, pl. 37, fig. 2. Croasdale and Scott, 1976: 508, pl. 1, fig. 7. Scott and Prescott, 1958: 24, pl. 1, fig. 12. L 80-110 wm; WM 20-25 um. Little Styx River, bog (Skinner and Wissman, Feb. 1974); Dumaresq Ck, U.N.E., Armidale (Skinner, March 1974) ; Majors Ck, Howell (Garrard, May 1974) ; Round Mountain, drain in bog (Wessman, Nov. 1974); Baldersleigh Proc. Linn. Soc. N.S.W., 104 (4), (1979) 1980 250 ZYGNEMAPHYCEAE AND OEDOGONIOPHYCEAE near Kingston, swamp (Wzssman, Oct. 1974); Bullock Ck, Point Lookout (Skinner, Dec. 1974). DESMIDIACEAE Gronbladia neglecta (Racib.) Teiling 1952. Scott and Prescott, 1961: 122, pl. 61, fig. 7 Cells L/B 4-6, W 15-20 um, forming very long chains. Zygospore, present in March sample, irregular cruciform, D 80-85 um. Fig. 1, 4. Backwater, swamp (Skinner, March, June, Dec. 1974). Hyalotheca dissiliens (Sm.) Brébisson in Ralfs 1844. Bailey, 1893: 38, pl. 12, fig. 28; 1895: 37; 1898: 12. Borge, 1911: 203. Hardy, 1905: 70. Moebius, 1892: 439. Prescott and Scott, 1952: 68. End view of cell circular; cell wall of ten with fine plications; L 14-18 ym W 15 um; Diameter of cell 15 um. Zygospore ovoid, D 50 x 35 um. Backwater (Wissman, Feb. 1974); Aberfoyle River (Skinner, June 1974) ; Round Mountain (Wzssman, Nov. 1974); Deep Ck, near Baryulgil, swamp, with zygospores (Skznner, Dec. 1974). Hyalotheca hians Nordstedt 1888, Bailey, 1898: 12, pl. 5, fig. la, b. End view of cell oval, with two antipodal peaks; walls smooth, with a central invagination; L 20-25 um; W 20-25 um; Diameter of cell 25 ym. Backwater (Skznner, March 1974) ; Howell (Garrard, June 1974). Hyalotheca mucosa (Dillw.) Ehrenberg 1840. Scott and Prescott, 1958: 69, pl. 1, fig. 19 Cells cylindrical, with double rings of fine plications towards either end; L 15- 25 um; W 15 um. Backwater (Skznner, June 1974); Sandy Ck, near the dog-gate, Armidale- Dorrigo Road (Skinner, Dec. 1974) ; Cooney Ck, near Hillgrove (Skznner, Dec. 1974). Phymatodocts nordstedtiana Wolle 1884. Scott and Prescott, 1961: 123, pl. 61, fig. 9, 10. L 25-30 uymum; W 30-40 um; 1 25 um. Backwater, swamp (Skinner, March, Dec. 1974); Round Mountain, drain in bog (Wzissman, Oct. 1974); Bullock Ck, Point Lookout, fen (Skznner, Dec. 1974. Desmidium bailey: (Ralfs) Nordstedt 1880. Prescott and Scott, 1952: 68, pl. 3, fig. 14. Schmidle, 1896: 303. This form, which is similar to the South Australian form, is very like that of Rich (1932, fig. 17C), but shows arms linking across the sinus, and is more squared off at the corners of the cell. L 25 um; W 30 um. Fig. 1, 6. Backwater (Skznner, March, June 1974). Desmidium suboccidentale Scott and Prescott, 1958: 70, pl. 21, fig. 9, 1961: 125, pl. 63, fig. 7. Cells a little larger than Northern Territory form, with greater constriction of the lateral lobes, otherwise similar; L 17-20 um; W 20-30 um; 1 15-20 um. Fig. 1, 5a, b. Backwater, fen (Skinner, June, Dec. 1974). Desmidium swartza C. Agardh 1824. Scott and Prescott, 1958: 70, pl. 21, fig. 18. Hardy, 1905: 71. Thomasson, 1973: 392. West, 1909: 16. Some chains of cells very long indeed, and this species may occur as the dominant photosynthetic organism at a site. The form from Baryulgil is less Proc. Linn. Soc. N.S.W., 104 (4), (1979) 1980 S. SKINNER 251 See M2 Tt ay v bY af T yy M Fig. 1. 1, Spirotaenia obscura, Sandy Ck; 2, Penium phymatosporum, Baldersleigh, swamp; 3a, b, Clostertwm idiosporum, Sandy Ck; 4, Gronbladia neglecta, Backwater, swamp; 5, Desmidium suboccidentale, Backwater, fen; 6, D. bazley:, Backwater, swamp; 7a,b, Tetmemorus brebzssoni?, Baldersleigh, swamp; 8a,b, Euastrum longicolle var. capitatum, Backwater, fen; 9, Mrcrasterzas mahabuleshwarensis, (a) Bullock Ck, Point Lookout; (b) Cooney Ck; 10a, b, M. tropica var. indivisa, Baldersleigh, swamp; 11, Stauwrastrum bicorne, Backwater, swamp; 12a,b, S. sexangulare, Deep Ck, Baryulgil swamp; 13, Xanthidium inchoactum, Backwater, swamp; 14, Cosmartum askenasy, Bullock Ck, Point Lookout; 15, C. botryt7s, Dumaresq Ck, Armidale; 16, C. rotundum, Baldersleigh, swamp. 50 um scale, for 1; 2; 3a,b; 5; 6; 9a, b; 11; 14; 15. 60 um scale, for 4; 7; 8a,b; 10a, b; 12a, b; 13; 16. Proc. Linn. Soc. N.S.W., 104 (4), (1979) 1980 252 ZYGNEMAPHYCEAE AND OEDOGONIOPHYCEAE ornate than usual, the Round Mountain form is very large. L 15-25 um; W 30-50 um; I 35-45 um. Round Mountain (Wzsman, Oct. 1974); Sandy Ck, near the dog-gate, Armidale-Dorrigo Road (Skznner, Dec. 1974) ; Deep Ck, near Baryulgil, swamp (Skenner, Nov. 1974). Tetmemorus brebtssonz (Meneghini) Ralfs 1844. Krieger, 1937: 452, pl. 54, fig. 1-5. Bailey, 1893: 43. Prescott and Scott, 1952: 58. Scott and Prescott, 1958: 28. A very large form, L 230-300 um; WM 50-70 um; WP 20-25 um; I 30-45 um; from Baldersleigh and Mother of Ducks Lagoon (compare with a similar sized form of Prescott and Scott (1952), from Mt. Compass, South Australia), and, more commonly, a smaller form, L 90-110 ym; WM 20-30 um; 110 um. Fig. 1, 7a, b. Backwater (Skznner, March, June, Dec. 1974); Baldersleigh, near Kingston, swamp, both forms (Wzssman, Sept. 1974); Round Mountain, drain in bog (Wissman, Oct. 1974); Bullock Ck, Point Lookout (Skinner, Dec. 1974); Mother of Ducks Lagoon, Guyra, large form (Skznner, Dec. 1974). Tetmemorus granulatus (Breb.). Ralfs 1844. Krieger, 1937: 458, pl. 55, fig. 1-5. Schmidle, 1896: 304. L 70-80 um; WM 14-18 um; WP 10 pum. Baldersleigh, near Kingston, swamp (Wzssman, Sept. 1974). Tetmemorus laevis (Kutzing) Ralfs 1844. Krieger, 1937: 455, pl. 54, fig. 9-12. Prescott and Scott, 1952w: 58. L. 75-85 um; WM 25-30 um; WP 20 um; I 22 um Styx River state forest, soakage pool (Skznner and Wissman, Feb. 1974). Pleurotaentum nodosum (Bailey) Lundell 1871. Krieger, 1937: 436, pl. 47, fig. 1. Bailey, 1893: 44. Hardy, 1905: 66. Docidium nodosum Bailey 1898: 30, pl. 16, fig. 12. L 200-360 um; WM 55-65 um; WP 20-28 um; I 30-35 um. Backwater, fen (Skenner, June 1974); Round Mountain, drain in bog (Wissman, Oct. 1974) ; Bullock Ck, Point Lookout, bog (Skznner, Dec. 1974). Pleurotaentum ovatum var. tumzdum (Maskell) G.S. West zn Hardy, 1906; 21.G. S. West, 1909: 54, pl. 6, fig. 9. Krieger, 1937: 435: pl. 50, fig. 2, 3. L 200-250 um; WM 100-120 um; WP 30-35 um; 155 um. Bailey (1893, 1895) may also be discussing this taxon, as Moebius’ (1892) variety appears to be a variation from the Queensland form rather than the type. Bullock Ck, Point Lookout, bog (Skznner, Dec. 1974). Pleurotaenium verrucosum (Bailey) Lundell 1871. Krieger, 1937: 438, pl. 51, fig. 13. This form has pointed coronal teeth, perhaps agreeing more fully with var. bulbosum Krieger, 1937: 439, pl. 51, fig. 5. L 300-350 um; WM 35-40 um; WP 20-25 um; 131-35 um. Deep Ck, Baryulgil, swamp (Skznner, Nov. 1974). Triploceras gracile Bailey 1851. Krieger, 1937: 442, pl. 52, fig. 1-7. Bailey, 1893: 44, fig. 36, 1895: 38. Hardy, 1905: 66. Schmidle, 1896: 304. A number of varieties of this plastic species have been described (Prescott and Scott, 1952; Scott and Prescott, 1958; Thomasson, 1973) for Australian specimens. Although the specimens collected in the present survey showed some variation, they are treated as members of one variable taxon here. L 350-415 ym; W 30-40 um; I 30-35 wm. Zygospore with 14 several times furcate spines, mesospore brown, D 60-75 um. Backwater (Skinner, March, June (with zygospores), Dec. 1974); Round Mountain (Wissman, Oct. 1974); Bullock Ck, Point Lookout (Skznner, Dec. Proc. LINN. Soc. N.S.W., 104 (4), (1979) 1980 S. SKINNER 953 1974) ; Cooney Ck, near Hillgrove (Skznner, Dec. 1974); Deep Ck, near Baryulgil swamp (Skznner, Nov. 1974). Euastrum longicolle var. australicum Playfair, 1907: 172, pl. 3, fig. 6. Krieger, 1937; 494, pl. 61, fig. 1. L120 ym; WM 70 um; WP 35 um; 115 pm. Baldersleigh, near Kingston, swamp (Wzssman, Sept. 1974). Euastrum longicolle var. capitatum West and West 1902. Krieger, 1937: 494, pl. 60, fig. 11. Croasdale and Scott, 1976: 518, pl. 4, figs 1, 2. Scott and Prescott, 1958: 36, pl. 4, fig. 3. L 100-110 ym; WM 50 um; WP 30-33 um; I 15 um. Zygospore spherical to ovoid, mesospores red brown, spines simple and coarse, with four pointed anvil shaped spines holding the empty semicells to the spore, D 50-65 um. This zygospore with its anvil spines does not agree fully with Croasdale and Scott (1976). Fig. 1, 8a, b, c. Backwater, fen (Skznner, March, June, Dec. 1974), spores present in all samples) . Euastrum spinulosum var. tnermis Nordstedt 1888. Krieger, 1937: 635, pl. 93, fig. 8- 10. L 60 wm; W 55 um; 112 pm. Howell, near Tinga (Garrard, June 1974) ; Baldersleigh, near Kingston, swamp (Weissman, Sept. 1974) ; Bullock Ck, Point Lookout (Skznner, Dec. 1974). Euastrum turnert W. West. 1893. forma. L 35-40 um; WM 25-30 um; WP 20-22 um; 19-11 um. Backwater (Wissman, Feb. 1974; Skznner, March, June, Dec. 1974); Baldersleigh, near Kingston (Wissman, Sept. 1974); Round Mountain (Wissman, Oct. 1974); Mummulgum, Bruxner Highway (Wissman, Nov. 1974) ; Cooney Ck, near Hillgrove (Skznner, Dec. 1974). Micrasterias alata Wallich 1890. Scott and Prescott, 1958: 339, pl. 7, fig. 1, 2; Croasdale and Scott, 1976: 522, pl. 7, fig. 8. Tyler, 1970: 219, fig. 18, A, B. L 145-155 wm; W 150-165 wm; 125 um. Deep Ck, Baryulgil, swamp (Skinner, Nov. 1974); Cooney Ck, near Hillgrove (Skznner, Dec. 1974). Micrastertas anomala Turner 1893. Scott and Prescott, 1958: 39, pl. 10, fig. 2; 1961: 46, pl: 119) fig. A-3. Tyler) 1970: 219) fig. 23. Xanthidium bifurcatum Borge 1897: 16. Bailey, 1898: 19, pl. 14, 5a-c, 6a-c. Scott and Prescott, 1958: 56, pl. 10, fig. 3. Xanthidium pulcherrimum Playfair, 1907: 180, pl. 4, fig. 10. Xanthidium gloriosum G.S. West zn Hardy, 1906: 19. Playfair, 1908: 620. This very large desmid was found in two collections, only once in the Backwater collection. The form found fits Playfair’s description (Playfair, 1907) and plate, although somewhat larger. The differences between the various specimens in the literature have been delimited by each author. Until this taxon (or complex) can be studied in culture the nomenclature will remain uncertain. L 290-310 um; WM 165 um; WP 60 um; 1 45 um. Backwater, swamp (Skznner, June 1974) ; Bullock Ck, Point Lookout (Skznner, Dec. 1974). Micrasterzas jennert Ralfs 1848. Tyler, 1970: 224, fig. 28, B, C. L 200-320 um; W 100-120 um; 135 um. Backwater (Skznner, March 1974); Baldersleigh, near Kingston (Wessman, Sept. 1974) ; Sandy Ck, near the dog-gate, Armidale-Dorrigo Road (Skznner, Proc. Linn. Soc. N.S.W., 104 (4), (1979) 1980 254 ZYGNEMAPHYCEAE AND OEDOGONIOPHYCEAE Dec. 1974). Micrasterias mahabuleshwarensis Hobson 1863: Tyler, 1970: 216, fig. 11-15, 17. Bailey, 1895: 42, pl. X, fig. 14. Borge, 1911: 203. Playfair, 1915: 330. Tyler (1970) shows in his fig. 17 the range of variation in this taxon, in south eastern Australia, from forma ‘typica’ to forma “Wallichii’, and both ends of this range have been found among the northern tablelands specimens. The records of other forms and varieties [var. reducta West zn Hardy, 1905, Scott and Prescott, 1958, var. ampullacea (Mask.) Nordst. fa. australiensts Prescott and Scott, 1952] may also prove to be forms of this graded series. Fig. 1, 9a, b. forma ‘typica’ Bullock Ck, Point Lookout (Skznner, Dec. 1974) ; Sandy Ck near the dog-gate, Armidale-Dorrigo Road (Skznner, Dec. 1974); Yellow Gap, Guyra-Mt. Mitchell Road, swamp (Skinner, March 1974). forma ‘Wallichii’ Cooney Ck, near Hillgrove (Skinner, Dec. 1974). Micrasterias moebit (Borge) West and West 1894. Scott and Prescott, 1958: 41, pl. 8, fig. 5, 6. Euastrum turgidum var. moebit (W. andG.S. West) Playfair, 1915: 329. L 90-100 ym; WM 90 um; 155 um. Dumaresq Ck, U.N.E., Armidale (Skznner, Feb. 1974) ; Backwater (Wzssman Feb. 1974) : Mummulgum, Bruxner Highway, swamp (Wissman, Nov. 1974). Micrasterias thomaszana var. notata (Nordst.) Gronblad 1920. Tyler, 1970: 225, fig. 29, A-C. Prescott and Scott, 1952: 60, pl. 4, fig. 3. The northern tablelands form of this species is without much ornamentation, like Tyler (1970), fig. A. & C. L 200-250 um; W 165-180 ym 1 50 um. Backwater (Wissman, Feb. 1974; Skinner, March 1974); Baldersleigh (Wissman, Sept. 1974); Oakey River Hydroelectricity Dam, near Jeogla (Skinner, Feb. 1974). Micrastertas tropica var. indivisa (Nordst.) Eichl. and Rac. 1893. Tyler, 1970: 219, fig. 18 C, D. The form of this taxon from the northern tablelands differs from those figured by Tyler (1970) in the possession of two (not just a single) circular raised processes on each face of each semi-cell, one below the other. L 90-120 pm; MW 80-90 um; WP 70 um; 150-55 um. Zygospore (in Baldersleigh sample) spherical with a mixture of simple and bifurcated spines, randomly distributed, mesospore brown, D 65-70 um. Fig. 1, 10a, b. Baldersleigh, near Kingston, with zygospore (Wessman, Sept. 1974); Round Mountain (Wissman, Oct. 1974); Cooney Ck, near Hillgrove (Skinner, Dec. 1974) ; Bullock Ck, Point Lookout (Skznner, Dec. 1974); Sandy Ck, near the dog-gate, Armidale-Dorrigo Road (Skznner, Dec. 1974). Staurastrum bicorne Hauptfl. 1888. forma L 50 um; W 60 wm; 115 um. Fig. 1, 11. Backwater (Skinner, March, June 1974); Deep Ck, near Baruylgil, swamp (Skinner, Nov. 1974). Staurastrum dickiet Ralfs 1848. Prescott, 1940: 91, pl. 2, fig. 8, 9. Hardy, 1905: 69. L 60-65 um; W 60-65 um; 18 pm. Backwater (Wissman, Feb. 1974); Round Mountain (Wissman, Oct. 1974) ; Proc. Linn. Soc. N.S.W., 104 (4), (1979) 1980 S. SKINNER 255 Deep Ck, near Baryulgil (Skznner, Nov. 1974) ; Cooney Ck, near Hillgrove. (Skenner, Dec. 1974) ; Dangar’s Lagoon, Uralla (Skinner, Dec. 1974). Staurastrum longispinum (Bailey) Archer. L 80 wm; W 100-110 mm; I 35 pm. Backwater, swamp (Wissman, Feb. 1974; Skinner, March, June 1974) ; Bullock Ck, Point Lookout (Skznner, Dec. 1974). Staurastrum pinnatum Turner 1892. L 30 wm; W 50 um; I 23 um. Deek Ck, Baryulgil, swamp (Skznner, Nov. 1974); Cooney Ck, near Hillgrove (Skinner, Dec. 1974). Staurastrum sagittarium Nordstedt 1887. Thomasson, 1973: 393, pl. 32, figs 7, 8. Hardy, 1905: 69. Moebius, 1892: 446, fig. 18. Prescott and Scott, 1952: 67, fig. 5, 5. Schmidle, 1896: 312. Scott and Prescott, 1958: 65, pl. 18, figs 3, 4. L 40-45 um; W 60 um; I 30 um. Backwater (Skinner, June 1974). Staurastrum sexangulare Lundell, 1871. Thomasson, 1973: 387, pl. 34, fig. 1. Hardy, 1905: 69. Playfair, 1907: 185, pl. 5, fig. 11. An ornate form; not as simple as Scott and Prescott (1958), pl. 18, fig. 1, occasional five-armed form found. Thomasson (1973) comments on the variety of forms displayed by this taxon. L 40-42 um; W 60-65 um; radius (top view) 65-70 um; 1 30 um. Fig. 1,12 a,b. Backwater (Skznner, March, June 1974); Majors Ck, Howell, near Tinga (Garrard, June 1974) ; Deep Ck, near Baryulgil, swamp (Skznner, Nov. 1974). Xanthidium hastiferum Turner 1892. Thomasson, 1973: 387, pl. 34, 7. Hardy, 1905: 68, 41. West, 1909: 15. L 75-80 um; W 65 um; 1 25 um. Backwater (Skinner, June 1974); Bullock Ck, Point Lookout, bog (Skznner, Dec. 1974). Xanthidium inchoactum Nordstedt 1887. Playfair, 1915: 330, pl. 42, fig. 9a. Form very close to # mamillatum described by Playfair (1908), except that the triangular processes at either end of the sinus may be missing in one semicell. L 30-35 um; W 35-40 um; 112-15 wm. Fig. 1, 13. Backwater (Skinner, March 1974). Xanthidium octonarium var. cornutum Playfair, 1908: 620, pl. 12, fig. 7. Thomasson, 1973: pl. 33, fig. 7, 9. L 70 um; W 50 pm; 1 20 pm. Backwater (Skznner, March 1974) ; Majors Ck, Howell, near Tinga (Garrard, April-June 1974) ; Baldersleigh (Wzssman, Sept. 1974). Cosmarium amplum Nordstedt 1888. Bailey, 1898: 29, pl. 4, fig. 2a-d. Schmidle, 1896: 309. L 95-105 um; W 65-80 jim; 125-29 um; T 45-50 um. Fig. 2, 1. Baldersleigh, near Kingston, swamp (Wzssman, Sept. 1974). Cosmarium askenasyi Schmidle 1895. Bailey, 1898: pl. 15, fig. 9a, b. Scott and Prescott, 1961: 54, pl. 23, fig. 4. Cosmarium species Moebius in Bailey, 1895: 40, pl. 10, fig. 20. Cosmarium askenasyi var. cratertforme Playfair, 1915: 327, pl. 42, fig. 6. This form is similar to but not quite as wide as fa. latum of Scott and Prescott (1958). Proc. Linn. Soc. N.S.W., 104 (4), (1979) 1980 256 ZY GNEMAPHYCEAE AND OEDOGONIOPHYCEAE L 135-145 wm; W 120-130 um; 155 um. Fig. 1, 14. Bullock Ck, Point Lookout, bog (Skznner, Dec. 1974). Cosmarium botrytis (Bory) Meneghini 1840. Bailey, 1898: 28, pl. 6, fig. 13, a-g. L 35-50 um; W 35-45 um; I 12-20 um. Fig. 1, 15. Dumaresq Ck, U.N.E., Armidale (Skznner, Feb. 1974); Baldersleigh, near Kingston, swamp (Wissman, Sept. 1974); Bullock Ck, Point Lookout, bog (Skinner, Dec. 1974). Cosmarium denticulatum Borge 1897. Bailey, 1898: 21, pl. 15, fig. 5a-c. Scott and Prescott, 1958: 45, pl. 13, fig.4. L 150-175 pm; W 70-80 wm; 155 pm. Dumaresq Ck, U.N.E., Armidale (Skznner, Feb. 1974); Major’s Ck, Howell, near Tinga (Garrard, June 1974); Backwater, swamp (Skznner, June 1974) ; Round Mountain, drain in bog (Wzssman, Oct. 1974) ; Mummulgum, Bruxner Highway (Wzsman, Nov. 1974); Bullock Ck, Point Lookout, bog (Skznner, Dec. 1974). Cosmarium dentiferum Corda 1839. Playfair, 1914: 104, pl. 3, fig. 18. Prescott and Scott, 1952: 60, pl. 4, fig. 7. L 80 um; W 80 um; I 20 pm. Sandy Ck, near the dog-gate, Armidale-Dorrigo Road (Skznner, Dec. 1974). Cosmarium glyptodermum West and West. Playfair, 1908: 619. L 110-125 um; W 50-70 um; I 20-25 um. Fig. 2, 2. Baldersleigh, near Kingston, swamp (Wzssman, Sept. 1974). Cosmarium lundellit Delp. 1877. Borge, 1911: 200, pl. 2, fig. 3. Scott and Prescott, 1958: 47, pl. 12, fig. 19. L 120-130 um; W 90-95 um; 14-5 um. Fig. 2, 3. Backwater (Wzssman, Feb. 1974; Skinner, June 1974). Cosmarium magnificum Nordstedt 1887. Playfair, 1914: 104. L 100-110 um; W 85-96 um; I 35 um. Zygospore with simple spines, D 80 um. This form shows some of the pits described by Scott and Prescott (1961), but is not quite as highly ornamented. Fig. 2, 4. Backwater, swamp, with spores (Skinner, March, July 1974); Deep Ck, near Baryulgil, swamp (Skznner, Nov. 1974); Bullock Ck, Point Lookout, bog (Skenner, Dec. 1974). Cosmaritum obsoletum (Hautzsch.) Reinsch 1867; Scott and Prescott, 1958: 47, pl. 12, fig. 17. Bailey, 1893: 47. Borge, 1911: 200; Hardy, 1905: 68. Moebius, 1892: 444. West, 1909: 14. L 40-60 um; W 50-60 um; 1 40 um. Zygospore with simple spines, D 65 ym. Dumaresq Ck, U.N.E., Armidale (Skinner, Feb. 1974) ; Backwater [ Wzssman, Feb. 1974; Skinner, March, June (with spores), Dec. 1974]; Llangothlin Lagoon (Skinner, Sept. 1974); Deep Ck, near Baryulgil, swamp (Skznner, Nov. 1974) ; Cooney Ck, near Hillgrove (Skenner, Dec. 1974); Dangars Lagoon, Uralla (Skinner, Dec. 1974). Cosmarium rotundum Prescott and Scott, 1952: 64, pl. 3, fig. 6. Form similar to the type, but somewhat smaller. L 40-50 um; AW 25-30 um; T 15 um; 110 um. Fig. 1, 16. Proc. Linn. Soc. N.S.W., 104 (4), (1979) 1980 S. SKINNER 257 Baldersleigh, near Kingston, swamp (Wzssman, Sept. 1974). Cosmarium spirale (Playfair) Krieger and Gerloff 1962. Cosmarium stenonotum var. spirale Playfair, 1908: 618, pl. 13, fig. 20. The degree of spiral of the semi-cell and the disposition of the semi-cells to each other are very variable. L 60-65 um; W 25-30 wm; T 12-18 wm; 110-12 um. Fig. 2, 5a, b, c, d. Backwater, fen (Skznner, March, June, Dec. 1974) ; Bullock Ck, Point Lookout (Skinner, Dec. 1974). Cosmartum striolatum var. nordstedtz (Moebius) Krieger, 1932: 186, pl. 12, fig. 2. Gronblad and Croasdale, 1971: 17, fig. 112, 113. Pleurotaenzopsis tesselata (Delp.) De Toni var. nordstedtz Moebius 1892: 443, fig. 16. Bailey 1893: 45, fig. 40. Schmidle 1896: 305 [as Cosmarium (Pleurotaeniopsis) tessellata (Delp.) De Toni var. nordstedtzz]. L 90-110 um; W 50-70 um; T 240-50 um; I 30-35 um. Similar to C. lagerhetmianum (Turn.) Scott and Prescott (F1961), but spines not as pronounced. Fig. 2, 6. Backwater (Skznner, March, June, Dec. 1974) ; Bullock Ck, Point Lookout, bog (Skinner, Dec. 1974). Onychonema filiforme (Ehreb.) Roy and Bisset 1848. Playfair, 1915: 332, pl. 41, fig. 20 L 8-10 wm; 11-1.5 um. Backwater (Skznner, March 1974) ; Deep Ck, Baryulgil, swamp (Skznner, Nov. 1974). Playfair (1915) commented that there were low numbers of desmids in his Richmond River collections. He had records of 116 desmid taxa from lagoons and semipermanent pools in the Lismore area, and a further 56 taxa from the Richmond River, but he (1914, 1915) described very few of these, with comments on the presence of a few more. (His note on the conspecificity of Clostertum ehrenbergzt and C. moniliformis was all too brief) . Comparison of the desmid floras of the New England Tableland and Clarence River system with Playfair’s Richmond River district collections is rather difficult in the absence of complete records. There are only nine taxa recorded above which also appear in Playfair’s (1914, 1915) papers. To be fair to Playfair, some recent collections from the Clarence, e.g. the Mummulgum collection, did have a predominance of diatoms, euglenoids and bluegreen algae. The Baryulgil collection, by contrast, contained a wide variety of algae, including numerous desmid taxa. OEDOGONIOPHYCEAE OEDOGONIALES Oedogoniaceae : Bulbochaete elatior Pringsheim 1858. Tiffany, 1930: 32, pl. 1, fig. 1. Bailey, 1893: 16, pl. 4, fig. 7. Gauthier-Liévre, 1964: 237, pl. 25, fig. A. Gemeinhardt, 1939: 373, fig. 459. Moebius, 1892: 428, fig. 8. Cells medium-sized, L/B 4-6, W 14-18 um, gyandrosporous and nannandrous, androsporangia epigynous, one or two celled, dwarf males, stipe and one cell only, on supporting cell; oogonia closely fitting the oospores, supporting cell with a basal division, oospore depressed subquandrangular globose, 30-35 um in diameter, smooth walled. This form approaches fa. pumzla Hirn (Gauthier- Liévre 1964, 238, pl. 25, fig. C). Scott and Prescott (1958) show a form closer to Proc. Linn. Soc. N.S.W., 104 (4), (1979) 1980 258 ZY GNEMAPHYCEAE AND OEDOGONIOPHYCEAE 3 | 60m (on Fig. 2. 1, Cosmartum amplum, Baldersleigh, swamp; 2, C. glyptodermum, Baldersleigh, swamp; 3, C. lundelliz, Backwater, swamp; 4, C. magnificum, Backwater, swamp; 5a-d, C. sperale, Backwater, fen; 6, C. striolatum var. nordstedtz, Bullock Ck, Point Lookout; 7a-c, Bulbochaete gigantea, Bullock Ck, Point Lookout; 8a, b, B. elatéor, Bullock Ck, Point Lookout; 9, Oedogonium areschougzz, Backwater, swamp; 10, O. undulatum, Baldersleigh, swamp; lla-c, O. boscz?, Yellow Gap, swamp. Proc. Linn. Soc. N.S.W., 104 (4), (1979) 1980 S. SKINNER 959 var. scrobiculata Tiffany. Fig. 2, 8a, b. Bullock Ck, Point Lookout, bog (Skznner, Dec. 1974). Bulbochaete gigantea Pringsheim 1858. Tiffany, 1930. 38, pl. 5, figs 35, 36. Gauthier-Lievre, 1964: 248, pl. 239, fig. 44, c-g. Gemeinhardt, 1939: 386, fig. 475. Cells large, L/B 4-6, W 20-25 um; idioandrosporous and nannandrous, androsporangia on separate plants in this collection, 1-5 celled, terminal or subterminal on branch, 15x15 um; dwarf males epigynous, 3 celled; oogonium subglobular, terminal, L/B 0.8-1, W 45-50 um, supporting cell division median or slightly above, oospore filling oogonium reticulate scrobiculate. This form differs slightly from that described by Tiffany (1930). Fig. 2, 7a, b, c. Bullock Ck, Point Lookout, bog (Skznner, Dec. 1974). Oedogonium areschougiw Wittrock 1870. forma. Tiffany, 1930: 140, pl. 53, fig. 500. Gauthier-Liévre, 1964: 450, pl. 98, fig. 161, a-e. Gemeinhardt, 1939: 383, fig. Valle Cells small and narrow with a distinct basal capitulum, L/B 10-15, W 5-8 um; nannandrous (androsporangia not observed), dwarf males one celled, bean shaped epigynous; oogonium compressed globose, opening by a central suture, 18-22 um in diameter; oospore not quite filling the oogonium, brown, wall papillose, 16-20 zm in diameter. Fig. 2, 9. Backwater, hanging swamp (Skznner, March, June, Dec. 1974). Oedogonium bosci (Le Clerc) Wittrock 1874. Tiffany, 1930: 91, pl. 26, fig. 225-226. Gauthier-Liévre, 1964: 319, pl. 50, fig. 82, a-d. Gemeinhardt, 1939: 149, fig. este Cells moderately large, cylindrical L/B 3-10, W 15-18 um; only oogonia found in collection; pore superior, oogonium single (in groups separated by two or three vegetative cells), oblong ellipsoid, L/B 144-2, W 36-40 um, oospore ellipsoid striate, light brown, not filling oogonium longitudinally, L/B 1-14, W 35-38 um. Fig. 2, lla, b,c. Yellow Gap, Guyra-Mt. Mitchell Road, swamp (Skznner, June 1974). Oedogonium bourellyanum Villeret, 1951: 39, fig. 3. Gauthier-Liévre, 1964: 280. Cells moderately large, cylindrical, L/B 5-7, W 12-18 um; gynandrosporous, nannandrous, androsporangium up to 8-celled each cell 15-20 um long; dwarf males large, 55-60 um long, three-celled (stipe and two sporangial cells), on supporting cell of oogonium, numerous; oogonia one or two together inflated, constricted at the superior suture, cap projecting to upper vegetative cell, L/B 1- 14%, W 57-62 um, supporting cell elongate cup-shaped cospore the shape of the oogonium, but not quite filling it, 55-60 um wide. The form found in the Yellow Gap collection differs from the type being narrower in width of vegetative cells, the position of the oogonium, intercalary in this form, not terminal, and the oogonium shows an invagination at the suture. This taxon keys to O. mirandrium in Tiffany (1930), but is altogether larger and has multicellular dwarf males. Fig. 3, la, b,c. Oedogomum capilliforme Kutzing 1853. Tiffany, 1930: 81, pl. 19, fig. 172-173. Gauthier-Liévre, 1964: 307, pl. 44, fig. 72a, pl. 47, fig. 72, a-c. Gemeinhardt, 1939: 149, fig. 51. Proc. Linn. Soc. N.S.W., 104 (4), (1979) 1980 260 ZYGNEMAPHYCEAE AND OEDOGONIOPHYCEAE | Fig. 3. la-c, Oedogonium bourrellyanum, Yellow Gap, swamp; 2a,b, O. capilliforme, Cooney Ck; 3a- c, O. wissmaniz, Bullock Ck, Point Lookout, bog; 4a-d, O. wolleanum, Bullock Ck, Point Lookout, bog. Proc. Linn. Soc. N.S.W., 104 (4), (1979) 1980 S. SKINNER 261 Cells large, cylindrical, L/B 2-5, W 30-40um; androsporangia not observed with certainty, one or two celled among vegetative cells; oogonia inflated cylindrical, only slightly wider than vegetative cells L/B 1-14, W 40-48 um, opening by a superior pore; oospores spherical, golden brown, smooth walled, almost filling the oogonium, 40-45 ym wide. Fig. 3, 2a, b. Cooney Creek, near Hillgrove (Skznner, Dec. 1974). Oedogonium undulatum (Brébisson) A. Braun 1854. Tiffany, 1930: 118, pl. 42, fig. 407. Gauthier-Liévre, 1964: 466, pl. 103, fig. 171f. Gemeinhardt, 1939: 222, fig. 250. Moebius, 1892: 429, fig. 9a-c. A form similar to that described by Moebius in Bailey (1895), and described as var. moebzusi Schmidle (1896: 297, pl. 9, fig. 1) and accepted by Playfair (1917), with flattened undulations, cells moderately narrow, L/B 4-6, W 12- 15 um; attached oogonia few in collection, mostly broken. Fig. 2, 10. Baldersleigh, near Kingston, swamp (Wzssman, Sept. 1974). Oedogonium wolleanum Wittrock 1878. Tiffany, 1930: 135, pl. 50, fig. 479, Gauthier-Liévre, 1964: 353, pl. 64, fig. 104a-c. Gemeinhardt, 1939: 267, fig. 310. A very large species; cells moderately large, L/B 6-10, W 20-25 um; idioandrosporous, nannandrous; androsporangium 8-12 (16) celled; dwarf males numerous on a supporting cell, 4 celled (3 + stipe), 70-90 um long, W 15-20 pm in the stipe; oogonia solitary to three celled, with a terminal dome, suture superior, supporting cell elongate cupshaped, maximum width 60- 65 um, oospores filling the oogonium, striated, golden brown, 65-75 um wide. This form should also be compared with O. striatum Tiffany (1930) (O. wolleanum var. insigne Nordst.) in Gemeinhardt (1939). Fig. 3, 4a-d. . Bullock Creek, Point Lookout, bog (Skznner, Dec. 1974). Oedogonium wissmanii sp. nov. Diagnosis: Paries cellulae undulata 4 undis cellulae, L/B 3-6, 23-30 um late; idioandrosporous sine nannandroecio, androsporangium 4-7 cellulare duobus undis cellulae, L/B 1; oogonium globosum, sutura inframedia, 55-60 um oogonium globosum, sutura inframedia, 55-60 ym diametro; oospora globosa laevis, 48-53 um diametro. Iconotypus: Fig. 3, 3a, b, c. Cells moderately large, walls undulate, with 4 undulations per cell, L/B 3-6, W 23-50 um; idioandrosporous, androsporangium four- to seven-celled, with two undulations per cell, L/B 1; oogonium globose, with a terminal dome, suture wide and inframedian, 55-60 um wide, oospore globose, smooth walled, not filling the oogonium, 48-53 ym. Iconotype: Fig. 3, 3a, b, c. Bullock Creek, Point Lookout, bog (Skznner, Dec. 1974). Named for Hans Wissman, who collected many samples of freshwater algae for the author and suggested other sites for collecting. Differs from O. undulatum in size, lacking dwarf male plants, and in having undulate walls on the androsporangial cells. Type material stored at National Herbarium, Royal Botanical Gardens, Sydney. Some records of the occurrence of Oedogoniophyceae, seven taxa in Oedogonium and two taxa in Bulbochaete, in New South Wales appear in Playfair (1917) but without localities. This class is not well documented for Proc. Linn. Soc. N.S.W., 104 (4), (1979) 1980 262 ZY GNEMAPHYCEAE AND OEDOGONIOPHYCEAE Australia, but two taxa from the present collections are also recorded from Queensland by Moebius (1892). SUMMARY The desmid flora of north-eastern New South Wales, as presently known, has many species in common with both the Indo-Malay-northern Australia and temperate Australia-New Zealand floras of Kneger (1932). Gronbladia neglecta, Desmidium suboccidentale, Phymatodocis nordstedttana, Euastrum longicolle formae, Cosmarium askenaskiyt and C. denticulatum are species common to the Indo- Malayan flora and this region. Most other taxa are common throughout the world. Many species, e.g. Staurastrum sexangulare, which reaches its greatest diversity of form in Indonesia (Scott and Prescott, 1961), are found throughout Australia and New Zealand. Much further research is needed before the interrelations between these tropical and temperate floras are clearly documented. The flora of the north-eastern New South Wales may prove to be part of the interface between the two floras as the climate and ecological variables are present in this region. ACKNOWLEDGEMENTS The collections from which this paper was drawn were made as part of the work for a Master of Science Degree. The author wishes to acknowledge the encouragement of members of the Department of Botany at the University of New England, especially Professor N. C. W. Beadle and Dr R. A. de Fossard. Mr I. Garrard and particularly Mr H. Wissman did invaluable collecting. Thanks are also due to Professor H. B. S. Womersley, Department of Botany, University of Adelaide for reading the manuscript and subsequent suggestions. References BaILey, F. M., 1893. — Contributions to the Queensland Flora. Botany Bull. (Qld Dept. Agric.), No. VI.: 1-58, pls 1-19. ——,, 1895. — Contributions to the Queensland Flora. Botany Bull. (Qld Dept. 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Rabenhorst Kryptogamen-Flora von Deutschland und der Schwezz, 12 (4). Leipzig: Akademische Verlagsgesellschaft. Gr®@NBLAD, R., and CrRoaspALE, H., 1971. — Desmids from Namibia (S.W. Africa). Acta Bot. Fenn. 93, 40 p. ——., Prowse, G. A., and Scott, A. M., 1958. — Sudanese desmids. Acta Bot. Fenn. 58, 82 p. Harpy, A. D., 1904. — The freshwater Algae of Victoria. Vic. Nat. 21: 81-87. ——, 1905. — The freshwater Algae of Victoria. II. Vic. Nat. 22: 31-35, 62-73. —— , 1906. — The freshwater Algae of Victoria. III. Vic. Nat. 23: 18-22, 33-42. ——, 1913. — Some Algae of the Zoological Gardens, Melbourne, Vic. Nat. 30: 89-95. KoLkwitz, R., and Krigcer, H., 1941. — Zygnemales. Vol. 13, Part 2. In L. RABENHORST Kryptogamen- Flora von Deutschland und der Schweiz. Leipzig: Akademische Verlagsgesellschaft. Proc. LINN. Soc. N.S.W., 104 (4), (1979) 1980 S. SKINNER 263 KRIEGER, W., 1932. — Die Desmidiaceen der Deutschen Limnologischen Sunda-expedition. Archiv. fur Hydrobiol. 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Supplement I Freshwater Algae, pp. 219-263 In Matpen, J. H. and Betcue, E., A Census of New South Wales Plants. Sydney: Government Printer. Prescott, G. W., 1940. — Desmids of Isle Royale, Michigan. The genera Stauwrastrum, Micrasterzas, Xanthidium, and Euastrum, with a note on Spinoclostertum. Pap. Mich. Acad. Sct. Arts Lett. 25: 89-100 with 4 plates. , and Scotr, A. M., 1952. — Some South Australian desmids. Trans. R. Soc. S. Aust. 75: 55-69. *RaciBORSKI, M., 1892. — Desmidyja zebrane przez Dr. E. Ciastonia w podrozy na okolo ziemi. Rozpr. Aka. Umiej Wydxial. Mat. — przyr. Krakow, Ser. 2, 2: 361-393, pl. 1, 2. RANDHAWA, M., 1959. — Zygnemaceae. New Delhi: I.C.A.R. RicH, R., 1932. — Contributions to our knowledge of the freshwater algae of Africa. 10. Phytoplankton from South African pans and vleis. Trans. R. Soc. S. Africa 20: 149-188. Rounp, F. E., 1971. — The taxonomy of the Chlorophyta. II. Br. phycol. J., 6 (2) : 235-264. RUZICKA, J., 1977. — Die Desmidiaceen Mitteleuropas. 1. Stuttgart. SCHMIDLE, W., 1896. — Siisswasseralgen aus Australien. Flora 82: 297-313. Scott, A. M., and Prescott, G. W., 1958. — Some freshwater algae from Arnhem Land in the Northern Territory of Australia. Pp. 9-136 In SpEcHT, R. L., and Mountrorp, C. P., Records of the American-Australian Expedition to Arnhem Land. 3. Botany and Plant Ecology. Melbourne: Melbourne University Press. , and , 1961. — Indonesian desmids. Hydrobiol. 17: 1-182. Tuomasson, K., 1973. — Notes on the plankton of some Sydney reservoirs, with descriptions of two interesting desmids. Contrib. N.S.W. Nat. Herb. 4 (6) : 384-394. , and Tyrer, P. A., 1971. — Taxonomy of Australian freshwater Algae. 2. Some planktic Staurastra from Tasmania. Nova Hedw. 2] (1) : 287-319. TirFany, L. H., 1930. — The Oedogonzaceae. Columbus, Ohio. 188p + 64 plates. TyLer, P. A., 1970. — Taxonomy of Australian fresh-water Algae. I. The genus Micrasterzas in south- eastern Australia. Br. phycol. J. 5 (2) :; 211-234. VILLERET, S., 1951. — Quelques especes d’Algues d’eau douce nouvelles. Bull. Soc. Bot. France 98 : 37-40. West, G.S., 1905. — Desmids from Victoria. J. Bot. 63 : 252-254. ——, 1909. — Algae of the Yan Yean Reservoir, Victoria: A biological and oceanological Study. J. Lznn. Soc. Lond. (Bot.) 39: 1-88. *Not seen by author. Proc. Linn. Soc. N.S.W., 104 (4), (1979) 1980 S Teese tbe “iy eee AD Magee Racha S PAG hea Lae AS i hat Darwin and Diprotodon: The Wellington Caves Fossils and the Law of Succession KATHLEEN G. DUGAN (Communicated by T. G. VALLANCE) Ducan, K. G. Darwin and Diprotodon: the Wellington Caves fossils and the law of succession. Proc. Linn. Soc. N.S.W. 104 (4), (1979) 1980: 265-272. Fossil evidence from the Wellington Caves of New South Wales contributed to the overthrow of the theory of special creation and promoted the development of Darwinian theory. The law of succession, which notes the close affinities between recently extinct and living species, was first established on the basis of the Wellington Caves fossils. This law provided a powerful argument in favour of evolution and first attracted Darwin’s attention to the problem of the origin of species. Kathleen G. Dugan, Department of History, University of Papua New Guinea, Box 4820 University P.O., Papua New Guinea; manuscript received 22 August 1979, accepted in revised form 21 May 1980. INTRODUCTION In the early decades of the nineteenth century Australia was sparsely settled and its colonists had little time to devote to scientific investigation. Palaeontological discoveries were rare and the colonists themselves lacked the scientific expertise necessary to interpret their significance. But the Australian fossil evidence provided European biologists with the key to a fundamental law of distribution and contributed to the development of a new theoretical framework, Darwinian evolution. The exploration of the Wellington Caves of New South Wales in 1830 led to the first major discovery of mammalian fossils in Australia. The caves aroused a great deal of interest and speculation in Europe because they provided the first evidence of past geographic distribution of mammals in Australia, a continent known for its biological peculiarities. The Wellington fossils challenged some of the treasured assumptions of the Scriptural geologists, particularly belief in the universal Deluge, and thus raised uncomfortable doubts regarding the literal truth of the Bible. More significantly, the fact that the recently extinct Australian mammals were marsupials and thus clearly related to the living mammals of Australia led to the formulation of the ‘law of the succession of types’, a generalization of fundamental importance in the development of evolutionary theory. Colonist George Ranken first discovered the fossil remains of the Wellington Caves (Lane and Richards, 1963) and brought them to the attention of the Surveyor- General of New South Wales, Thomas Livingstone Mitchell, who conducted further explorations. Mitchell was particularly interested in cave fossils because he wished to show that the diluvial geology of William Buckland applied in Australia as well as in Europe (Foster, 1936). In Reliquiae Diluvianae (1824) Buckland had argued that the recent fossilized remains of large extinct mammals in European caves revealed the action of a universal deluge. These inhabitants of the antediluvian world were, he claimed, destroyed by a world-wide flood. Buckland’s views, supportive of the literal truth of Genes7s, were widely adopted in Australia where conservative religious beliefs predominated in scientific circles. Proc. Linn. Soc. N.S.W., 104 (4), (1979) 1980 266 DARWIN AND DIPROTODON Colonist John Dunmore Lang first announced the Wellington discovery (Lang, 1830) , interpreting the fossils in the context of traditional Christian belief as proof of the literal truth of Scripture and evidence of the wisdom and foresight of the Creator. Lang, a Presbyterian clergyman with an amateur interest in geology, was eager to show that the facts of science were not in conflict with the Mosaic account of creation and the Deluge (Lang, 1846, 1951). He noted that many of the cave animals were extinct or at least were no longer to be found in New South Wales. Lang adopted Buckland’s theory, attributing their extinction to natural catastrophe, a catastrophe which did not materially change the external appearance of the country, i.e., a flood. He concluded : While this very interesting discovery supplies us, therefore, with another convincing proof of the reality and universality of the deluge, it supplies us also with a powerful motive of gratitude to Divine providence for that long-forgotten visitation. For if this territory were over-run with such beasts of prey as the antediluvian inhabitants of the cave at Wellington Valley, it would not have been so eligible a place for the residence of man as it actually is. The tiger or hyaena would have been a much more formidable enemy of the Bathurst settler than the despicable native dog, though indeed they would certainly have afforded a much nobler game to the gentlemeu [sic] of the Bathurst Hunt. And if the huge rhinoceros had inhabited the lagoons of Hunter’s River, it might have been a much more serious work to displace him than to shoot the pelican or emu. [ Lang, 1830] Just as Lang and other colonists sought to explain the huge fossils in a manner consistent with their Christian beliefs, so the Aborigines explained them within their own frame of reference. The Aborigines of Eastern Australia were very fearful of the bunyip, a legendary aquatic monster inhabiting deep waterholes and roaming the billabongs at night. Confronted with the fossil remains of gigantic animals, Aborigines often identified these as the remains of the bunyip (Barrett, 1946). As one colonist observed : It may not be amiss to state that all the Natives throughout these Northern Districts have a tradition relative to a very large animal having at one time existed in the large Creeks & Rivers & by many it is said that such animals now exist & several of the Fossil bones which I have at various times shown to them they have ascribed to them. Whether such animals as those to which they refer be yet living is a matter of doubt, but their fear of them is certainly not the less & their dread of bathing in the very large waterholes is well known — [Isaac, 1845] J. W. Gregory, Professor of Geology at the University of Melbourne (later at the University of Glasgow) , suggested that Aboriginal legends of gigantic monsters might be based upon a knowledge of the living Diprotodon (Gregory, 1906, p. 7). Lang’s theory was published in Europe (Lang, 1831) but European biologists were quick to offer an alternative explanation. Examples of the Wellington Caves fossils were sent to Robert Jameson, Professor of Natural History at Edinburgh University, for identification by European experts. Jameson forwarded them to William Clift, Conservator of the Hunterian Museum, who identified the remains of dasyurids, wombats, and kangaroos (Clift, 1831). All the bones belonged to marsupials of the Australian type with one apparent exception. Lang had suggested that a large thigh bone found in the caves belonged to an Irish elk, rhino, or elephant (Lang, 1830). Clift compared it to the thigh of an ox or hippo (Clift, 1831), and William Pentland claimed that it represented the remains of an elephant (Pentland, 1831). From these data, Jameson observed that Australia, like Europe, was formerly populated with gigantic animals which have since become extinct. Moreover, he argued that the cause of extinction was the same in Europe and Australia, but he did not identify this cause as the Biblical flood. Most significantly, he concluded “‘[t]hat New Holland was, at a former period, distinguished from the other parts of the world, by the same peculiarities in the organization of its animals, which so strikingly characterize it at the present day” (Jameson, 1831). Proc. LINN. Soc. N.S.W., 104 (4), (1979) 1980 K. G. DUGAN 267 This conclusion challenged catastrophist theories. Georges Cuvier, of the Muséum d'Histoire Naturelle in Paris, had developed methods of comparative anatomy which had enabled palaeontologists to reconstruct the skeletons of animals from the fragmentary remains preserved in the fossil record. A vast array of fantastic creatures, now extinct, had been revealed for the first time to an astonished public. Cuvier believed that past geological changes had been sudden and violent, thus causing the extinction of whole populations of plants and animals. These had been replaced by new, unrelated species, either by migration or (as many of Cuvier’s followers, including Buckland, believed) by a succession of miraculous, divine creations. Catastrophist theory necessarily ruled out evolution because rapid, violent changes did not allow the necessary continuity of generations and because a comparatively limited age of the earth did not allow adequate time for gradual evolutionary change. Cuvier was recognized as the foremost naturalist of his day, and the full weight of his formidable reputation was solidly opposed to evolution (Coleman, 1964). The full significance of the Wellington Caves discoveries was not recognized until after Cuvier’s death in 1832. The fossils raised uncomfortable doubts about catastrophism and special creation. If all the plants and animals of the Tertiary were destroyed by a universal deluge and subsequently replaced by a specially created, entirely new set of plants and animals, why should there be any continuity between existing species and recently extinct species? In fact, from the principle of adaptation of organisms to their environment one would expect that organic changes would accompany drastic changes in the physical environment. The discontinuities of fossil distribution provided Buckland with the major evidence in support of his theory. European caves contained the fossil remains of tropical species like hyaenas and elephants which no longer survived in Europe. Buckland concluded that these animals had been destroyed by a world-wide flood and expected to find evidence of similar discontinuous distribution on other continents. The Wellington fossils, however, suggested quite the opposite conclusion. Some of the species found in the caves were still living in Australia, and most European scientists were struck with the similarities between the extinct and living species rather than with the differences. Pentland, for example, observed: with a single exception, all the genera to which these fossils are referable, are now found inhabiting the Australasian Continent, a remarkable coincidence with the fossil animals of the same geological epoch in Europe, where, with few exceptions, the animals which have been found in what have been called Diluvial Deposits, belong to genera still inhabiting our countries. [ Pentland, 1832 ] This fact was taken to cast doubt on Buckland’s diluvialist theories. In 1833 Mitchell wrote to George Ranken concerning the significance of their discovery at Wellington: I understand Buckland’s nose is put completely out of joint by the bones from Australia, their not being those of lions and hyenas is, I find, a fact which is considered in England to entirely upset his theory. And I have now heard from the best authority that the fact of their fossil bones belonging to animals similar to those now existing has worked a great change in all their learned speculating on such subjects at home. [Ranken, 1916, p. 29] The discovery that the peculiarities of the living Australian flora and fauna were reflected in the fossil species as well suggested that the laws of geographic distribution which currently confine particular groups of animals within particular geographic regions applied in the recent geologic past as well. The Wellington discoveries, coupled with Darwin’s observations in South America, led him to formulate the law of the succession of types. This law provided important evidence in favour of evolution and, indeed, turned Darwin’s attention towards the problem of the origin of species (De Beer, 1968, pp. 79-80; Eiseley, 1961, pp. 161-166; Himmelfarb, 1962, pp. 108-113). Proc. Linn. Soc. N.S.W., 104 (4), (1979) 1980 268 DARWIN AND DIPROTODON Darwin is credited with developing the law in 1837 as a result of his fossil discoveries in South America. Finding the remains of giant mammals related to sloths, llamas and armadilloes, he noted that these extinct mammals are now represented by smaller animals, also confined to South America, which display the same peculiarities of anatomy as their larger predecessors (C. Darwin, 1838). Subsequently, Darwin (1839, pp. 209-210) wrote: The most important result of this discovery, is the confirmation of the law that existing animals have a close relationship in form with extinct species . . . The law of the succession of types, although subject to some remarkable exceptions, must possess the highest interest to every philosophical naturalist, and was first clearly observed in regard to Australia, where fossil remains of a large and extinct species of Kangaroo and other marsupial animals were discovered buried in a cave. In America the most marked change among the mammalia has been the loss of several species of Mastodon, of an elephant, and of the horse ... If Buffon had known of these gigantic armadilloes, llamas, great rodents, and lost pachydermata, he would have said with a greater semblance of truth, that the creative force in America had lost its vigour, rather than that it had never possessed such powers. Contemplating the Wellington fossils, Thomas Mitchell offered a similar suggestion with regard to the waning power of Australian nature: It is consolatory here to find that Australia did once support herbivorous animals of such magnitude — and that an animal so well provided for a country of burning woods and fallen timber — by its young = [sic] protecting pouch and saltatory powers has always belonged to Australia — although the curious gradation of species — and the diminutive character of existing classes seem to indicate the energies of animal nature here to be on the wane — unless indeed this is a wise provision of providence for the introduction of those other large animals by man’s agency — which have been found better suited to his wants. [ Mitchell, 1843] The influence of the Australian fossils on the development of the law of the succession of types has not been generally emphasized. Historians have tended to stress instead the importance of Darwin’s own South American experiences. Darwin himself, as he tried to reconstruct the development of his ideas in retrospect, recalled the importance of the South American observations. He wrote in his Journal : In July [1837] opened first note book on “Transmutation of Species” — Had been greatly struck from about Month of previous March on character of S. American fossils — & species on Galapagos Archipelago. These facts origin (especially latter) of all my views. [C. Darwin, 1959, p. 7] However, as historian Camille Limoges points out, it is doubtful if Darwin could have developed a comprehensive generalization on the basis of a single South American example (Limoges, 1970, pp. 17-18). The significance of the discovery is unclear until one recognizes that it is true for other parts of the world as well. In fact, Darwin himself cited Clift’s work on the Wellington fossils as evidence for the law of succession (C. Darwin, 1859, p. 339). Clift’s work was also cited favourably in Lyell’s Principles of Geology (Lyell, 1833, p. 144), which Darwin had studied while on the Beagle. In 1831 E. W. Brayley suggested the possibility of such a correlation in distribution (Brayley, 1831), but the Wellington Caves provided the first and most dramatic evidence for the law. In 1844 Richard Owen developed a similar law, again based on the Wellington find. Owen, Britain’s leading comparative anatomist and palaeontologist, was intensely interested in Australian natural history and developed an extensive correspondence with observers in Australia (Moyal, 1976). Owen classified the vertebrate fossils Darwin had collected on the voyage of the Beagle (C. Darwin, 1840) and provided a description of the Wellington fossils for Mitchell’s Three Expeditzons into the intertor of Eastern Australia (Mitchell, 1838). Owen cited the Australian fossils as evidence that, with extinct as with existing Mammalia, particular forms were assigned to particular provinces, and, what is still more interesting and suggestive, that the same forms were restricted to the same provinces at a former geological period as they are at the present day. [| Owen, 1845] Proc. Linn. Soc. N.S.W., 104 (4), (1979) 1980 K. G. DUGAN 269 This generalization was frequently repeated in Owen’s publications and, together with his work on Darwin’s ‘Beagle’ fossils, formed the basis of his claim to priority in formulating the law of succession. Although Darwin readily acknowledged that Owen had extended the law to apply to the Old World, Owen’s attempt to claim credit for the law irritated him. Ina letter to Lyell in 1859, he complained: Why I gave [in the Orzgzn] in some detail references to my own work is that Owen (not the first occasion with respect to myself and others) quietly ignores my having ever generalised on the subject, and makes a great fuss on more than one occasion at having discovered the law of succession . . . Long before Owen published I had in MS. worked out the succession of types in the Old World . . . [F. Darwin and Seward, 1903, 1, p. 133] As further research provided additional evidence for the law of succession, it became an accepted rule of geographic distribution. The close relationship between existing species and recently extinct species strongly suggested an evolutionary connection. Such a connection was, of course, denied by the anti-evolutionists, but they could offer no satisfactory alternative explanation. Although the discovery at Wellington Caves led to the formulation of the law of succession, it also offered a major exception to it, the alleged Australian elephant. Naturalists wished to show a close affinity between existing species and recently extinct species. Reports of a large Australian placental violated this rule. Thomas Mitchell had already questioned the identification. He wrote to Ranken in 1831, “They find most of them [the Wellington Caves fossils] to be wombats and kangaroos, but Cuvier calls your large bone an elephant’s. The London surgeons, however, seemed puzzled about it, and I have doubts. . .’ (Ranken, 1916, p. 25). In 1838 Owen resolved the problem by identifying the large Wellington fossil as a new species, Diprotodon optatum, a giant, wombat-like marsupial (Mitchell, 1838, 1, p. xix; 2, pp. 362-363). But this was not the end of claims that proboscideans once roamed the Australian bush. In 1843 Owen identified a fossil from the Darling Downs as a Dinothertum, an extinct placental pachyderm (Owen, 1843a, 1843b). The following year he corrected this error, noting that some of these bones, too, belonged to Diprotodon. At the same time, however, he identified a fossil tooth, ostensibly from Australia, as that of a Mastodon (Owen, 1844). This tooth, which the Polish explorer Strzelecki claimed to have acquired from an Australian Aborigine, served as the basis for later accounts of mastodons in Australia. These false identifications and conflicting reports caused a great deal of confusion. Explorer Ludwig Leichhardt (1855) questioned whether there was sufficient evidence to prove this dramatic exception to a well-established rule of geographic distribution. Nevertheless, in Europe, as in Australia, the former existence of an Australian placental pachyderm was generally accepted. For evolutionists, it was important to get the mastodon out of Australia. Darwinists wished to explain the unique character of the Australian fauna as a result of isolation and natural selection. They claimed that Australia had at an early geological period become separated from the rest of the world by vast oceans. Marsupials, isolated from competition with placentals, evolved to fill a variety of ecological niches. One might account for the presence of placental rodents by Darwin’s mechanisms of chance dispersal but these were hardly sufficient to account for the migration of the huge mastodons. The Australian mastodon remained an anomaly until 1863 when the British palaeontologist Hugh Falconer challenged its existence. Falconer agreed that Strzelecki’s tooth belonged to a mastodon, but noted that it appeared to belong to a South American species. Since claims for the existence of mastodons in Australia rested solely on this isolated example, Falconer concluded there must be an error respecting the origin of the fossil (Falconer, 1863). Owen quietly abandoned his Proc. LINN. Soc. N.S.W., 104 (4), (1979) 1980 270 DARWIN AND DIPROTODON claim. Darwin rejoiced in the overthrow of the mastodon, writing to Falconer in November, 1862, ‘I never did or could believe in him’ (F. Darwin and Seward, 1903, I, p. 211). In 1882, Owen made one final attempt to revive the Australian proboscidean (Owen, 1882), but he was unsuccessful. The law of succession, once firmly established, provided a powerful argument in favour of evolution. If one adopts the theory that new species develop from preexisting ones by a process of descent with modification, then it is absolutely necessary that there be a continuity between existing species and recently extinct species. Moreover, the opposing theories of the anti-evolutionists failed to explain this continuity. The special creationists emphasized the perfect adaptation of animals to their environment, and they attributed this adaptation to God’s benevolent design. Yet, as Darwin pointed out, such theories were insufficient to account for the South American and Australian observations. He noted that the animals of Australia are very different from those of South America, even though parts of each continent share a similar climate. Therefore, one could not account for the dissimilarities between South American and Australian animals solely on the basis of adaptation to different environments. At the same time, one could not explain the similarities between living and recently extinct animals on the same continent solely as a result of adaptation to similar environments, because geological change should presumably be accompanied by organic change. Darwin claimed that only a theory of evolution could adequately explain these facts: On the theory of descent with modification, the great law of the long enduring, but not immutable, succession of the same types within the same areas, is at once explained; for the inhabitants of each quarter of the world will obviously tend to leave in that quarter, during the next succeeding period of time, closely allied though in some degree modified descendants. If the inhabitants of one continent formerly differed greatly from those of another continent, so will their modified descendants still differ in nearly the same manner and degree. [C. Darwin, 1859, p. 340) The law of succession not only provided important evidence in support of evolution, it also played a role in convincing Darwin of the validity of evolution. He wrote to Lyell in 1859, ‘In fact, this law, with the Galapagos distribution, first turned my mind on the origin of species’ (F. Darwin and Seward, 1903, I, p. 133). ACKNOWLEDGEMENTS I am indebted to Mr T. Darragh, Dr L. Farrall, Mr A. McEvey, Dr D. Ospovat, Dr P. Rich and Dr T. Rich for their valuable comments on the manuscript. I gratefully acknowledge the invaluable assistance provided by Ms Karen Borell and the guidance provided by my dissertation supervisor, Dr Jerry Stannard. The Owen Correspondence is quoted with the permission of the Trustees of the British Museum (Natural History). This work was undertaken as part of my research as the National Museum of Victoria’s Research Scholar in Science and Humanities, and was supported by grants from the Myer Foundation and the Ian Potter Foundation. References BARRETT, C., 1946. — The bunytp and other mythical monsters and legends. Melbourne: Reed & Harris. BrayLey, E. W., 1831. — On the odour exhaled from certain organic remains in the Diluvium of the Arctic Circle, as confirmatory of Dr Buckland’s opinion of a sudden change of climate at the period of destruction of the animals to which they belonged; and on the probability that one of the fossil bones, brought from Eschscholtz Bay, by Captain Beechey, belonged to a species of Megatherium. Phil. Mag. 9: 411-418. Proc. LINN. Soc. N.S.W., 104 (4), (1979) 1980 K. G. DUGAN 271 BUCKLAND, W., 1824. — Reliquzae diluvianae ; or, observations on the organic remains contained in caves, fissures, and diluvial gravel, and on other geological phenomena, attesting the action of an universal deluge. 2nd ed. London: John Murray. Curr, W., 1831. — Report by Mr Clift, of the College of Surgeons, London, in regard to the fossil bones found in the caves and bone-breccia of New Holland. Edinb. New Phil. J. 10: 394-395. CoLeMAN, W., 1964. — Georges Cuvier zoologist; a study in the history of evolution theory. Cambridge, Mass. : Harvard University Press. Darwin, C., 1838. — A sketch of the deposits containing extinct Mammalia in the neighbourhood of the Plata. Proc. Geol. Soc. Lond. 2: 542-544. ——, 1839. — Journal of researches into the geology and natural history of the various countries visited by H.M.S. Beagle, under the command of Captain FitzRoy, R.N., from 1832 to 1836. London: Henry Colburn. ——, 1840. — The zoology of the voyage of H.M.S. Beagle, under the command of Captain FitzRoy, R.N., during the years 1832 to 1836. Part 1. Fossil Mammalia; by Richard Owen. London: Smith, Elder and Co. ——, 1859. — On the origin of species by means of natural selection, or, the preservation of favoured races in the struggle for life. London: John Murray. ——, 1959. — Darwin’s Journal. Gavin de Beer (ed.). Bull. Br. Mus. nat. Hist. (F. Historical) 2: 3-21. Darwin, F., and Sewarp, A. C., (eds), 1903. — More letters of Charles Darwin; a record of his work ina series of hitherto unpublished letters. 2 vols. London: John Murray. Dre Beer, G., 1968. — Charles Darwin: evolution by natural selection. Melbourne: Thomas Nelson (Australia) Limited. EIsELEY, L., 1961. — Darwin’s century; evolution and the men who discovered it. Garden City, New York: Doubleday & Company, Inc. FALconer, H., 1863. — On the American fossil elephant of the regions bordering the Gulf of Mexico (E. Columbi, Falc.) ; with general observations on the living and extinct species. Nat. Hist. Review 10: 43-114. Foster, W., 1936. — Colonel Sir Thomas Mitchell, D.C.L., and fossil mammalian research. Roy. Aust. Hist. Soc. J. 22: 433-443. Grecory, J. W., 1906. — The dead heart of Australia; a journey around Lake Eyre in the summer of 1901- 1902, with some account of the Lake Eyre basin and the flowing wells of central Australia. London: John Murray. HIMMELFARB, G., 1962. — Darwin and the Darwinian revolution. New York: W. W. Norton & Company Inc. Isaac, F. N., 1845. — An account of some fossil bones found in Darling Downs [ Unpublished Ms. ]. British Museum (Natural History) Owen Correspondence, vol. 16, folios 26-27. JAMESON, R., 1831. — On the fossil bones found in the bone-caves and bone-breccia of New Holland. Edinb. New Phil. J. 10: 393-396. Lane, E. A., and RicHarps, A. M., 1963. — The discovery, exploration and scientific investigation of the Wellington Caves, New South Wales. Helictzte 2: 1-53. [Lanc, J. D.], 1830. — Letter to the editor. Sydney Gazette, 25 May 1830, 3. ——, 1831. — Account of the discovery of bone caves in Wellington Valley, about 210 miles west from Sydney in New Holland. Edinb. New Phil. J. 10: 364-368. [ The letter to the Sydney Gazette, cited above, is here republished as an article. | ——, 1846. — The Mosaic account of the creation compared with the deductions of modern geology: a lecture, delivered in the hall of the Mechanics’ Institution, Melbourne, Port Phillip, 9th February, 1846. ——, 1951. — John Dunmore Lang: chiefly autobiographical 1799 to 1878. Archibald Gilchrist, ed. 2 vols. Melbourne: Jedgram Publications. LEICHHARDT, L., 1855. — Beitrage zur Geologie von Australien. Halle: H. W. Schmidt. Limoces, C., 1970. — La sélection naturelle ; étude sur la premiere constitution d’un concept (1837-1859). Paris: Presses Universitaires de France. LyELL, C., 1833. — Principles of geology, being an attempt to explain the former changes of the earth's surface by reference to causes now in operation. Vol. 3. London: J. Murray. MITCHELL, T. L., 1838. — Three expeditions into the interior of eastern Australia, with descriptions of the recently explored region of Australia Felix, and of the present colony of New South Wales. 2 vols. London: T. & W. Boone. ——, 1843. — Letter to Richard Owen, 28 January 1843. British Museum (Natural History) Owen Correspondence, vol. 19, folios 242-247. Moyat, A. M., 1976. — Sir Richard Owen and his influence on Australian zoological and palaeontological science. Rec. Aust. Acad. Sci. 3: 41-56. Owen, R., 1843a. — On the discovery of the remains of a mastodontoid pachyderm in Australia. Ann. Mag. nat. Hist. 11: 7-12. Proc. Linn. Soc. N.S.W., 104 (4), (1979) 1980 272 DARWIN AND DIPROTODON ——, 1843b. Additional evidence proving the Australian pachyderm described in a former number of the ‘Annals’ to be a Dinothertum, with remarks on the nature and affinities of that genus. Ann. Mag. nat Hast. 11: 329-333. ——, 1844. — Description of a fossil molar tooth of a Mastodon discovered by Count Strzelecki in Australia. Ann. Mag. nat. Hist. 14: 268-271. ——, 1845. — Report on the extinct mammals of Australia, with descriptions of certain fossils indicative of the former existence in that continent of large marsupial representatives of the Order Pachydermata. 14th Rep. Brit. Ass. Adv. Sct. : 223-240. —— , 1882. — Description of portions of a tusk of a proboscidean mammal (Notelephas australis, Owen). Phil. Trans. R. Soc. 173: 777-781. PENTLAND, W. [sic = J.B.*], 1831. — Jn Further notices in regard to the fossil bones found in Wellington Country, New South Wales. By Major Mitchell, Surveyor-General of New South Wales. Edinb. New Phil. J. 11: 179-180. [This article is attributed to Mitchell but it is actually an editorial note in which all new material is directly quoted from Pentland. | ——, 1832. — On the fossil bones of Wellington Valley, New Holland, or New South Wales. Edinb. New Phil. J. 12: 301-308. RANKEN, C.G., 1916. — The Rankens of Bathurst. Sydney: S. D. Townsend. *The ascription to William Pentland is almost certainly an error given currency by Robert Jameson, editor of the Edinburgh New Philosophical Journal. W. A. S. Sarjeant and J. B. Delair (Bull. Brit. Mus. (Nat. Hist.) , hist. series, 6(7), 1980, p. 319) assign the work to Joseph Barclay Pentland [1797-1873]. Note added by T. G. Vallance. Proc. Linn. Soc. N.S.W., 104 (4), (1979) 1980 Rock Units, Structure and Metamorphism of the Port Macquarie Block, eastern New England Fold Belt EVAN C. LEITCH Leitcu, E. C. Rock units, structure and metamorphism of the Port Macquarie Block, eastern New England Fold Belt. Proc. Linn. Soc. N.S.W. 104 (4), (1979) 1980: 273-292. The presence of syn- and late-orogenic rocks, relationships between recrystallization and imposed structures, and contrasts between units separated by large faults, has allowed reconstruction of a detailed structural and metamorphic history of the Port Macquarie Block. Three units of stratified rocks are recognized: the Watonga Formation mainly composed of chert and slate of pre-Devonian age, the Middle Palaeozoic Touchwood Formation consisting of volcanogenic clastic sedimentary rocks and andesite, and the Thrumster Slate comprising slate and meta-sandstone of Early Permian (?) age. These units have been intruded by dolerite dykes collectively grouped in the Karikeree Metadolerite, by serpentinite bodies, and by felsic dykes, and are unconformably overlain by Early Triassic conglomerate of the Camden Haven Group. _ The Watonga Formation and Thrumster Slate together with early members of the Karikeree Metadolerite were cleaved and recrystallized under greenschist facies conditions at an early stage during Late Permian orogenesis. Later dolerite bodies emplaced in the cleaved rocks are massive but also show greenschist facies mineral assemblages. Touchwood Formation rocks and associated Karikeree Metadolerite dykes lack cleavage and suffered only burial metamorphism, under prehnite- pumpellyite metagreywacke facies conditions. They were brought into contact with the more intensely deformed rocks by transcurrent movements along a system of northnorthwest-trending faults that slice the block. Subsequently serpentinite masses rose along some of these fractures as well as along a somewhat younger northwest striking fault. Isolated glaucophane schist blocks in soil at one locality have probably weathered out of a serpentinite lens. A small thermal high in which static recrystallization produced biotite post-dates most deformation and may be associated with a buried intrusive body. Here the serpentinite contains antigorite, in contrast with the chrysotile-lizardite serpentinites elsewhere in the block, and is associated with lenses of talc and chlorite-tremolite rocks. Fault movements continued into post-Early Triassic times, juxtaposing Camden Haven rocks and both serpentinite and earlier Palaeozoic rocks. E. C. Leitch, Department of Geology and Geophysics, University of Sydney, Australia 2006; manuscript received 22 February 1980, accepted in revised form 18 June 1980. INTRODUCTION The meridional trend of major tectonic units that characterizes most of the Tasman Orogenic Zone cannot be recognized in the eastern part of the New England Fold Belt. Instead, stratified rocks of diverse facies, structural history, and metamorphic character, are juxtaposed across a complex series of faults that divide the region into irregular blocks, of which the 150 km? Port Macquarie Block is the smallest (Fig. 1; Leitch, 1974). The only accessible contact of this block with other Palaeozoic rocks is on its west, where it abuts Carboniferous and Early Permian sedimentary rocks of the Hastings Block along the Cowarra Fault. To the south the block is faulted against Early Triassic strata of the Lorne Basin, and to the north it disappears beneath Quaternary sediment. The eastern edge of the block lies beyond the coastline except perhaps north of Tacking Point where coastline and a northwest- bounding fault may coincide. Proc. LINN. Soc. N.S.W., 104 (4), (1979) 1980 274 PORT MACQUARIE BLOCK No systematic account of the nature of the block has been published previously, although Voisey (1939) described some of the constituent rocks. Carne (1896), Quodling (1964) and Barron, Scheibner and Slansky (1976) have provided data concerning serpentinite and associated rocks that occur along the coast north of Tacking Point, and in view of these reports, and forthcoming accounts by Samuels (in prep.) and Leitch (zn press) the geology of this complex zone is not treated here. Recent investigations by the author confirm the distinctive character of the Port Macquarie Block but indicate that it is more geologically diverse than has previously been recognized. Northnortheast-trending faults divide the predominantly Palaeozoic mass into domains of differing rock sequences, structural character, and metamorphic history, and its unity derives principally from a persistent structural grain and the presence in each domain of members of a suite of metadolerites. ROCK UNITS Most of the Palaeozoic rocks of the Port Macquarie Block are placed in lithostratigraphic units of formational status that are defined here for the first time. Distribution of the various units is shown on Fig. 1. Watonga Formation The Watonga Formation comprises abundant chert and slate, uncommon meta- sandstone, and rare metabasalt, found east of the Lake Innes Fault. The name is derived from Watonga Rock (932171*) designated the type locality for the unit. Irregular folds and numerous faults throughout the formation prevent designation of a meaningful type section. Chert is typically thin-bedded with stratification defined by colour changes and the presence of thin slate beds and argillaceous partings. Massive chert found particularly adjacent to faults and in some fold hinges has resulted, at least in part, from intense deformation and partial recrystallization of originally thin-bedded units, for in some mesoscopic folds massive chert in the hinge area passes into stratified material in the fold limbs. The cherts are composed of anhedral interlocking quartz grains 0.01-0.02 mm across cut by several generations of quartz veins; traces of radiolaria remain in some samples. A few small mica flakes are scattered through the rocks, which contain tiny hematite grains that impart a progressively more intense red colour as their amount increases. At several localities (876144, 837095) hematite has been concentrated sufficiently to yield impure ironstone intercalations in the cherts. Slate forms units up to several tens of metres thick. It ranges from green chloritic quartz-poor varieties to dark grey micaceous types in which discontinuous quartz segregations occur parallel to cleavage. Stratification is indicated by colour changes and thin fine-grained meta-sandstone laminae. The rocks are texturally reconstituted, detrital relics are absent and cleavage is defined by parallel phyllosilicate films. Meta- sandstone is interstratified with slate at 873140. Little primary structure is preserved and relic detrital grains of plagioclase and less abundant quartz are scattered through a groundmass rich in white mica. Exposures of igneous rocks of the Watonga Formation (904197, 904191, 905185) are extremely weathered; abundant chloritic material suggests a mafic composition, and relic textural features indicated fine to medium grainsize. Although no stratigraphic divisions have been recognized within the formation several chert-dominated units each probably originally in excess of 100 m thick, are shown on Fig. 1. It is unclear whether the units comprise different stratigraphic levels, *Localities are specified by 6-digit grid references read from 1: 25,000 sheets Port Macquarie and Grants Head (lst edition, 9434-I-N and 9435-II-S) published by the New South Wales Department of Lands. Proc. LINN. Soc. N.S.W., 104 (4), (1979) 1980 NAMBUCCA i oh. CAINOZOIC ROCKS Laterite, alluvial, swamp and dune complexes 4 CAMDEN HAVEN GROUP 5 Osa) Conglomerate, sandstone FELSIC IGNEOUS ROCKS [FF | Strained porphyritic microgranodiorite Early 8: Triassic gee Late Permian Serpentinite, chlorite-tremolite and talcose rocks, exotic blocks KARIKEREE METADOLERITE Altered dolerite, in places massive, elsewhere cleaved A a (pe . y) : Y Middle Rock SERPENTINITE AND ASSOCIATES E. C. LEITCH 275 “a S(O a Py ) Z | (E a « S MG; Mal ee fi: 1 Point D) ah Fault (concealed) we Cleavage _-~ Bedding 90 9 Early Permian GOLGL G0, THRUMSTER SLATE WA: Slate, slaty sandstone "Middle" Palaeozoic TOUCHWOOD FORMATION Siltstone, sandstone, parconglomerate breccia, andesite Palaeozoic \ WATONGA FORMATION i Chert, slate, rare slaty sandstone. Chert-rich horizons indicated Sz Fig. 1. Geological map of the Port Macquarie Block. (Note an arrow head on the bedding symbol denotes direction of younging. ) Proc. Linn. Soc. N.S.W., 104 (4), (1979) 1980 276 PORT MACQUARIE BLOCK or whether they are tectonically repeated slices of the same horizon. The western contacts of two of the units are exposed (913207, 905197). At the first locality thin- bedded chert adjoins slate along a near vertical surface slightly oblique to the overall attitude of stratification in the chert and along which small weathered lenses of serpentinous material are found. Relationships at the second locality are less clear, but again an abrupt boundary is indicated. Several small serpentinite pods occur some 30- 50 m to the west of the contact, elongate parallel to it. At both localities isolated blocks of chert several metres long are imbedded in the slates and, especially at 905197, the structure of the slates is characterized by sudden along-strike changes, irregular sheared contacts and abrupt changes in degree of deformation. It is possible that many chert contacts in the Watonga Formation are complex shears that have largely remained unrecognized because of poor exposure. Elsewhere in the unit disruption is suggested by the presence of blocks of chert floating in clay (904191), and steeply-dipping chert zones 2-20 m wide alternating with clay zones 1-50 m wide across contacts oblique to stratification (905185). Biostratigraphically useful fossils have not been found in the unit and its age is uncertain. It is intruded by Late Permian metadolerite in the south and is lithologically similar to the Woolomin Beds as defined by Crook (1961) which are of pre-Devonian age (Leitch and Cawood, 1980). Interbedded meta-sandstone and slate at 873140 may belong to a different (? younger) sequence from the rocks further east, for they occur close to the Lake Cathie Fault and are not clearly interstratified with chert-slate sequences typical of the Watonga Formation. Touchwood Formation The name Touchwood Formation, derived from the property of that name (877177), is applied to a sequence of siltstone, sandstone, paraconglomerate, basalt breccia and andesite that lies between the Lake Innes and Innes Estate faults north of Lake Innes. Two small areas further south that lack outcrop are mapped as Touchwood Formation by extrapolation (Fig. 1). Neither top nor bottom of the unit is exposed, but it forms a west-younging sequence at least 600 m thick of which the upper 250 m comprises andesite. Typical epiclastic rocks of the formation are exposed in a 40 m section in an old quarry in western Port Macquarie (889224), which is designated the type section. Siltstone, dark grey to black in colour with a subconchoidal fracture, lacks primary structures apart from horizontal lamination defined by changes in colour and grain size; it characteristically occurs in beds less than 0.1 m thick interstratified with sandstone. The latter are indurated, grey, feldspatholithic rocks containing abundant volcanic debris that form units ranging in thickness from 0.01 to 1.0 m. Many beds are simply graded, a few show small-scale cross lamination, intraformational siltstone clasts are widespread, but the base of beds is usually planar. Paraconglomerate is Fig. 2. A. Paraconglomerate of the Touchwood Formation with fragments of limestone (white), siltstone and volcanic rock fragments (889224). B. Andesite from the upper part of the Touchwood Formation (882205). Scale bar = 2 mm. Crossed polars. C. Scattered quartz and plagioclase grains in a micaceous groundmass. Meta-sandstone of the Thrumster Slate (824171). Scale bar = 2mm. Crossed polars. D. Highly porphyritic Karikeree Metadolerite (beneath hammer head) in contact with Touchwood Formation rocks (beneath handle) (889224). E. Mylonitic groundmass containing strained and fractured relic quartz and plagioclase phenocrysts. From felsic dyke adjacent to Lake Cathie fault (838087). Scale bar = 2 mm. Crossed polars. F. Rounded folds affecting S, with incipient axial plane crenulation. Slates of Watonga Formation (873140). G. Tremolite-chlorite rocks to left of hammer contain small folds with axial plane cleavage dipping vertically and parallel to the contact of these rocks with cleaved slates to the right of hammer. Cleavage within the slates is oblique to the contact. Margin of Lake Innes mass (873140). H. Lenticular biotite aggregate cutting across crenulations in S, and their associated axial surface structure (S2). Same locality as F. Scale bar = 0.8 mm. Plane polarized light. Proc. Linn. Soc. N.S.W., 104 (4), (1979) 1980 277 E. C. LEITCH ey Ties. Proc. Linn. Soc. N.S.W., 104 (4), (1979) 1980 278 PORT MACQUARIE BLOCK composed of subrounded clasts of limestone, basalt, and andesite, and angular siltstone and interbedded sandstone-siltstone fragments similar to adjacent finer- grained rocks, set in a poorly sorted feldspatholithic sandstone matrix (Fig. 2A). Most conglomerate-grade material is in the size range 0.02-0.1 m diameter, but includes infrequent clasts of limestone up to 0.6 m and bedded sedimentary rocks up to 1.5 m. Clast to matrix ratio is about 1:2. Paraconglomerate forms beds ranging in thickness from 1.5-20+m. Internally the rocks are massive, although there is some preferred orientation of the long axes of clasts parallel to bedding, and in a thick bed at the base of the type section local concentrations of limestone pebbles are found. The top 1 m of this bed is graded from granule conglomerate to sandstone. All of the clastic rocks are characterized by their quartz-poor character and volcanic provenance. Lithic volcanic debris ranges from basalt to dacite with basalt and andesite dominant. Plagioclase is the most common detrital mineral, quartz is rare, and clinopyroxene is nearly always present in at least accessory amounts. A massive volcanic breccia horizon at least 50 m thick intercalated between bedded sandstone and siltstone below and coarse sandstone above, is exposed in an abandoned quarry (876183). The rock is composed of vesicular basalt fragments 5- 50 mm in diameter together with a few larger clasts (up to 0.1 m) of bedded sedimentary rocks comparable with those underlying the breccia, set in a coarse ill- sorted sandstone matrix. A coarse basalt breccia lacking sedimentary fragments occurs on the north side of the Hastings River (915252). Poorly exposed andesitic (keratophyric) rocks comprise the upper part of the formation. They are slightly porphyritic rocks, in which small phenocrysts of altered plagioclase occur scattered through a groundmass of aligned plagioclase laths and secondary minerals replacing intersertal glass (Fig. 2B). In contrast to the basaltic rocks clinopyroxene is absent. Tabulate and rugose corals occur in limestone blocks in the thick paraconglomerate of the type section but these are too altered to allow specific identification. Attempts to obtain conodonts from the limestone blocks were unsuccessful. Thrumster Slate Slate, meta-sandstone, and meta-granule conglomerate that outcrop between the Innes Estate and Cowarra faults are termed Thrumster Slate, after the parish of Thrumster in the northwestern part of the Port Macquarie Block. Scattered exposures along Lake Innes Drive (817171 to 824171) comprise the type section. Here, as elsewhere, outcrops are discontinuous and usually deeply weathered, and an estimated thickness of 650 m for this section, which provides a minimum for the unit, assumes no structural repetition of rocks and ignores tectonic thinning attendant upon cleavage formation. The stratigraphic limits of the Thrumster Slate have not been observed and no internal stratigraphy has been recognized. Slate, the dominant rock type, is of dark blue-grey to black colour when unweathered and has a distinct micaceous sheen. A single planar cleavage is ubiquitous and in some outcrops stratification is indicated by thin beds of poorly cleaved siliceous slate, and fine-grained meta-sandstone laminae. The slate is almost totally recrystallized with cleavage resulting from the parallel growth of white mica films that separate similarly aligned lenses of small quartz and albite grains. Coarse meta-sandstone and granule meta-conglomerate occur together in intervals several tens of metres thick accompanied by little finer-grained material. Individual beds are often simply graded and contain rip-up clasts of siltstone, some over 1 m long. These rocks are dominated by detrital quartz, with lesser relic detrital grains of plagioclase Proc. Linn. Soc. N.S.W., 104 (4), (1979) 1980 E. C. LEITCH 279 and felsic volcanic rock fragments scattered through a groundmass of white mica (Fig. 2C). No fossils have been found in the slate and the only signs of organic activity are faecal pellets found at one locality (830497). The unit closely resembles rocks of the Nambucca Slate Belt and on this basis is tentatively assigned an Early Permian age (Runnegar, 1970). Kartkeree Metadolerite Altered dolerite bodies emplaced within all three stratified Palaeozoic units are grouped in the Karikeree Metadolerite, named from Karikeree Creek that cuts several of the bodies along its course across the western part of the block. Outcrops along Lake Innes Drive (832168 to 827160) constitute the type section. The doleritic rocks are holocrystalline, of medium grain-size, and at least incipiently altered. Some are crammed with plagioclase phenocrysts up to 20 mm long (Fig. 2D) or contain large clinopyroxene plates, but most are approximately equigranular. Those relatively rich in clinopyroxene have an ophitic texture, whereas more felsic varieties tend to be hypidiomorphic-granular aggregates of equant clinopyroxene grains and plagioclase laths. Plagioclase of intermediate composition was the most common magmatic phase. Although it has been partially replaced by albite, relic labradorite, sometimes normally zoned, occurs in a number of specimens and even some quite highly reconstituted rocks retain feldspar of this composition. Magmatic calcic clinopyroxene is preserved in many metadolerites; colourless, very pale green and distinctly pink varieties are found in different rocks. Coarsely crystalline brown hornblende found in several metadolerites, either as discrete grains or mantling clinopyroxene, is a late-magmatic phase. Apatite rods and angular irregular opaque oxide grains are also magmatic relics. The alteration of dolerite ranges from incipient to complete. Albite, actinolite, chlorite, epidote and sphene are widespread secondary phases, white mica, clinozoisite, calcite and quartz are less widespread, and garnet is rare. Pseudomorphous replacement characterizes the massive metadolerites, but foliated bodies show a marked preferred orientation of secondary phases and the start of metamorphic differentiation. Planar zones of an exclusively metamorphic character up to a metre wide and containing restricted mineral assemblages, usually dominated by epidote, mark sites of extensive metasomatic alteration and were probably major hydrothermal passageways during metamorphism. Chemical composition and C.1.P.W. norms for a selection of metadolerites are given in Table 1. On present composition three samples, those with normative nepheline, would be considered alkalic, six samples are olivine-hypersthene normative, and one sample quartz normative and hence apparently tholeiitic. However the norm of the latter is much affected by a high Fe,O,/FeO ratio (0.58) and when recalculated for a value of 0.20, normative quartz virtually disappears (qz =0.01). As expected porphyritic samples contain high normative plagioclase and ophitic rocks have relatively large amounts of normative pyroxene plus olivine. The total alkali versus silica relationship (Fig. 3A, Macdonald and Katsura, 1964) would indicate that both tholeiitic and alkalic rocks are present, with a tendency for more highly metamorphosed rocks to appear more tholeiitic. However, when plotted on Miyashiro’s (1975) Na,O/K,O versus Na,O +K,O diagram some samples fall outside the field occupied by fresh volcanic rocks and the others occur in tholeiitic rather than alkali basalt fields (Fig. 3B). Changes in the amount of Na,O and K,O during metamorphism are indicated, and the magmatic affinities of the metadolerites cannot be unambiguously determined from their major element composition. Proc. Linn. Soc. N.S.W., 104 (4), (1979) 1980 280 PORT MACQUARIE BLOCK TABLE 1 Chemical Data 1 2 3 4 5 6 7 8 9 10 SiO, 49.09 48.13 47.99 47.90 47.75 47.01 46.92 47.04 46.94 44.83 TiO, 1.69 2.97 2.66 2.46 1.54 1.99 1.29 2.19 2.98 2.29 Al,O; 18.73 14.36 14.73 14.16 18.53 15.05 15.81 14.90 14.61 13.37 Fe,0, 0.84 2.28 2.34 1.56 1.72 1.63 1.30 4.29 4.99 3.14 FeO 7.69 10.86 9.97 10.68 7.22 8.98 7.50 7.79 8.54 9.32 MnO 0.15 0.23 0.21 0.23 0.16 0.19 0.16 0.22 0.23 0.20 MgO 5.31 5.46 5.75 6.65 6.16 7.44 9.08 7.16 6.20 11.76 CaO 10.38 8.76 8.50 9.90 11.84 10.48 10.20 9.84 9.29 7.97 Na,O 3.90 3.27 4.01 3.13 2.42 3.74 3.77 2.92 2.51 1.68 K,0 0.26 0.39 0.16 0.12 0.09 0.08 0.14 0.50 0.32 0.06 H,0* 2.08 2.39 3.88 2.85 2.49 3.85 3.41 2.82 2.79 5.63 H,O- 0.09 0.16 0.14 0.12 0.12 0.13 0.18 0.14 0.14 0.39 P.O; 0.19 0.32 0.27 0.25 0.18 0.20 0.11 — 0.20 0.30 0.25 Total 100.40 99.58 100.61 100.01 100.22 100.77 99.87 100.01 99.84 100.89 C.I.P.W. NORMS (anhydrous) qz 3.25 or 1.56 2.38 0.98 0.73 0.54 0.49 0.86 3.04 1.95 0.37 ab 31.68 28.51 35.13 27.29 20.98 27.30 24.67 25.46 21.92 14.98 an 33.43 24.07 22.49 24.99 40.40 24.85 26.80 26.87 28.54 30.32 ne 1.04 2.92 4.59 di 14.57 15.35 15.92 19.73 15.13 22.46 20.22 17.80 13.72 7.74 hy 17.71 5.88 11.37 13.74 10.66 16.59 30.72 ol 12.76 1.98 10.20 8.14 322) 15.15 18.09 4.99 5.87 mt 1.24 3.41 3.51 2.33 2.55 2.44 1.96 6.41 7.46 4.80 il 3.27 5.81 5.23 4.81 3.00 3.90 2.54 4.28 5.84 4.58 ap 0.46 0.78 0.66 0.61 0.44 0.49 0.27 0.49 0.73 0.62 Total 100.00 100.00 100.00 100.00 100.00 100.00 100.00 100.00 100.00 100.00 1 — 57518 Little-altered porphyritic dolerite (898224) 2 — 57519 Moderately altered metadolerite (812163). 3 — 57520 Moderately altered metadolerite (811160). 4 — 57521 Moderately altered ophitic metadolerite (815140). 5 — 57522 Moderately altered porphyritic metadolerite (817137). 6 — 57523 Little-altered ophitic dolerite (812183) . 7 — 57524 Moderately altered ophitic metadolerite (834153). 8 — 57525 Moderately altered metadolerite (858077) . 9 — 57526 Moderately altered ophitic metadolerite (826083). 10 — 57527 Highly altered metadolerite (832168). Analyses by X-ray fluorescence spectrometry except for FeO (titrimetry), H.O (gravimetry). R. Beck, analyst. The metadolerite masses comprise mainly tabular bodies that range in width from 1m to more than 30m. Many of the larger masses shown on Fig. 1 are composite, formed of several parallel bodies often separated by thin (1-10 m) screens of country rock. Where intrusive relationships have been determined the massive, little altered and sometimes porphyritic bodies post-date more altered foliated dykes. The latter tend to lie parallel to cleavage in adjacent rocks, whereas the former though Proc. Linn. Soc. N.S.W., 104 (4), (1979) 1980 E. C. LEITCH 281 =~. Satlantic-a Island arc volcanic rocks xs (o) N | sas [e) Nw ic} 2 ine) te Atlantic: if ae A Fig. 3. A. SiO, versus Na,O + K,O for Karikeree Metadolerite. Alkalic-tholeiitic division from Macdonald and Katsura (1964). B. Na.O / K,O versus Na,O + K,O for Karikeree Metadolerite with fields of Cainozoic volcanic rocks indicated (after Miyashiro, 1975). Abyssal tholeiites (Aby-th) , Hawaiian tholeiites (Hw-th), Icelandic tholeiites (Ic-th), Icelandic alkalic rocks (Ic-a), alkalic rocks from other Atlantic Islands (Atlantic-a) and from eastern Asia (Asia-a) , and common arc volcanic rocks. Numbers are last two digits of University of Sydney numbers indicated on Table 1. maintaining this orientation in places elsewhere cut obliquely across structural surfaces in the surrounding formations. Cleavage within the metadolerites is variably developed; some bodies are uniformly cleaved, others contain narrow zones of enhanced cleavage, and some otherwise massive dykes have narrow cleaved margins. Contact effects adjacent to the bodies are restricted to a zone from 0.1 to 0.4 m wide wherein the country rocks have been partially silicified and cleavage is less conspicuous. Karikeree Metadolerite intrudes the Early Permian(?) Thrumster Slate and is truncated by the Late Permian Burrawan serpentinite. The rocks were emplaced during and perhaps immediately after orogenesis, and a Late Permian age is favoured. Serpentinite bodies and related rocks Serpentinite bodies occur both within and at the margin of the Port Macquarie Block. The largest mass is that at the southwest corner of the block in the parish of Burrawan, here referred to as the Burrawan serpentinite. A lens of tremolite-chlorite rock containing talc-rich areas and serpentinite blocks on the eastern shore of Lake Innes (873140) is referred to as the Lake Innes mass. Small serpentinite lenses occur along the Cowarra Fault (153800, 157801) and in quarries near Port Macquarie (913207, 905197). Serpentinite mapped in the vicinity of the Lake Cathie Road (827083) and on the Pacific Highway (811160) by Brunker, Offenberg and Cameron (1970) were not located; only outcrops of Karikeree Metadolerite were found at these localities. Both massive and schistose serpentinite are present, the former variety being more common in the Burrawan mass and the latter forming the bulk of the smaller bodies. In the schistose rocks several generations of structural surfaces can be Proc. Linn. Soc. N.S.W., 104 (4), (1979) 1980 282 PORT MACQUARIE BLOCK recognized, with the earliest and dominant often folded and overprinted by an axial surface cleavage and, in some outcrops, a later discrete spaced cleavage. Massive serpentinite comprises dark, subconchoidally-fracturing material containing bastite pseudomorphs. It occurs in blocks up to a metre in maximum dimension separated by schistose material that in places is only a selvedge a few centimetres wide, but elsewhere forms a matrix in which individual blocks are separated by distances as great as their maximum dimension. Clinochrysotile is the dominant serpentine mineral in most bodies. Massive serpentinite also contains lizardite which probably constitutes the bastite pseudomorphs (Wicks and Whittaker, 1977) that are scattered through the mesh- textured groundmass. Progressive deformation and destruction of bastite in increasingly more schistose material is accompanied by a decrease in the amount of lizardite and the appearance of orthochrysotile. Brucite is present in small amounts and magnetite is widespread in all chrysotile serpentinites. No relics of pre- serpentinization minerals remain apart from irregular rounded chromite grains. Serpentinite blocks in the Lake Innes mass are composed of a bladed mat of small crystals forming a groundmass and partially replacing strained bastite crystals. Antigorite is the only serpentine phase identified in these rocks, which also contain small amounts of talc. Magnesite is present as a weathering product of the serpentinites, and chalcedonic silica occurs in the southern part of the Burrawan body. Tectonic inclusions that are scattered throughout the Burrawan serpentinite are mostly chert identical with that in the Watonga Formation, and highly altered dolerite and amphibolite, in which prehnite is a common phase. Inclusions of massive siltstone similar to that in the Hastings Block are restricted to the western part of this body. Several blocks of glaucophane schist up to a metre long are associated with metadolerite and a highly foliated quartz-albite rock, along the trace of the Innes Estate Fault (826117). None of this material is zm sztu, but it is almost certainly of local derivation. The blocks are probably tectonic inclusions weathered out of a recessive serpentinite lens. The serpentinite bodies are intrusive with respect to the stratified Palaeozoic rocks and the Karikeree Metadolerite, and have been emplaced as cold masses along faults. Voisey (1939) reported that the Burrawan serpentinite is unconformably overlain by Triassic strata, and although I have not located an exposure of this contact, his interpretation is accepted and a Late Permian age for emplacement of the body favoured. However, movement on the Sapling Creek Fault subsequent to deposition of the Triassic rocks has locally brought these into tectonic contact with the serpentinite (Fig. 1). Along this section the southern margin of the mass is silicified, probably as a result of these late movements. Felstc dykes Two narrow felsic dykes have been mapped within the Port Macquarie Block, one trending just west of north adjacent to the Pacific Highway (813183-814177), and the other striking northeast west of Lake Cathie (833076-839090). The rocks of both bodies are strained and altered. Their general composition is granodioritic, with quartz and plagioclase the dominant constituents; potassic feldspar is uncommon and primary mafic minerals are not preserved. The Lake Cathie body, which lies adjacent to the Lake Cathie Fault, has been converted to a blastomylonite; plagioclase and quartz phenocrysts remain in a fine groundmass of albite grains, highly strained and marginally recrystallized elongate quartz grains, and slightly wavy white mica films (Fig. 2E). The phenocrysts have been fractured, bent, and rotated during deformation as is indicated by the disruption Proc. Linn. Soc. N.S.W., 104 (4), (1979) 1980 E. C. LEITCH 283 of twin lamellae in formerly contiguous fragments of feldspar. That they were originally igneous is indicated by relic magmatic embayments preserved in some quartz grains. The igneous texture of the Pacific Highway dyke is clearer; rare plagioclase microphenocrysts and graphically intergrown quartz-feldspar clots are scattered through a granular quartz-feldspar groundmass. Both quartz and plagioclase crystals are strained, the rock is crossed by quartz-albite veins, and secondary pyrite and chlorite are present. The Pacific Highway body intrudes Karikeree Metadolerite and hence is probably of post-Early Permian age. Because of its similar composition a similar age is suggested for the Lake Cathie body. Both dykes were emplaced prior to the end of fault movements which probably continued into post-Early Triassic times (Leitch and Bocking, 27 press) . Camden Haven Group Quartzose coarse clastic rocks of the Early Triassic Camden Haven Group, previously only recognized south of the Sapling Creek Fault, also occur in the southern part of the Port Macquarie Block where they are believed to unconformably overlie Palaeozoic units (Fig. 1). Both the prominent scarp-forming chert conglomerate termed the Laurieton Conglomerate by Pratt and Herbert (1973), and an older lithic conglomerate unit (Leitch and Bocking, 7n press) have been recognized. Tertiary and Quaternary rocks Very deep weathered zones, laterite, and extensive Quaternary alluvial, swamp, and dune complexes mask much of the Palaeozoic basement. A metre-wide camptonite dyke cutting Karikeree Metadolerite at Middle Rock Point (857076) probably belongs to the Tertiary alkaline province more voluminously represented west and southwest of the Port Macquarie Block (McDougall and Wilkinson, 1967). STRUCTURE Faults The structure of the Port Macquarie Block is dominated by a set of northnortheast-striking faults which juxtapose stratified rocks belonging to different formations and of contrasting metamorphic grade and structural character. Large but unestablished strike-slip movements are indicated, for no relationship exists between metamorphic grade and the age of rock units, a relationship which might be anticipated if vertical movements had led to the exposure of different levels of a stratified sequence. Major fault surfaces have not been seen, but steep dips are suggested by approximately straight fault traces, the vertical attitude of serpentinite bodies emplaced along the faults, and the steep inclination of small-scale shear fractures within the Block. The Cowarra Fault bounds the Block to the northwest, its position marked by an abrupt change in rock types, from uncleaved conglomerate sandstone and siltstone of the Hastings Block to metadolerite and slate. Small serpentinite lenses occur along the southern part of the fault and further north (819202) highly irregular folds in the Thrumster Slate indicate its proximity. A sliver of Hastings Block rocks is surrounded by slate where the fault cuts the Pacific Highway (832212), suggesting the fracture here is of more complex structure than elsewhere. The presence of the Tenterden Fault is inferred from the distribution of Thrumster Slate and Karikeree Metadolerite south of Karikeree Creek. The Innes Estate Fault marks the western limit of the Touchwood Formation and is a major structural and metamorphic discontinuity: cleavage, ubiquitous in pelitic rocks west of the fault, is absent on its eastern side, and metamorphic grade changes from Proc. Linn. Soc. N.S.W., 104 (4), (1979) 1980 284 PORT MACQUARIE BLOCK greenschist in the west to prehnite-pumpellyite in the east. Close to its trace Thrumster Slate shows numerous kink bands and associated less regular small folds. The eastern extent of the Touchwood Formation is determined by the Lake Innes Fault east of which cleaved rocks of greenschist grade are again found. Pits from which lateritic iron was once quarried (876173, 894212 and 896215) occur along the trace of the fault and Harrison (1955) recorded serpentinite, not now visible, in the pit at the last locality. The Lake Cathie Fault is mapped on the basis of the presence and shape of the Lake Innes serpentinite mass, the abrupt termination of a prominent hematite chert horizon in the Watonga Formation northwest of Lake Cathie, and the mylonitic structure of the granodiorite dyke west of Lake Cathie. The northern continuation of the fault passes through a body of serpentinite in the grounds of the Catholic Church in Port Macquarie (913223). In the south the Cowarra and Tenterden faults abut the Burrawan serpentinite and the three fractures situated further east are cut off by the northwest striking Sapling Creek Fault. This structure brings Palaeozoic rocks in the northeast in contact with Triassic strata to the southwest. A small mass of serpentinite, mapped by Leitch and Bocking (zn press) at 813046 (see their fig. 1), possibly marks the position of the Cowarra Fault south of the Sapling Creek Fault (Fig. 1), suggesting sinistral strike-slip movement of about 4 km on the latter. Structural domains The major northnortheast faults bound domains of differing structural character (Fig. 4). Within these domains bedding (S,) and slaty cleavage (S,) are the dominant surfaces, the latter forming the axial surface to folds in the former (Bj). A lineation produced by the intersection of the two surfaces (L(0x1)) is occasionally discernible. The internal structure of the domains is discussed below. Domain I: S,, the dominant structural surface in Domain I, occurring both in the Thrumster Slate and in early members of the Karikeree Metadolerite, parallels the axial surface of small, rather angular tight to isoclinal folds in So, but is unaffected by later mesoscopic structures apart from kink-bands and less regular folds close to the Innes Estate Fault. The stereographic projection of poles to S, (Fig. 4A) shows a slightly elongate point maximum suggesting an average orientation of 015/75/W but with slight flexure about an axis plunging approximately 75 to 196, a flexure also indicated by the curve of metadolerite bodies in the southwest of the domain (Fig. 1). Stratification is not common in this domain and is most readily observed where it is at a high angle to S,. Hence in spite of the narrow hinges and near-parallel limbs of mesoscopic Bg structures, the distribution of S, differs from that of S, (Fig. 4B). Insufficient readings are available to allow a detailed study of the geometry of this surface, and the absence of mappable marker horizons and a dearth of younging structures inhibit recognition of major Bé folds. Most mesoscopic Bo folds and L (0x1) lineations plunge very steeply (Fig. 4B) and probably maintain a coherence because of the steep plunge of the axis about which S, flexure occurred. The two readings that plunge moderately southwest come from within 1 km of the Burrawan serpentinite and may have been rotated during emplacement of this mass. S, in this area strikes west of north and may also have been so affected. Domain II: So in the Touchwood Formation strikes approximately northeast and dips about the vertical, younging consistently northwest (Fig. 4C). No mesoscopic folds are present and cleavage is absent both from these rocks and Karikeree Metadolerite dykes emplaced within them. Domain III: S,, the only widely developed structural marker in the rocks of domain III, has an average strike of about northeast and generally dips at a moderate angle northwest (Fig. 4D). Slate and meta-sandstone adjacent to the Lake Innes mass Proc. Linn. Soc. N.S.W., 104 (4), (1979) 1980 E. C. LEITCH 285 “TT So xL(Ox1), Bo - "S" folds x "Z" folds * "Z" kinks Fog. 4. Structural data for the Port Macquarie Block. Plots are equal angle stereographic projections and roman numerals refer to the domains indicated in H. See text for detailed descriptions. Proc. Linn. Soc. N.S.W., 104 (4), (1979) 1980 286 PORT MACQUARIE BLOCK are unique in the Port Macquarie Block in showing small-scale rounded folds in S, with an axial surface crenulation cleavage (Fig. 2F). However dispersion of S, overall in domain III is not related to structures of this generation which lack a consistent orientation and appear to have been affected by later movement (Fig. 4D). Domain IV: A diversity of styles and a wide range in orientations suggest that several generations of mesoscopic folds are present in bedded cherts in the northern part of domain IV, but their analysis is hampered by the absence of axial surface structures and clear overprinting relationships. Some folds are extremely intricate convoluted structures possibly formed before complete lithification of the rocks, others have hinge zones in which bedding is partially obscured by recrystallization and close jointing, and appear to be of significantly later origin. The distribution of poles to Sy (Fig. 4E) clearly indicates a complex overall geometry for this surface. Observations of slaty cleavage in domain IV although limited in number, suggest that it is less complexly deformed than So, and poles to S, occupy a broad partial girdle that indicates flexure about an axis plunging approximately 60 to 335 (Fig. 4F). This deformation appears on a megascopic scale in the progressive change in the strike of S, in the southern part of the domain, from near north-south close to the Lake Cathie Fault to east-west at Middle Rock Point. It has also probably resulted in the flexure of the chert-rich units south of Port Macquarie (Fig. 1). Slates at Watonga Rock show a prominent set of small conjugate folds that are probably related to faulting, and imply a near horizontal principal compressive stress trending northnorthwest (Fig. 4G). Kink bands from domain I close to the Innes Estate Fault are of similar orientation to Z-shaped folds at Watonga Rock and show the same vergence. Serpentinites and associated rocks: No systematic study of the internal structure of the serpentinites and their associates has been attempted but scattered observations indicate that the structure within these masses are largely independent of those in the surrounding rocks. The earliest surface identified is frequently folded, usually about steeply plunging axes. In the Lake Innes mass the axial surface of the folds is parallel to the contact of the lens with surround rocks, but is oblique to S, in these rocks (Fig. 2G). The mesoscopic folds affecting S, in the country rocks here have also affected the margin of the mass, and keel-like lenses of talc-rich material have been partially folded into adjacent slates. Structural correlation: The presence of Karikeree Metadolerite with a single cleavage coincident with that in adjacent rock units in domains I, III and IV suggests S, developed in post-Early Permian times, and is of comparable age in each domain. These domains have a similar deformation history, with cleavage formation followed by broad large-scale warping about moderate-steeply plunging axes and only local development of post-S, mesoscopic features, suggesting their structure evolved in closely related circumstances. By contrast domain II lacks imposed penetrative structures or obvious folds, and was probably brought into association with the other domains as a result of large fault movements late in the history of deformation. METAMORPHISM All Palaeozoic rocks of the Port Macquarie Block are at least incipiently altered, and many show the effects of pervasive metamorphism. Differences betwen the rocks of domain II and those of the remainder of the block indicated by structural characters, are also reflected in their metamorphic grade and style. Other domains contain greenschist facies assemblages and most rocks have a strong preferred orientation of metamorphic phases, but the rocks of domain II are of subgreenschist grade and new minerals have grown pseudomorphously or in irregular replacement Proc. Linn. Soc. N.S.W., 104 (4), (1979) 1980 E. C. LEITCH 287 patches and veins. These two groups of rocks are discussed separately below, as are the products of a late thermal event that affected a small area east of Lake Innes, and glaucophane schist blocks associated with the Innes Estate Fault. Metamorphism in domain II All domain II rocks retain their original texture and much of their pre- metamorphic mineralogy; secondary minerals are patchily developed and there is abundant evidence of incomplete replacement. Rocks of the Touchwood Formation have developed a range of low-grade metamorphic assemblages including: (i) albite — chlorite — epidote — prehnite — pumpellyite (ii) albite — chlorite — epidote — prehnite (iii) albite — chlorite — actinolite — prehnite (iv) albite — chlorite — epidote (v) albite — chlorite — actinolite — epidote In addition sphene is a ubiquitous metamorphic phase, calcite is frequently encountered but only in small amounts, quartz has crystallized during metamorphism in some rocks and in others is present as a relic phase showing no sign of alteration, and white mica is a common but minor secondary mineral. There is little control of metamorphic mineralogy by rock type, although white mica is restricted to epiclastic rocks and (iv) characterizes the andesites of the formation. Assemblages (1), (ii) and (iii) are all characteristic of the prehnite-pumpellyite metagreywacke facies, with (iii) suggesting the rocks were subjected to conditions close to those at the upper limit of this facies (Coombs, Horodyski and Naylor, 1970). Neither (iv) nor (v) is restricted to a particular facies, but both confirm the low grade of alteration. Assemblage (v) is probably more typical of greenschist facies metamorphism than lower grade facies, especially in rocks reconstituted under conditions of low fCO, as are indicated for the Touchwood Formation. Specimens showing this assemblage are known only from the southern part of the main outcrop of domain II rocks, and it is possible that they fall within the Lake Innes thermal high (see below) and hence have been affected by a second metamorphic event. Karikeree Metadolerite from domain II contains the secondary mineral asemblage: (albite) — chlorite — actinolite — sphene — white mica — calcite and is noteworthy for the preservation of most magmatic calcic plagioclase, alteration of which is restricted to narrow irregular veins filled by albite, and the crystallization of tiny white mica flakes. The secondary mineral assemblage is not specific as to grade but is consistent with that indicated by the Touchwood Formation. The retention of plagioclase (and also calcic clinopyroxene) has meant that components necessary for the formation of calcium aluminosilicate minerals were not released in these rocks. Regional metamorphism in domains I, III and IV Stratified rocks of domains I, III and IV show the imprint of a regional metamorphic event that also affected members of the Karikeree Metadolerite in these domains. There is little evidence for variation in metamorphic grade throughout the rocks, although the metadolerite bodies show a range in degree of reconstitution and fabric development which suggests some were introduced at only a late stage during metamorphism. Pelitic and psammitic rocks show typical sub-biotite grade mineral assemblages of the type quartz — albite — white mica — (chlorite) — (epidote) whereas chert has reconstituted to assemblages including quartz — white mica — hematite, quartz — stilpnomelane — hematite and quartz — chlorite — stilpnomelane — hematite. Proc. LInn. Soc. N.S.W., 104 (4), (1979) 1980 288 PORT MACQUARIE BLOCK Metamorphic assemblages recognized in the Karikeree Metadolerite are: (i) albite — actinolite — chlorite — epidote — sphene — (white mica) — (quartz) — (calcite) (ii) actinolite — chlorite — epidote — sphene — white mica — (quartz) — (calcite) (iii) albite — actinolite — epidote — sphene — (quartz) (iv) albite — chlorite — epidote — sphene (v) albite — chlorite — quartz (vi) epidote — garnet — calcite Of a total of 31 specimens examined, 18 contained assemblage (i), 5 contained (11), 4 contained (ii1)), 2 contained (iv), 1 contained (v) and 1 contained (vi). Assemblages (i) and (ii) include the least altered and texturally restructured metadolerites but there is no systematic difference in degree of alteration between the two assemblages. In particular the failure of albite to form at the expense of calcic plagioclase in (ii) is not related to an overall low degree of alteration. Rocks characterized by (ii) contain abundant epidote, and it is likely that the absence of albite is related to a very high Ca’*/Na* ratio in the local fluid phase during metamorphism, which both enhanced the stability of calcic plagioclase relative to albite, and supplied the calcium necessary for epidote crystallization. The ubiquitous presence of small amounts of white mica in assemblage (ii) rocks is possibly a result of the failure of albite to form. Small amounts of potassium in the rocks, that could have been accommodated in albite had it formed, instead gave rise to a potassic phase. It is noteworthy that white mica occurs in all rocks of assemblage (ii) but occurs in only 3 of the assemblage (i) samples, in each of which much magmatic calcic plagioclase remains and albite is present in only small amounts. White mica also occurs in all domain II metadolerites which are characterized by little or no albite. Assemblages (iii)-(vi) occur in highly altered rocks believed to have suffered metasomatic changes involving increase in Ca ( (iii) and (vi) ), relative increase in Al (iv), and loss of Ca (v). The mineral assemblages found in domains I, III and IV indicate regional metamorphism took place under low greenschist facies conditions. Neither prehnite nor pumpellyite is present and biotite has not formed in the pelitic or psammitic rocks. Assemblage (i) in the Karikeree Metadolerite is typical of the lower part of the greenschist facies. Similar assemblages occur a little to the north of the Port Macquarie Block in the Nambucca Slate Belt (Leitch, 1976a). The Lakes Innes thermal high Rocks that outcrop in the southern part of the promontory separating Lake Innes from Innes Swamp show the impress of a static thermal metamorphic event on the earlier regional metamorphic fabric. Mineral assemblages identified in stratified rocks here are: (1) quartz — albite — white mica — biotite — chlorite — epidote — tourmaline (ii) quartz — albite — white mica — chlorite — epidote (iii) quartz — hematite — (white mica) — (chlorite) — (garnet) Assemblage (i) is confined to pelitic rocks, (ii) typifies psammites and (iii) occurs in metamorphosed chert. The pelitic and psammitic rocks are those of domain III that possess both S, and a crenulation cleavage S, axial plane to folds in S,. Textural relationships indicate that the assemblages are the result of recrystallization both during the formation of S, and S,, as well as subsequent to the development of the latter surface. S, is defined by the parallel orientation of white mica and chlorite flakes which are bent and have polygonized in the hinges of the post-S, folds. Some white mica has grown along S, in pelitic rocks and irregular patches of chlorite are Proc. Linn. Soc. N.S.W., 104 (4), (1979) 1980 E. C. LEITCH 289 concentrated in the hinge zone of microfolds in psammites. Biotite in the pelites is pleochroic in drab shades of green and brown. It occurs in decussate aggregates cutting across S, and S, (Fig. 2H), and in randomly oriented grains concentrated along chlorite-rich layers parallel to S,. Biotite is nowhere deformed and it clearly has formed subsequent to the development of S,. Tourmaline also crystallized in these rocks after deformation, for prisms of this phase grow across S, and S, but are neither bent nor fractured. In addition to the presence of small amounts of garnet in some samples, a somewhat higher metamorphic grade for the cherts of this area compared with those elsewhere in the Block is indicated by their coarser grain size. Cherts in the Lake Innes thermal high have average quartz grain diameter of about 0.05 mm compared with 0.01-0.02 mm elsewhere. Additional evidence for a late-stage thermal metamorphism in this region is furnished by the serpentinite in the Lakes Innes mass. Although emplacement of these rocks post-dated regional metamorphism, blocks within the mass are composed of antigorite, rather than lizardite and chrysotile that characterize the other serpentinite bodies of the Port Macquarie Block. Antigorite serpentinites are generally considered to result from alteration at significantly higher temperatures than are lizardite- chrysotile serpentinites (e.g. Coleman, 1971) and the antigorite has probably resulted from the metamorphism of lizardite-chrysotile material during late-stage heating. Talc-rich lenses on the margins of this mass, and widespread tremolite-chlorite rocks, probably also result from reactions during the thermal event. Post-tectonic metamorphic highs similar to that at Lake Innes occur elsewhere in the New England Fold Belt (e.g. Gunthorpe, 1970; Leitch, 1972; Korsch, 1978), in places associated with abundant silicic dykes suggesting a subjacent granite pluton. Although no dykes have been discovered at Lake Innes a buried plutonic body is considered to be the most likely heat source. Late stage crystallization of tourmaline might be construed as evidence of boron addition to the rocks from a granite body, but the amount of tourmaline present is not large, and the required boron may have been inherited from the precursor sedimentary parents of the metamorphic rocks (cf. Reed, 1958). Glaucophane schist blocks The glaucophane schist blocks along the Innes Estate Fault consist of dark blue fine-grained, schistose rock characterized by the presence of lavender blue to colourless amphibole prisms. The amphibole forms a nematoblastic mat enclosing lenses and clots of fine-grained chlorite and pumpellyite, and tabular clinozoisite crystals. Small murky sphene grains are concentrated along fine seams roughly parallel to cleavage. Calcic clinopyroxene crystals, fractured and partially replaced by glaucophane, are pre-metamorphic relics. The rocks are cut by veins of glaucophane and clinozoisite and by later irregular calcite or calcite-albite patches. The metamorphic mineralogy, and the presence of relic calcic clinopyroxene suggests the schists were derived from basic igneous rocks. The metamorphic mineral assemblage in these rocks, glaucophane — chlorite — clinozoisite — pumpellyite — sphene — calcite — (albite) is that characteristic of rocks transitional between greenschist and blueschist facies. Absence of lawsonite, jadeite and aragonite indicates metamorphic pressures not greatly above those attained in the greenschist facies, and the presence of pumpellyite suggests relatively low temperatures, less than those of the greenschist facies. The relationship between the metamorphism giving rise to the glaucophane schists and that responsible for the greenschist facies rocks of the Port Macquarie block is not known. Schistosity in the glaucophanitic rocks is strongly crenulated, perhaps Proc. Linn. Soc. N.S.W., 104 (4), (1979) 1980 290 PORT MACQUARIE BLOCK indicating a more complex deformation history than that suffered by the greenschist facies rocks. Although it has been suggested that the blocks are tectonic inclusions within a serpentinite lens (p. 282), an origin as accidental fragments derived from beneath the associated greenschist rocks appears unlikely. GEOLOGICAL HISTORY Three phases can be recognized in the geological development of the Port Macquarie Block: a pre-orogenic phase during which the stratified Palaeozoic rocks accumulated, an orogenic phase that commenced with the onset of penetrative deformation and regional metamorphism of many of the stratified rocks and ended with the juxtaposition of the various fault slices that comprise the block, and a late- orogenic phase with faulting on a more restricted scale, probably involving mainly vertical movements and perhaps associated with local plutonic igneous activity. Pre-orogentc phase The Watonga Formation is a member of an Early Palaeozoic chert-siliceous argillite-basalt association, widely distributed in the southern part of the New England Fold Belt, and believed to comprise mostly ocean-floor deposits scraped from downgoing lithosphere at a consuming plate margin (Leitch, 1974). The dominance of fine-grained terrigenous detritus, the absence of limestone or massive sandstone, and the presence of widespread bedded radiolarian chert, accord with a deep marine depositional environment. Progressive detachment of the rocks from basaltic ocean floor along a system of imbricate thrust faults could give rise to the repetition of beds suggested by the several chert units, and the disrupted character of the formation with occasional basic igneous intercalations would be anticipated in the rocks of a subduction zone. The Touchwood Formation clearly belongs to a quite different setting, having accumulated close to a volcanic region comprising rocks ranging from basalt to dacite, but in which subsilicic material was most common. Clastic sedimentary rocks of the formation are mostly turbidite and debris-flow deposits, suggesting accumulation in a relatively steep-sided basin fed by material swept from unstable shelf or delta-front environments. The oligomictic nature of some volcanic-derived units indicates rapid remobilization of debris the initial accumulation of which may have closely followed eruption. Coralline limestone blocks in some paraconglomerates suggest erosion of newly-deposited shelf material and channelling of the basin floor is indicated by abundant intraformational siltstone fragments in many of the coarser rocks. Lateral migration of volcanic activity gave rise to the thick andesite mass that caps the exposed sedimentary sequence. The parent material of the Thrumster Slate accumulated in a region dominated by siltstone deposition but into which coarse clastic debris derived from silicic volcanic rocks was periodically carried by turbidity currents. The Slate is closely related to the Watonga Formation in its orogenic history, and it is possible that it accumulated in a basin developed on Watonga rocks. All three formations can be envisaged as fragments of a Palaeozoic active margin. Subduction zone rocks of the Watonga Formation formed a basement for the Thrumster Slate that accumulated either in a slope basin on the accreting face of the zone, or, more likely in view of the probable age difference between the two units, in the outer part of an evolved fore-arc basin above the subsiding older part of the subduction zone. Touchwood rocks are representative of the magmatic arc — inner fore-arc basin realm that were juxtaposed with the other rocks by transcurrent faulting that sliced the margin obliquely at a late stage in orogenesis. Proc. Linn. Soc. N.S.W., 104 (4), (1979) 1980 E. C. LEITCH 291 Orogenic phase Orogenesis affected the Port Macquarie Block in the Late Permian, in the interval between deposition of the Thrumster Slate and the Camden Haven Group. The earliest and most intense deformation, and accompanying greenschist facies metamorphism, affected the Thrumster Slate, the Watonga Formation and the oldest members of the Karikeree Metadolerite. It resulted in the production of near-isoclinal steeply plunging folds and a steeply dipping slaty cleavage. Emplacement of dolerite dykes continued through this period and the presence of little-deformed dykes showing greenschist facies metamorphism suggests that elevated temperatures continued for a period after the relaxation of pervasive stresses. ' This relaxation may have followed inception of movement on the northnorthwest- trending faults. Although little control is available, contrasts across the Cowarra, Innes Estate and Lake Innes faults point to large amounts of transcurrent displacement, most of which was completed before emplacement of the serpentinite masses. Thus the Burrawan body truncates several of these fractures and was probably emplaced during movement on the Sapling Creek Fault. By this time temperatures had fallen to sub-greenschist values as indicated by the presence of chrysotile and lizardite and the replacement of plagioclase by prehnite in dolerite blocks. The conditions under which mobilization of the serpentinite bodies occurred are unclear, but it is likely that their rise was initiated under relatively low temperatures and perhaps was accompanied by some re-equilibration of the surrounding metamorphic rocks producing glaucophane schists. Local folding and the formation of crenulation cleavage post-dated emplacement of the Lake Innes mass indicating minor coherent deformation took place later in orogenic history. Late-orogenic phase Although the main orogenic phase was relatively short-lived, structural adjustments continued until after deposition of the Camden Haven Group. Vertical movement on the Sapling Creek Fault disrupted these strata and several faults with northnortheast trends have affected Camden Haven rocks northwest of Grants Head. Abrupt changes in the thickness of formations within the Camden Haven Group take place across northnortheast-trending faults in the Palaeozoic rocks suggesting fault control of sedimentation in the Early Triassic (Leitch and Bocking, zn press). Emplacement of Triassic granitic rocks elsewhere in the eastern part of the New England Fold Belt was accompanied by vertical faulting (Leitch, 1976b), and the inferred plutonic mass beneath the Lake Innes thermal high was possibly intruded at this time. Further south in the Lorne Basin several large granitic plutons yield Late Triassic K-Ar ages (McDougall and Wellman, 1976). It is unclear whether the felsic dykes of the Port Macquarie block are related to this activity, and owe their strained character to proximity to faults on which there was significant late movement or whether they are representatives of an earlier episode of granitic magmatism. ACKNOWLEDGEMENTS Field work has been supported by funds from the Australian Research Grants Committee and the University of Sydney. Discussions with the Honorary Editor, Associate Professor T. G. Vallance, are gratefully acknowledged. Mr Rolf Beck is thanked for the chemical analyses. I am grateful to Messrs George Navratil, Neil McLeod, Jeff Imison and Dick Sealy for technical assistance, and thank Mr Len Hay for drafting the diagrams, and Miss Sheila Binns for typing several drafts of the manuscript. Proc. Linn. Soc. N.S.W., 104 (4), (1979) 1980 292 PORT MACQUARIE BLOCK References BarRRON, B. J., SCHEIBNER, E., and SLansky, E., 1976. — A dismembered ophiolite suite at Port Macquarie, New South Wales. Rec. Geol. Surv. N.S.W., 13: 69-102. BRuNKER, R. L., OFFENBERG, A. C., and CAMERON, R. G., 1970. — 1: 250,000 Geological sheet SH/56-14, Hastings. Geol. Surv. N.S. W. CaRNE, J. E., 1897. — Notes on the general and economic geology of the coast between Port Macquarie and Cape Hawke. Records Geol. Surv. N.S.W., 5: 533-64. CoLeMaN, R. J., 1971. — Petrologic and geophysical nature of serpentinites. Geol. Soc. Amer. Bull., 82: 897-918. Coomss, D. S., Horopyski, R. J., and NayLor, R. S., 1970. Occurrence of prehnite-pumpellyite facies metamorphism in northern Maine. Amer. J. Sct., 268: 142-156. Crook, K. A. W., 1961. — Stratigraphy of the Tamworth Group (lower and middle Devonian), Tamworth-Nundle district. J. Proc. R. Soc. N.S.W., 94: 173-188. GuNTHORPE, R. J., 1970. — Plutonic and metamorphic rocks of the Walcha-Nowendoc- Yarrowitch district, northern New South Wales. Armidale: University of New England, Ph.D. thesis, unpubl. Harrison, E. J., 1955. — Port Macquarie iron oxide deposits. Annual Rept. Dept. Mines, N.S.W., for TO 5 le iiloS: KorscH, R. J., 1978. — Regional-scale thermal metamorphism overprinting low-grade regional metamorphism, Coffs Harbour block, northern New South Wales. J. Proc. Roy. Soc. N.S.W., 111: 89-96. LeitcH, E. C., 1972. — The geological development of the Bellinger-Macleay region, northeastern New South Wales. Armidale: University of New England, Ph.D. thesis, unpubl. ——, 1974. — The geological development of the New England fold belt. J. geol. Soc. Aust., 21: 133-156. ——, 1976a. — Zonation of low grade regional metamorphic rocks, Nambucca Slate Belt, northeastern New South Wales. J. geol. Soc. Aust., 22: 413-422. —— , 1976b. — Emplacement of an epizonal pluton by vertical block elevation. Geol. Mag., 113: 553-560. , In press. — The Great Serpentine Belt of New South Wales: diverse mafic-ultramafic complexes set in a Palaeozoic arc. Proc. Internat. Ophiolite Sympostum Nicosza, 1979. ——., and BockinG, M. A., in press. — Triassic rocks of the Grants Head district and the post-Permian deformation of the southern New England Fold belt. J. Proc. Roy. Soc. N.S.W. ——, and Cawoop, P. A., 1980. — Olistoliths and debris flow deposits at ancient consuming plate margins: an eastern Australian example. Sed. Geol., 25: 5-22. MAcDONALD, G. A., and Katsura, T., 1964. — Chemical composition of Hawaiian lavas. J. Petrol., 5: 82- 133. McDouca.t, I., and WELLMAN, P., 1976. — Potassium-argon dates on some Cainozoic volcanic rocks from northeastern New South Wales. J. geol. soc. Aust., 23: 1-9. , and WILKINSON, J. F. G., 1967. — Potassium-argon dates on some Cainozoic volcanic rocks from northeastern New South Wales. J. geol. soc. Aust., 14: 225-233. MiyasHiro, A., 1975. — Classification, characteristics, and origin of ophiolites. J. Geol., 83: 249-281. Pratt, G. W., and HERBERT, C., 1973. — A reappraisal of the Lorne Basin. Rec. Geol. Surv. N.S.W., 15: 205-212. QuopLinGc, F. M., 1964. — On traces of native iron at Port Macquarie, New South Wales. J. Proc. Roy. Soc. N.S.W., 97: 81-82. REED, J. J., 1958. — Regional metamorphism in south-east Nelson. Bull. N.Z. Geol. Surv., 60: 1-64. RuNNEGAR, B., 1970. — The Permian faunas of northern New South Wales and the connection between the Sydney and Bowen Basins. J. geol. Soc. Aust., 16: 697-710. SAMUELS, J. (in prep). — Igneous rocks and their associates at Tacking Point, Port Macquarie. VoisEY, A. H., 1939. — The Lorne Triassic basin and associated rocks. Proc. Linn. Soc. N.S.W., 64: 255- 265. Wicks, F. J., and Wuitraker, E. J. W., 1977. — Serpentine textures and serpentinization. Canad. Mineral., 15: 459-488. Proc. Linn. Soc. N.S.W., 104 (4), (1979) 1980 LINNEAN SOCIETY OF NEW SOUTH WALES PRESIDENTIAL ADDRESSES PRINTED IN THE PROCEEDINGS 1926-79 Compiled by T. G. VALLANCE Honorary Editor The convention that a retiring president deliver an address on a subject of his or her interest and expertise was introduced to the Linnean Society of New South Wales by its founding president, Sir William Macleay, at the first annual general meeting, early in 1876. Macleay’s example has been followed and refined by most of his successors. It is a convention that seems to have arisen in the nineteenth century as scientific societies came to elect to presiding office, members who were active in science. The Linnean Society of London, founded in 1788, waited until 1854 and the presidency of Thomas Bell before receiving a scientific anniversary address. Bell’s predecessors, if they attended the anniversary meetings, had been content to report on the society’s affairs and read obituaries of deceased Fellows. An earlier model is the Geological Society of London (founded 1807), of which W. J. Stephens — by all accounts the sponsor of our name, the Linnean Society of New South Wales — was a Fellow. The Geological Society takes pride in a series of printed scientific discourses reaching back to that of W. H. Fitton in 1828. Both these innovative presidents, Bell and Fitton, incidentally, had links with Australia and the Macleay family. The record of the first fifty years of the Linnean Society of New South Wales, compiled by the then Secretary A. B. Walkom and published as a pamphlet in 1925, contains details of early presidents and other officers. It was once hoped to issue a sequel to celebrate our centenary session (1974-5) but the scheme fell victim to the financial problems that have beset the Society during the past decade and show no sign of abating. Some of the information gathered for that sequel, however, ought not be lost and as opportunity offers will be put on record in the Proceedings. A key to the Memorial Series appeared recently (Proc. 103, 1979: 133-4). It is followed now by summary details of presidential addresses printed since 1925. Many of these works have lasting value, as fine examples of scientific exposition and as important statements of original observation, penetrating discussion or historical record. Collectively, they mark significant contributions to science, and not just Australian science, offered in the name of the Linnean Society of New South Wales. Sesston 1925-26 HERBERT JAMES CARTER [1858-1940] Entomology — past and present. Proc. 51, 1926: x-xxix 1926-27 EUSTACE WILLIAM FERGUSON [1884-1927 ] Medical and veterinary entomology in Australia — a review. Proc. 52, 1927: xv-xxviii 1927-28 LAUNCELOT HARRISON [1880-1928] Host and parasite. Proc. 53, 1928: ix-xxxi 1928-29 WILLIAM ROWAN BROWNE [1884-1975] An outline of the history of igneous action in New South Wales till the close of the Palaeozoic era. Proc. 54, 1929: ix-xxxix 1929-30 HENRY SLOANE HALCRO WARDLAW [1889-1970] Some aspects of the adaptation of living organisms to their environment. Proc. 55, 1930: viii-xxv Proc. Linn. Soc. N.S.W., 104 (4), (1979) 1980 294 1930-31 1931-32 1932-33 1933-34 1934-35 1935-36 1936-37 1937-38 1938-39 1939-40 1940-41 1941-42 1942-43 1943-44 1944-45 1945-46 PRESIDENTIAL ADDRESSES EDWIN CHEEL [1872-1951] A review of the myrtle family (Myrtaceae) . Proc. 56, 1931: vi-xxvii THEODORE GEORGE BENTLEY OSBORN [1887-1973] The plant in relation to water. Proc. 57, 1932: vi-xxii CHARLES ANDERSON [1876-1944] The fossil mammals of Australia. Proc. 58, 1933: ix-xxv ARTHUR NEVILLE St GEORGE BURKITT [1891-1959] Some aspects of the vertebrate nervous system. Proc. 59, 1934: v-xxv WILLIAM JOHN DAKIN [1883-1950] The aquatic animal and its environment. Proc. 60, 1935: vii-xxxil WALTER LAWRY WATERHOUSE [1887-1969 ] Some observations on cereal rust problems in Australia. Proc. 61, 1936: v-xxxviii CARL ADOLPH SUSSMILCH [1875-1946 ] The geological history of the Cainozoic era in New South Wales. Proc. 62, 1937: vili-xxxili ERNEST CLAYTON ANDREWS [1870-1948 ] Some major problems of structural geology. Proc. 63, 1938: iv-xl THEODORE CLEVELAND ROUGHLEY [1888-1961 ] A review of the scientific investigation of the fisheries of New South Wales. Proc. 64, 1939: vi-xxvii JAMES MACDONALD HOLMES [1896-1966 | The science of the soil. A stocktaking of present trends. Proc. 65, 1940: vi-xxiv ROBERT HENRY ANDERSON [1899-1969] The effect of settlement upon the New South Wales flora. Proc. 66, 1941: v-xxiii ARTHUR BACHE WALKOM [1889-1976 | The background to William Macleay’s endowment of natural history. Proc. 67, 1942: iv-xv FRANK HENRY TAYLOR [1886-1945 ] Some aspects of the control of disease-carrying insects. Proc. 68, 1943: iv-x ELLIS Le GEYT TROUGHTON [1893-1974] The imperative need for Federal control of post-war protection of Nature. Proc. 69, 1944: iv-xv WILLIAM ROWAN BROWNE [1884-1975 | An attempted post-Tertiary chronology for Australia. Proc. 70, 1945: v-xxiv IDA ALISON BROWN [1900-1976] An outline of the history of palaeontology in Australia. Proc. 71, 1946: v-xviii Proc. Linn. Soc. N.S.W., 104 (4), (1979) 1980 1946-47 1947-48 1948-49 1949-50 1950-51 1951-52 1952-53 1953-54 1954-55 1955-56 1956-57 1957-58 1958-59 1959-60 1960-61 PRESIDENTIAL ADDRESSES 295 ANTHONY REEVE WOODHILL [1900-1965 ] A brief review of progress in the control of some major agricultural insect pests in New South Wales during the period 1920-1945. Proc. 72, 1947: iv-xi GEORGE DAVENPORT OSBORNE [1899-1955 ] A review of some aspects of the stratigraphy, structure and physiography of the Sydney Basin. Proc. 73, 1948: iv-xxxvii LILIAN ROSS FRASER [1908- } A gummosis disease of citrus in relation to its environment. Proc. 74, 1949: v-xvili RUTHERFORD NESS ROBERTSON [1913- ] The last haunts of demons: a comparative study of secretion and accumulation. Proc. 75, 12950: iv-xx DAVID JOSEPH LEE [1915- | _ The problems of insect quarantine. Proc. 76, 1951: v-xix ALAN NEVILLE COLEFAX [1908-1961 ] Variations on a theme. Some aspects of scale structure in fishes. Proc. 77, 1952: viii-xlvi STEPHEN JOHN COPLAND [1907- ]} Recent Australian herpetology. Proc. 78, 1953: v-xxxvil JAMES MATTHEW VINCENT [1911- ] The root-nodule bacteria of pasture legumes. Proc. 79, 1954: iv-xxxii FRANK VERDUN MERCER [1916- ] The water relations of plant cells. Proc. 80, 1955: 6-29. FRANK VERDUN MERCER [1916- | Cytology and the electron microscope. Proc. 81, 1956: 4-19. STEPHEN JOHN COPLAND [1907- |] Australian tree frogs of the genus Hyla. Proc. 82, 1957: 9-108 LILIAN ROSS FRASER [1908- | Virus diseases in citrus in Australia. Proc. 83, 1958: 9-19 SPENCER SMITH-WHITE [1909-__] Pollen development patterns in the Epacridaceae. A problem in cytoplasm -nucleus interaction. Proc. 84, 1959: 8-35 THOMAS GEORGE VALLANCE [1928- | Concerning spilites. Proc. 85, 1960: 8-52 IVOR VICKERY NEWMAN [1902- _ ] Pattern in the meristems of vascular plants. II. A review of shoot apical Proc. Linn. Soc. N.S.W., 104 (4), (1979) 1980 296 1961-62 1962-63 1963-64 1964-65 1965-66 1966-67 1967-68 1968-69 1969-70 1970-71 1971-72 1972-73 1973-74 1974-75 1975-76 PRESIDENTIAL ADDRESSES meristems of gymnosperms, with comments on apical biology and taxonomy, and a statement of some fundamental concepts. * Proc. 86, 1961: 9-59 JAMES MATTHEW VINCENT [1911- ] Australian studies of the root-nodule bacteria. A review. Proc. 87, 1962: 8-38 BERNHARD JOHN FREDERICK RALPH [1916-_ ] Biochemical peculiarities of the larger marine Algae. Proc. 88, 1963: 3 (abstract only) GILBERT PERCY WHITLEY [1903-1975 | A survey of Australian ichthyology. Proc. 89, 1964: 11-127 ELIZABETH CARINGTON POPE [1912- | A review of Australian and some Indomalayan Chthamalidae (Crustacea: Cirripedia) . Proc. 90, 1965: 10-77 DONALD THOMAS ANDERSON [1931- | The comparative early embryology of the Oligochaeta, Hirudinea and Onychophora. Proc. 91, 1966: 10-43. ROGER CHARLES CAROLIN [1929- | The concept of the inflorescence in the order Campanulales. Proc. 92, 1967: 7-26 LAWRENCE ALEXANDER SIDNEY JOHNSON [1925- | Rainbow’s end: the quest for an optimal taxonomy. Proc. 93, 1968: 8-45 THOMAS GEORGE VALLANCE [1928- | Spilites again: some consequences of the degradation of basalts. Proc. 94, 8-51 FRANK VERDUN MERCER [1916- | (Annual Report only) NEVILLE GEORGE STEPHENSON [1916- | (Annual Report only) LAWRENCE ALEXANDER SIDNEY JOHNSON [1925- | Evolution and classification in Eucalyptus. Proc. 97, 1972: 11-29 HAROLD GEORGE COGGER [1935-_ ] (Annual Report only) PETER JOHN TERENCE CATHCART STANBURY [1934- | The role of scientific societies — some suggestions for the future. Proc. 99, 1974: 7-9 THOMAS GEORGE VALLANCE [1928-_ ] Origins of Australian geology. Proc. 100, 1975: 13-43 DARE WILLIAM EDWARDS [1922- | (Annual Report only) *For part I see Phytomorphology, 6 (1), 1956: 1-19; part III was presented, by invitation, to the 10th International Botanical Congress (1964) and printed J. Linn. Soc. London (Botany), 59, 1965: 185:214. Proc. Linn. Soc. N.S.W., 104 (4), (1979) 1980 PRESIDENTIAL ADDRESSES 297 1976-77 BARBARA GILLIAN BRIGGs [1934- | Evolution of the Myrtaceae — evidence from inflorescence structure. PROG MO2 (UIT) OTS Naio25 Or: 1977-78 BARRY DEANE WEBBY [1934- | The Ordovician stromatoporoids. Proc. 103, (1978) 1979: 83-121 +The text printed is an expanded paper, with Dr L. A. S. Johnson as joint-author, related to Dr Briggs’ Presidential Address. Proc. Linn. Soc. N.S.W., 104 (4), (1979) 1980 Index VOLUME 104 Page Acari: Dermanyssidae 183, 221 Anderson, D. T., Cirral activity and feeding in the lepadomorph barnacle Lepas pectinata Spengler (Cirripedia) 147 Benthos of the Kosciusko glacial lakes, by B. V. Timms 119 Bow, N.S.W., Cainozoic geology and fossil fauna 171 Brachiopods, Carboniferous articulate 1 Brachythyris cobarkensts sp. nov. 13 Buchanan, R. A., The Lambert Peninsula, Ku-ring-gai Chase National Park. Physiography and the distribution of podzols, shrublands and swamps, with details of swamp vegetation and sediments 73 Buchanan, R. A., & Humphreys, G. S., The vegetation on two podzols on the Hornsby Plateau, Sydney 49 Bungonia, geology 111, 229 Bungonia Limestone 112, 233 Burrawan serpentinite 281 Calumza (Pisces: Eleotridae) 17 Calumia godeffroye 18 Calumia profunda sp. nov. 19 ‘Camarotoechia’ subtrigonalis sp. nov. 8 Carboniferous articulate brachiopods from eastern New South Wales, by S. Peou 1 Carr, P. F., Jones, B. G., Kanstler, A. J., Moore, P. S., & Cook, A. C., The geology of the Bungonia district, New South Wales 229 Carr, P. F., Jones, B. G., & Wright, A. J., Dating of rocks from the Bungonia district, New South Wales 111 Cartledge, E. G., see Shaw, D. E. Cirral activity and feeding in the lepadomorph barnacle Lepas pectinata Spengler (Cirripedia), by D. T. Anderson 147 Cook, A. C., see Carr, P. F. Darwin and Diprotodon: the Wellington Caves fossils and the law of succession, by K. G. Dugan 265 Dasyurus sp., from Bow 171 Dating of rocks from the Bungonia district, New South Wales, by P. F. Carr, B. G. Jones, & A. J. Wright 111 Devonian tabulate coral 211 Domrow, R., The genus Razllietia Trouessart in Australia (Acari: Dermanyssidae) 183 Domrow, R., A new species of the ulysses group, genus Haemolaelaps Berlese (Acari: Dermanyssidae) 221 Page Dugan, K. G., Darwin and Diprotodon: the Wellington Caves fossils and the law of succession 265 Echinoids, living schizasterid 127 Eelgrass Zsostera capricorni in Illawarra Lake, New South Wales, by M. McD. Harris, R. J. King, & J. Ellis 23 Ellis, J., see Harris, M.McD. Facer, R. A., Hutton, A. C., & Frost, D. J., Heat generation by siliceous igneous rocks of the basement and its possible influence on coal rank in the Sydney Basin, New South Wales 95 Fergusson, C. L., see Powell, C.McA. Flory, R. A., see Wright, A. J. Frost, D. J., see Facer, R. A. Genus Razllietza Trouessart in Australia (Acari: Dermanyssidae), by R. Domrow 183 Geology of the Bungonia district, New South Wales, by P. F. Carr, B. G. Jones, A. J. Kanstler, P.S. Moore, & A. C. Cook 229 Haemolaelaps (Acari: Dermanyssidae) 221 Haemolaelaps sesyphus sp. nov. 222 Harris, M.McD., King, R.J., & Ellis, J., The eelgrass Zostera capricornz in Illawarra Lake, New South Wales 23 Heat generation by siliceous igneous rocks of the basement and its possible influence on coal rank in the Sydney Basin, New South Wales 95 Hervey Range — Parkes area 195 Hoese, D. F., see Larson, H. K. Holacanthopora clarkez sp. nov. 214 Hornsby Plateau, Sydney, vegetation on podzols 49 Humphreys, G. S., see Buchanan, R. A. Hutchings, P., & Rainer, S., A key to estuarine polychaetes in New South Wales 35 Hutton, A.C., see Facer, R. A. Illawarra Lake, Zostera capricorn 23 Inverary Tonalite (new name) 238 Jones, B. G., see Carr, ?. F. Kanstler, A. J., see Carr, P. F. Karikeree Metadolerite (new name) 279 Key to estuarine polychaetes in New South Wales, by P. Hutchings & S. Rainer 35 King, R. J., see Harris, M.McD. Kosciusko glacial lakes, benthos 119 Lambert Peninsula, Ku-ring-gai Chase National Park. Physiography and the Proc. Linn. Soc. N.S.W., 104 (4), (1979) 1980 300 INDEX distribution of podzols, shrublands and swamps, with details of the swamp vegetation and sediments, by R. A. Buchanan 73 Lambian Unconformity, Hervey Range- Parkes area, N.S.W. 195 Larson, H. K., & Hoese, D. F., The species of the Indo-West Pacific genus Calumza (Pisces: Eleotridae) 17 Leitch, E. C., Rock units, structure and metamorphism of the Port Macquarie Block, eastern New England Fold Belt 273 Lepas pectinata, cirral activity and feeding 147 Linnean Society of New South Wales. Presidential addresses printed in the Proceedings 1926-79 293 Record of the annual general meeting 1979. Reports and balance sheets = annexure 1 Living Australian schizasterid echinoids, by K. J. McNamara & G. M. Philip 127 Lumley Adamellite (new name) 238 McNamara, K. J., & Philip, G. M., Living Australian schizasterid echinoids 127 Macropus (Osphranter) sp. cf. M. (Osphranter) woodsi, at Bow 179 Marulan Batholith 113, 238 Morra lethe 144 Moore, P. S., see Carr, P. F. Mount Frome Limestone 211 New Early Devonian tabulate coral from the Mount Frome Limestone, near Mudgee, New South Wales, by A. J. Wright & R. A. Flory 211 New records of Zygnemaphyceae and Oedogoniophyceae (Chlorophyta) from northern New South Wales, byS.Skinner 245 New species of the ulysses group, genus Haemolaelaps Berlese (Acari: Dermanyssidae) , by R. Domrow 221 Oedogoniophyceae 257 Oedogonium wissmanii sp. nov. 261 ?Palorchestes sp. cf. P. parvus., at Bow 178 Peou, S., Some Carboniferous articulate brachiopods from eastern New South Wales 1 Phascolonus sp., at Bow 177 Philip, G. M., see McNamara, K. J. Pisces: Eleotridae 17 Podtsheremia fasciculata sp. nov. 12 Podzols, near Sydney 49, 73 Polychaetes, estuarine, in New South Wales 35 Port Macquarie Block, geology 273 Powell, C.McA., Fergusson, C. L., & Williams, A. J., Structural relationships across the Lambian Unconformity in the Hervey Range-Parkes area, N.S.W. 195 Preliminary report on the late Cainozoic geology and fossil fauna of Bow, New South Wales, by C. G. Skilbeck 171 Presidential addresses 1926-79 293 Proc. Linn. Soc. N.S.W., 104 (4), (1979) 1980 Productoid gen. et sp. nov. 6 Propleopus sp., at Bow 179 Proraster jukesw 143 Protemnodon chinchillaensis, at Bow 179 Quadratia boonienszs sp. nov. 5 Quadratia engeli sp. nov. 3 Raillietia aurzs 187 Raillietia australis 184 Raillietza manfred: sp. nov. 188 Rainer, S., see Hutchings, P. Reevesdale Basalt (new name) 239 Rock units, structure and metamorphism of the Port Macquarie Block, eastern New England Fold Belt, by E. C. Leitch 273 Schizaster (Ova) myorensis sp. nov. 133 Schizaster (Ova) portjacksonensis sp. nov. 140 Schizaster (Schizaster) lacunosus 129 Schizaster (Schizaster) sp. nov. A 131 Schizaster (Schizaster) sp. nov. B 132 Schizophoria subelliptica sp. nov. 9 Shaw, D. E., & Cartledge, E. G., Sporo- bolomycetaceae from Indooroopilly (Australia) and from Port Moresby (Papua New Guinea) 161 Skilbeck, C. G., A preliminary report on the late Cainozoic geology and fossil fauna of Bow, New South Wales 171 Skinner, S., New records of Zygnemaphyceae and Oedogoniophyceae (Chlorophyta) from northern New South Wales 245 Species of the Indo-West Pacific genus Calumiza (Pisces: Eleotridae), by H. K. . Larson & D. F. Hoese 17 Sporobolomycetaceae from Indooroopilly (Australia) and from Port Moresby (Papua New Guinea), by D. E. Shaw & E. G. Cartledge 161 Springponds Granodiorite (new name) 238 Sthenurus sp., at Bow 179 Structural relationships across the Lambian Unconformity in the Hervey Range- Parkes area, N.S.W., by C.McA. Powell, C. L. Fergusson & A. J. Williams 195 Swamps, Lambert Peninsula 81 Tallong Beds 112, 229 Tangerang volcanics 112, 236 Thrumster Slate (new name) 278 Thylacoleo crassidentatus, at Bow 177 Timms, B. V., The benthos of the Kosciusko glacial lakes 119 Touchwood Formation (new name) 276 Troposodon sp. cf. T. bluffenszs, at Bow 179 Vegetation on two podzols on the Hornsby Plateau, Sydney, by R. A. Buchanan & G.S. Humphreys 49 Watonga Formation (new name) 274 Wellington Caves, fossils and the law of succession 265 Williams, A.J., see Powell, C.McA. Wright, A. J.,, & Flory, R. A., A new Early Devonian tabulate coral from the Mount Frome Limestone, near Mudgee, New South Wales INDEX 301 211 Wright, A. J., see Carr, P. F. Wylora Quartz Gabbro (new name) 238 Zostera capricorni, in Illawarra Lake 23 Zygnemaphyceae 246 Proc. Linn. Soc. N.S.W., 104 (4), (1979) 1980 ADVICE TO AUTHORS The Linnean Society of New South Wales publishes in its Proceedings original papers and review articles dealing with biological and earth science. Papers of general significance are preferred but the Proceedings also provides a medium for the dissemination of useful works of more limited scope. Manuscripts will be received for assessment from non-members as well as members of the Society though non-members must communicate their works through a member. Subject to acceptance, a member’s paper may be given priority in publication over that of a non-member. Manuscripts (originals and two copies of text and illustrations) should be forwarded to the Secretary, Linnean Society of New South Wales, 35-43 Clarence Street, Sydney, Australia, 2000. _ Authors who are members of the Society are supplied with 25 free offprints of their papers after publication. Additional copies may be purchased, provided an order is placed when the corrected proofs are returned to the Honorary Editor. Donations towards the cost of publishing papers are always most welcome. In the case of lengthy papers or those with many illustrations or tables, contributions from authors, and especially non-member authors, may be requested at the discretion of Council. 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The general design of a paper should follow the scheme: (1) Title and author’s name — all in capitals. (2) A concise Abstract, complete in not more than 200 words, indicating the scope of the paper. Authors should adopt the lay-out used in this issue of the Proceedings, including details of postal address but leaving spaces for editorial] insertions. (3) Main text. Footnotes should be avoided. The text may be divided into sections introduced by short headings set out as in this issue. (4) Acknowledgements, if any. (5) References. These should be cited in the text by author’s name and date, e.g., Bullough (1939) or (Bullough, 1939) according to the context and listed alphabetically by authors under References thus: BuLLoucu, W. S., 1939. — A study of the reproductive cycle of the minnow in relation to the environment. Proc. zool. Soc. Lond., Ser. A, 109: 79-108. Titles of periodicals should be abbreviated as in the World List of Scientific Periodicals. 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Figures must therefore be designed to yield clear images within the limits of a single page. Close attention should be paid to the matter of scale on figures. Where possible add a linear scale (with the dimension clearly marked) to the figure rather than trust that a statement of scale in the caption will be correct after the plate-maker and printer have finished their jobs. All line drawings should be in India ink on a suitable surface, such as Bristol board, tracing linen or plastic film. In general, however, the platemaker prefers to work from good quality, glossy photographs rather than originals of various sizes. Authors are urged to supply such photographic reproductions which, if made to a scale appropriate to the size of a printed page, will show whether ornament and lettering can be read in the final print. All photographs, whether for half-tone or line illustrations, should be high-contrast, glossy prints. Each illustration should be identified (author’s name, Fig. no. and orientation) in pencil on the back. Tables should be submitted in a clear format on separate sheets. Like illustrations, they should be designed to fit a single page of the journal. PROCEEDINGS of LINNEAN SOCIETY OF NEW SOUTH WALES VOLUME 104 Issued 16 January 1981 CONTENTS: NUMBER 3 161 D. E. SHAW and E. G. CARTLEDGE 171 183 195 2h 221 229 245 265 273. 293 299 Sporobolomycetaceae from Indooroopilly eal and from Port Moresby (Papua New Guinea) C. G. SKILBECK A Preliminary Report on the Late Cainozoic Geology and Fossil Fauna of Bow, New South Wales R. DOMROW ‘ The Genus Raillietia Trouessart in Australia (Acari: Dermanyssidae) C. McA. POWELL, C. L. FERGUSSON, and A. J. WILLIAMS Structural Relationships across the Lambian Unconformity in the Hervey Range-Parkes Area, N.S.W A. J. WRIGHT, and R. A. FLORY A New Early Devonian Tabulate Coral from the Mount Frome Limestone, near Mudaee, New South Wales NUMBER 4 R. DOMROW A New Species of the u/ysses Group, Genus Haemolaelaps Berlese ea Dermanyssidae) P. F. CARR, B. G. JONES, A.J. KANSTLER, P. ‘Ss MOORE and A. C. Cook The Geology of the Bungonia District, New South Wales S. SKINNER New Records of ZB agemannyer and Oedogoniophyceae (Chlorophyta) from northern New South Wales K. G. DUGAN Darwin and Diprotodon: The Wellington Caves Fossils and the ba of Succession E. C. LEITCH. Rock Units, Structure and Metamorphism of the Port Macquarie Block, eastern New England Fold Belt LINNEAN SOCIETY OF NEW SOUTH WALES Presidential Addresses printed in the Proceedings 1926-79 INDEX to Volume 104 Printed by Southwood Press Pty Limited, 80-92 Chapel Street, Marrickville 2204 7 uu . v4 y 4 - re } ‘ i ‘ 4 ” . y , « i} if i i i | \ : aw ) ee y mac ~ FO “) 1 = ay it \ 4 i) \, oa ‘ dt “xa vi YT ana Sedan ine ) ‘ i -$ oe) my mh \ . a ‘ ‘ f " 1 b * | | | 4 : ee i BAI fc f al PI of - sw ; ‘ * Ryd) . ( | mk ad Pa iY - _ r . * * id ; Ni ; 1 : . ‘ es ; ~ "4 Bis ” in ng, * 2 al Wie fl * | | * . Ten NOR 'MBL/WHOI LIBRARY MN WH LAET H 1 meg dit hi se ce ret 2! i vey 8 a Feasts OP» ag ty ih pol a tok Le i yete ft ; er cee Se, ae Pine Pet seab8e ah eore sy sfiahy at ei Mat oR READ nyt at pained S hy : ee %,