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Hy H Hy | mK ey ony via f ze) “i is ae evasscaur a, cP ac at alg ii | i i ly i t | | ih : di a sa a Al aft Hew Ve} wh nab I. iT Ga al Hi ib a fees a Ee “hy oe aa eS cS. romnsat ‘coe ay dl > Oe Ml Ge & pe | e ) goee, O _ Oo foots = Bs % a i Aya “eae a a pew \ Ae aE | as ae fs) gh fos Ry ‘ly, 4 st ea Ag £3, ph eS es a Fc al? aa ee ee : det | ake ed femntacinaentttt | BS as ay HOS “3 Aol rie] H sa oh lia “ie arr San P32, Ey ~~. eet ae a 2 < d ne u wm LH 18 hn tre! ong ae ‘fi Mal Pepe 2a Se te ae ROT NEE I se a ree Sorpebun ast oy “ihn al Se ih h itl “yt t ro eat a ae ott fg al AN #- let We 1 JOURNAL AND PROCEEDINGS OF THE ROYAL SOCIETY OF NEW SOUTH WALES VOLUME 97 1963-64 PUBLISHED BY THE SOCIETY, SCIENCE HOUSE, GLOUCESTER AND ESSEX STREETS SYDNEY Royal Society of New South Wales OFFICERS FOR 1964-1965 Patrons His EXCELLENCY THE GOVERNOR-GENERAL OF THE COMMONWEALTH OF AUSTRALIA, THE RIGHT HONOURABLE VISCOUNT De L’ISLE, V.c., P.c.,.G.¢.M.Gi) GiG.V.0.7 se-St.J- His EXCELLENCY THE GOVERNOR OF NEW SouTH WALES, LIEUTENANT-GENERAL SIR ERIC W. WOODWARD, k.c.M.G., K.C.V.O., C.B., C.B.E., D.S.O. President J. W. HUMPHRIES, B.se. Vice-Presidents Cc. L. ADAMSON, B.Sc. W. H. G. POGGENDORFF, B.Sc. Agr. H. H. G. McKERN, M.sc. W. B. SMITH-WHITE, o.a. Honorary Secretaries A. H. LOW, Ph.p., M.Sc. ALAN A. DAY, B.sc., Ph.D. Honorary Treasurer H. F. CONAGHAN, msc. Members of Council IDA A. BROWNE, D-sc. J. MIDDLEHURST, m.sc. R. M. GASCOIGNE, ph.p. J. W. G. NEUHAUS, A.s.T.c. H. G. GOLDING, M.sc. A, REICHEL jy mise: Re Je W.. LE FEVRE, p.Sc., F.R.S., F.A.A. R. L. STANTON, Ph.p. A. KEANE, Ph.p. A. UNGAR, Dr.ing. NOTICE The Royal Society of New South Wales originated in 1821 as the ‘‘ Philosophical Society of Australasia’ ; after an interval of inactivity it was resuscitated in 1850 under the name of the “ Australian Philosophical Society ’’, by which title it was known until 1856, when the name was changed to the ‘‘ Philosophical Society of New South Wales’’. In 1866, by the sanction of Her Most Gracious Majesty Queen Victoria, the Society assumed its present title, and was incorporated by Act of Parliament of New South Wales in 1881. CONTENTS Part 1 Palaeontology : A Lower Carboniferous Fauna from Lewinsbrook, New South Wales. John Roberts Part 2 Astronomy : Minor Planets Observed at Sydney Observatory during 1962. W. H. Robertson Geology : Depositional Environments and Provenance of Devonian and Carboniferous Sediments in the Tamworth Trough, N.S.W. K. A. W. Crook Petrology in Relation to Road Materials. Part Il: The Selection of Rock bE Rowe: snaking in Australia, with special reference to New South Wales. £. J. Minty The Geology of the Carroll- Ee aes Area of New South Wales. A. H. Vo aie ila K. L. Williams Part 3 Geology : The Eclogite-bearing Basic ae ee at a Hill near ee New South Wales. Jj. F. Loverig .. Mineralogy : On Traces of Native Iron at Port Macquarie, New South Wales. F. M. Quodling Palaeontology : Lepidophloios and ee dik from the Lambie Pome at Mount Lambie, N.'S.W. R. M. Mackay Devonian Trilobites om the + Wellington -Molong District i nee oan Wales. D. ro Sirusz oe : cy aus Part 4 Astronomy : Precise Observations of Minor Planets at ae Seo ee 1961 and 1962. W.H. Robertson . 7” = Geology : Quaternary Sedimentation by Pricr Streams on the Riverine Plain, South-west of Griffith, NESW... S. Pels Surveying : Some Applications of Aerial ir ae cae to the Solution of a oppereh as and C sea aa Eroblems. A: D. Albam Proceedings of the Society, 1962-63 33 4] 55 65 13 81 83 91 99 107 117 121 250 CONTENTS Part 5 Astronomy : Positional Astronomy. The Donovan Astronomical Lecture for 1963. H. Wood Geology : Our Permian Heritage in Central-Eastern New South Wales. The Clarke Memorial Lecture for 1961 Geology and Sub-surface Waters of the Jurassic Walloon Coal Measures in the Eastern Portion of the Coonample Basin, N.S.W. J. Rade Mathematics : On the Gibbs’ Phenomenon in n-Dimensional Fourier Transforms. /. L. Griffiths Palaeontology : Lower Cretaceous Sporomorphs from the Northern Part of the Clarence Basin, New South Wales. J. Rade i Part 6A Astronomy : Minor Planets Observed at Sydney Observatory during 1963. W. H. Robertson Occultations Observed at Sydney Observatory during 1962-63. K. P. Sims History of Science : James Dwight Dana in New South Wales, 1839-1840. Ann Mozley Palaeontology : Lower Carboniferous Faunas from Wiragulla and Dungog, New South Wales. J. Roberts Part 6B Proceedings of the Society, 1963-64 Index Dates of Issue of Separate Parts Part 1: December 24, 1963 Part 2: April 3, 1964 Part 3: April 21, 1964 Part 4.7, july 2, 1904 Part, 52. july 39; 1964 Part 6A: February 11, 1965 Part 6B: July 28, 1965 135 163 175 185 193 Royal Society of New South Wales ti s va \ e ve Gee £ - 7 4s "Bee J "TS i OFFICERS FOR 1963-1964 Patrons - . cain ss Ra His EXcELLENCY THE GOVERNOR-GENERAL OF THE CoMMONWEALTH OF Ageeoiice THE RicHT HONOURABLE VISCOUNT De L’ISLE, v. C., P.C., G.C.M.G., G.C.V.0., K.St. J. . His EXcELLENCY THE GOVERNOR oF NEw SouTH WALES, . Keil rash LIEUTENANT-GENERAL ah BRIC W. WOODWARD, K.ciM.G., K.C.V.0., C.B., C.B.E., DSS. 9. Peete. 4g) President Rs Wc ane H. H.'G. McKERN, misc. * ‘offs Naa ORIN NETY CRP RE (tat y “f GPS) 0h he “ta ir - *) Vice-Presidents ce ie rng J. L. GRIFFITH, B.a., M.sc. W. H, G. POGGENDORFF, B.SC.ART. pe ae R. J. W. Le FEVRE, pisc., F.RS., F.A.A. W. B. SMITH-WHITE, ma, | ey e : Hon. Secretaries | ik i a ¥ Deal % Ge A, H. LOW, Phv., Msc. hee 8 TENN DAY, Ie be. ph aor ani PM lg Hon. Treasurer ig Ge he ca ap RE Ks: C. L. ADAMSON, B.se. : Members of Council ‘ IDA A. BROWNE, D.sc. | J. W. HUMPHRIES, Biseut b ee H. F. CONAGHAN, M.se. - Ao KEANE, Ph.p. Pomp nie th A. G. FYNN, B.Sc. ) J: MIDDLEHURST, M.Sc. ae N. A. GIBSON, Ph.p. R. L. STANTON, Ph.p. H.. G. GOLDING, m-se. . A. UNGAR, Dring. — ‘ s ae 4 ae oh ‘ets ae me oo a yt "4 Rte . Siaps, F7 wee 4 pie i iy v : yor ata wp bre Wig a ty ieee 4 ANON BAY Ve adh | i ay Ge AB y Mil oa ‘ The Royal Society of New South Wales originated in 1821 as the “ Philosophical Society tise OE Bay SE of Australasia "’ ;, after an interval of inactivi At was resuscitated i in 1850 under the name of the “ Australian Philosophical Society ””, by which title it was known’ until 1856; when the name was changed to the “’ Philosophical Society of New South Wales ’’. In 1866, by the sanction of Her ~ Most Gracious Majesty Queen Victoria, the Society assumed its resent title, and was sal sak dn Si by Act of Parlhament of New. South Wales in 1881. Raa he Re ae > ane * ited Journal and Proceedings, Royal Society of New South Wales, Vol. 97, p. 1-29, 1963 A Lower Carboniferous Fauna from Lewinsbrook, New South Wales JOHN ROBERTS Department of Geology, Umversity of New England, Armidale, N.S.W.* Apstract—An Upper Tournaisian fauna from the Bingleburra Formation, Lewinsbrook, N.S.W., is described, including three new genera—an auloporoid coral Bibucia, the brachiopod Acuminothyris and the trilobite Conophillipsia. Fourteen new species described are: Bzibucia tubiformis, Fenestella brownet, F. gresfordensis, F. wilsont, Productina globosa, Pustula multispinata, Acuminothyris triangularis, Brachythyris elliptica, ? Delthyvis paptilionis, ? Thomasaria voiseyt, Cleiothyridina segmentata, C. squamosa, Streblochondria obsoleta, and Conophillipsia brevicaudata. Streptorhynchus spinigera (McCoy) is redescribed. The palaeoecology and affinities of the fauna are discussed. Introduction The study of the palaeontology of the lowest Carboniferous beds in the Hunter Valley, New South Wales, has been almost entirely neglected since the last century. The present work is the first detailed examination of the Lewinsbrook fauna. The first worker to examine the fauna was McCoy (1847) who described Orthis australis McCoy, Spirifer lata McCoy, Orthis striatula Schlotheim, Productus antiquatus Sowerby and Productus setosus Phillips from material collected by the Rev. W. B. Clarke. Campbell (1957), who redescribed Rhipidomella australis (McCoy) and Asyrinxia lata (McCoy) on _ topotype material, has been the only other worker to collect from Lewinsbrook. The Lewinsbrook localities are the lowest known fossil horizons in the Bingleburra Formation, the oldest formation exposed in the Gresford-Dungog district. The horizons do not crop out elsewhere in the region studied by the author ; asa whole the fauna, on present-day knowledge, is unique in the Carboniferous of New South Wales. All locality numbers in the figures and text of this paper refer to The University of New England Collection. Grid references are from the Dungog 1 Mile Military Sheet. Specimen numbers, unless otherwise stated, refer to The University of New England Palaeontological Collection. STRATIGRAPHY Lewinsbrook is situated 2-5 miles south-east of the town of Gresford and approximately 40 miles north-east of Newcastle (Text-fig. 1). The geology of the Gresford district has been * Present address: Geological Branch, Bureau of Mineral Resources, Canberra, A.C.T. A described in a previous paper (Roberts, 1961). Text-figure 2 illustrates the stratigraphic nomen- clature of the formations described in this work. The following information is a brief summary of the stratigraphy of the Gresford district. The Bingleburra Formation (approximately 3,000 feet in thickness) consists of mudstones, siltstones, oolitic and crinoidal limestones and interbedded sandstones and conglomerates and is overlain by the Ararat Formation (1,500 feet in thickness). This formation is composed of calcareous tuffaceous sandstones with minor mudstones and oolitic and crinoidal limestone lenses. Following Ararat sedimentation marine con- ditions continued without interruption in the north of the area. The Bonnington Formation Gresford * Lewinsbrook Newcastle .¢ ‘. Co 2° “Miles TEXT-FIG. | Locality map. 9 JOHN ROBERTS Areg Area _ \~ Stage Se Flagstoff Sandstone Bonnington Formation Ararat Formation Wiragulla ie Beds Formation Bingleburra |. Bingleburra Formation Formation ie) Marine Formations 64 Non Marine Formations TEXT-FIG. 2 Stratigraphic nomenclature of formations in the Gresford District. (400 feet in thickness) consisting of siltstone and mudstone, underlies the coarse tuffaceous Flagstaff Sandstone (5,500-++ feet in thickness). To the south, following the deposition of the Ararat Formation, conditions changed in parts to a non-marine environment due to the uplift of a narrow belt stretching from Greenhills to Mt. Ararat (Roberts, 1961). Away from the influence of the uplift, for example at Wiragulla near Dungog, a thin marine mudstone and siltstone sequence (Wiragulla Beds) interfingers between the Ararat Formation and the non- marine Wallaringa Formation. The Wallaringa Formation (950 feet in thickness) comprises the Wallarobba Conglomerate Member and coarse tuffaceous sandstones. It is overlain by the Gilmore Volcanics, the Mt. Johnstone Beds (Sussmilch and David, 1920) and rocks of the Glacial “‘ Stage ’’ (Osborne, 1922). LEWINSBROOK LOCALITIES AND STRATIGRAPHIC SECTION The Lewinsbrook-Trevallyn fault block contains the majority of the important fossil horizons in the Gresford district and occurs in an area of considerable structural com- plexity to the east of the Camyr-Allyn fault. Text-figure 3 is a diagrammatic stratigraphic section showing lithologies and the stratigraphic relationships of the fossil localities. The L.50 and L.203 horizons have not been located in the Lewinsbrook-Trevallyn section, but are assigned to their present position on lithological and palaeontological grounds as their faunal com- position is intermediate between that of the Lewinsbrook and Trevallyn horizons. ‘This stratigraphic section differs from the type section of the Bingleburra Formation (Roberts, 1961) found seven miles to the north on the western limb of Lewinsbrook Syncline due to the bank-type oolitic limestone facies in the type area giving way southwards to a more clastic environment containing large con- glomerate lenses. The Lewinsbrook fossil localities in super- positional order are : L. 86 46059883 E2n7 46069882 L.216 46079882 L.215 46089882 L.215 is characterized by a rich assemblage of Schizobhoria cf. resupinata (Martin) in a closely jointed grey siltstone. L.216, approximately 15 feet above L.215, is in a dark grey siltstone containing abundant Rhipidomella australis (McCoy). L.217, a spiriferoid horizon, three to four feet above L.216, contains Asyrinxia lata (McCoy), Brachythyris elliptica n.sp. and Acumzinothyris triangularis n.sp. in a dark grey siltstone. L.86, approximately 20 feet above L.217, contains crowded fragments of polyzoa and small brachiopods in a pale brown mudstone. THE FAUNA OF THE LEWINSBROOK LOCALITIES The following faunal list contains all identi- fiable forms collected from Lewinsbrook during the current investigation. The author has spent a total time of approximately one week collecting at Lewinsbrook and holds the opinion LOWER CARBONIFEROUS FAUNA FROM LEWINSBROOK, N.S.W. E233 Trevallyn L270 L208 Trevallyn Conglomerate Gresford L203 Quarry L218 LSO Gresford Conglomerate Glenroy Conglomerate peongientarate L86 Lewinsbrook L 217 L216 | sandstone L215 | siltstone aR Oo mudstone oO Lewinsbrook = : limestone Conglomerate fossil horjzon TEXT-FIG. 3 Diagrammatic stratigraphic column of the Bingleburra Formation, Lewins- brook- Trevallyn fault-block, showing lithologies and fossil horizons. For the sake of clarity the separation of fossil horizons is exaggerated. 4 JOHN ROBERTS that this list is likely to represent at least 85 per cent of the total fauna. Forms described in the text are distinguished by an asterisk. The following species are common to all four localities : *Fistulamina mornata Crockford *Gontocladia laxa (de Koninck) Rhipidomella australis (McCoy) Schizophoria cf. vesupinata (Martin) Eomarginifera cf. paradoxus (Campbell) Leptagoma ct. analoga (Phillips) *Brachythynis elliptica n. sp. Unispirifer striatoconvolutus (Benson and Dun). L.86 Fauna *Bibucia tubsformis n. gen. and sp. *Cladochonus tenmecollis (McCoy) *Cladochonus sp. Streblotrypa parallella Crockford Ramipora sp. *Ptilopora koninckt Crockford *Fenestella brownei n. sp. * Fenestella gresfordensis n. sp. *Fenestella wilsont n. sp. Orbiculoidea sp. Lingula sp. Schuchertella sp. *Streptorhynchus spinigera (McCoy) *Pustula multispinata n. sp. * Productina globosa n. sp. Marginatia sp. Fluctuaria sp. *Acuminothyris triangularis n. gen. and sp. *Cletothyridina segmentata n. sp. *Clerothyridina squamosa 0. sp. Cletothyridina sp. Athyris sp. *? Delthyris papilionis n. sp. Asyrinxia lata (McCoy) *? Thomasaria voiseyt n. sp. Kitakamithyris sp. Ptychospira sp. Dielasma sp. **“ Camarotoecma’’ sp. A. Stenoscisma sp. ? Girtypecten sp. *Streblochondria obsoleta n. sp. *Conophillipsia brevicaudata n. gen. and sp. L.217 Fauna Kyrotovia sp. *Productina globosa n. sp. *Acuminothyns triangularis n. gen. and sp. Dvielasma sp. Athynis sp. Asyrinxta lata (McCoy). L.216 Fauna Orbiculoidea sp. L.215 Fauna *Cladochonus tenuicollis (McCoy) *Cladochonus sp. Ramipora bifurcata Crockford Streblotrypa parallella Crockford Krotovia sp. *Cletothyridina squamosa N. sp. *Acuminothynis triangularis n. gen. and sp. *? Thomasania voiseyi n. sp. For local correlation it is significant to note that the following species are restricted to the Lewinsbrook horizons : Bibucia tubtformis n. gen. and sp. Fenestella browne n. sp. Fenestella gresfordensis n. sp. Fenestella wilson n. sp. Pustula multispinata n. sp. ? Thomasaria voiseyi n. sp. Conophillipsia brevicaudata n. gen. and sp. Streblochondria obsoleta n. sp. Productina globosa n.sp and_ ? Delthyris papilionis n. sp. occur in the Lewinsbrook and L.50 Gresford Quarry horizons and Acumino- thyris triangularis n. gen. and sp. is recorded from Lewinsbrook, L.50 Gresford Quarry and L.233 Trevallyn. Most other forms appear to be longer ranging. TYPE OF PRESERVATION Most of the specimens are preserved as internal and external moulds, the fine-grained sediment infilling the finest features of the shell ornament and even the zooecia of polyzoa. Original shell material still remains in the unweathered portions of the L.215—-L.217 localities. PALAEOECOLOGY From a study of the faunal lists it is obvious that the L.215-—L.217 localities do not have as diverse a fauna as L.86. These three localities all occur in bedded siltstone. The following points relevant to the palaeo- ecology have been noted in the three lower localities (L.215-L.217). They are by no means conclusive because of the restricted outcrops. (1) The long spines of LEomarginifera cf. paradoxus (Campbell) frequently remain unbroken, indicating a quiet environment. (2) Pedicle valves of Schizophoria ct. resupinata (Martin) are generally oriented in a lower or ventral position. LOWER CARBONIFEROUS FAUNA FROM LEWINSBROOK, N.S.W. 5 (3) A common position of Acuminothyris triangularis in the L.217 locality is with its hinge line lying flat on the bedding plane of the sediment, apparently in its living position. (4) Fragmentary material is relatively un- common and is restricted to minor crinoidal debris associated with L.215. (5) Fragmentary worm burrows penetrate much of the siltstone. The above evidence suggests that the shells may be in approximate positions of growth, that current activity was minimal, and that the bottom sediment was apparently a suitable habitat. L.86, with a richer and more diverse fauna, shows more satisfactory evidence regarding the conditions existing during its accumulation. (1) Many brachiopod shells are dissociated, presumably as a result of current action. (2) The great majority had been killed by a boring organism, probably a_ predatory gastropod, which bored vertically through the shell into their adductor muscles (see Pl. 3, fig. Ta, Streptorhynchus spinigera McCoy). (3) Fenestrate polyzoa and Gomntocladia are usually broken, have fragmentary margins, and lie flat on the bedding planes. (4) All productids, including the common genera Productina, Pustula and Eomarginifera, have broken spines. (5) Many shells are distorted, probably due to compaction of sediment during lithification. (6) There is a large amount of fragmentary material, particularly disarticulated crinoid stems and plates, polyzoa and tabulate coral debris. As most shells are not worn, it appears that the fauna had been transported a short distance before burial. The muddy conditions existing during the deposition of the sediment at L.86 would not, in my opinion, have provided a suitable bottom environment for such a rich fauna, as clear water would have been essential for the growth of the polyzoan and coelenterate members of the assemblage. The mass of fragmentary material indicates substantial current activity at the time of deposition. THE AGE OF THE FAUNA The Lewinsbrook fauna is dated as Upper Tournaisian. Two distinctive species from this fauna, Productina globosa and ? Thomasaria cf. voiseyt, have been collected from the Werrie Basin, N.S.W., where they occur in association with an Upper Tournaisian (probably Cu II,) goniatite fauna at the base of the Merlewood Section (Delépine, 1941 ; Campbell and Engel, in press). The Upper Tournaisian age is supported by the following evidence. Productina globosa morphologically resembles P. sampsont (Weller) from the Fern Glen Formation, Missouri; the Caballero and Lake Valley Formations, New Mexico ; the Rockford Formation, Indiana; and the Kinderhook of Iowa (Muir-Wood and Cooper, 1960). The Chouteau Limestone and its equivalents, for example the Rockford Limestone, have been dated as Upper Tournaisian (Cu II,) by Voges (1960) and Collinson e¢ al. (1962). The latter workers considered the Fern Glen Formation to be Lower Viséan (probably Cu II,) in age. It is also highly significant that the Upper Tournaisian goniatite assemblage from the Rockford and Chouteau Limestones is very close to that from the lower parts of the Carbon- iferous sequence in the Werrie Basin (Miller and Collinson, 1951) from where this species has been collected. Brachythynis elluptica is morphologically close to B. pinguis (Sowerby) which occurs in the Viséan of Great Britain and in the Upper Tournaisian (Tn3p) and Lower Viséan in Belgium. The trilobite Conophilliipsia brevicaudata suggests a slightly older age because of its morphological similarity with C. labrosa (Weber) and C. kazakensis var. paucicostata (Weber). The latter species occur in the Lower Tournaisian Kassin Beds and possibly in the Transition Beds of the Kirgiz Steppe of Russia (Weber, 1937). The general form of the colonies and the arrangement of the branches and fenestrules of the fenestrate polyzoa, viz. Fenestella browne and F. wilson1, resemble certain members of the fauna described by Koenig (1958) from the Chouteau Group of Central Missouri. RELATIONSHIP TO OTHER FAUNAS As previously mentioned, the fauna from the base of the Namoi Formation in the Werrie Basin, N.S.W., contains two diagnostic species, Productina globosa and ? Thomasana cf. votseyt, in common with the Lewinsbrook fauna. These species occur in mudstones of the Namoi Formation at Keepit Dam on the Namoi River, approximately 500 feet above the Rangari Limestone, and on a comparable horizon in the Merlewood Section. The Lower Carboniferous fauna described by Maxwell (1954) from Mt. Morgan, Queensland, approximately 1,000 miles north of the Gresford 6 | JOHN ROBERTS district, contains two distinctive species which may be related morphologically with forms in the Lewinsbrook fauna. The species Dimegelasma kennedyense may be close to that referred to ? Thomasaria voisey1, and Brachy- thynis cf. pingums (Sowerby) is possibly similar to B. ellptica. Closer comparison is hampered by the poor preservation of the Queensland specimens. Schizophoria cf. resupinata (Martin) and Leptagonza cf. analoga (Phillips) are common to both faunas. Closest general relations with overseas faunas appear to be with the Kinderhook of America, where Leptagonia analoga (Phillips) resembles L. cf. analoga (Phillips), Schizophoria post- triatula Weller is similar to S. cf. resupinata (Martin) and Pvroductina sampson (Weller) resembles P. globosa. Tournaisian faunas from the Moscow Basin (Sarycheva and Sokolskaya, 1952), the Donetz Basin (Rotai, 1931) and the Kousnetzk Vasin (Tolmachoff, 1924) have no similarities with the Lewinsbrook fauna except for very common forms such as Leptagonia analoga (Phillips). Morphologically related species in_ the European Lower Carboniferous are, in general, long ranging and cannot indicate a precise age. Umspirifer striatoconvolutus Benson and Dun is closely related morphologically to S#fuirifer tornacensis de Koninck, which ranges throughout most of the Tournaisian. Schizophoria cf. vesupinata (Martin) and Leptogonia cf. analoga (Phillips) are virtually indistinguishable from the European species and Riipidomella australis (McCoy) is considered by Campbell (1957) to be very close to R. michelina (L’Eveillé). In Europe, S. resupinata, L. analoga and R. michelint range throughout the Dinantian. ACKNOWLEDGMENTS This work was undertaken at the Department of Geology, University of New England, ‘Armidale, New South Wales. The author is grateful to Dr. K. S. W. Campbell for his constant advice on all aspects of the work and to Professor A. H. Voisey for making available all the facilities of his department. In addition, the author wishes to thank Dr. R. Goldring, of the University of Reading, England, for his interest in the problem and for his Opinions regarding the trilobite described below. This paper was finalized at the University of Western Australia. Thanks are due to Dr. P. J. Coleman for his critical reading of the manuscript and to Mr. K. Bauer for assistance with the photography. Finance was provided by a Commonwealth Post-Graduate Fellowship, held at the University of New England. SYSTEMATIC PALAEONTOLOGY Coelenterata Order TABULATA Milne Edwards and Haime 1850 Family AULOPORIDAE Milne Edwards and Haime 1851 Genus BIBUCIA n. gen. Type SPECIES: Buibucia tubtformis n. sp. DiaGnosis: Biserial stem-like colony with two separate, opposing, alternating rows of corallites connected by mural pores ;_ trumpet- shaped corallites bud from the distal portion of the parent corallite ; branches occur at irregular intervals and arise from a second bud on proximal portions of parent corallite ; epithecal tissue between corallites probably lamellar calcite. REMARKS: The only auloporoid resembling this genus is the North American Silurian genus Bainbridgia Ball and Grove (in Hill and Stumm, 1956, p. F470, fig. 355, 11a—b). The corallites of Bainbrndgia are not connected by mural pores and have a different shape from those in Brbucia. The name Bzbucia is taken from the Latin “ bucina’’, a trumpet, and refers to the two rows of trumpet-shaped corallites. Bibucia tubtformis n. sp. Plate 3, figs. 8-9 Diacnosis: Branches always arise from immediately beneath an aperture; corallites elongate, trumpet-shaped ; apertures 0-4 mm. in diameter, with small lip-like projections ; they are inclined at approximately 30° to the main stem; distance between apertures 2-2-5 mm. DESCRIPTION: The colony consists of a main biserial stem giving rise to unconnected, slightly inclined biserial branches at irregular intervals ; the colony is probably an erect ramose structure with branches arranged both in the same plane as the corallites and also possibly at 90° to this ; one broken branch normal to the plane of the corallites has been observed. The exterior is smooth and devoid of ornament. Alternating corallites are arranged in two separate opposing rows on either side of the stem; corallites increase by budding from immediately below the calice on the distal portion of the parent corallite. Corallites are LOWER CARBONIFEROUS FAUNA FROM LEWINSBROOK, N.S.W. 7 TEXT-FIG. 4 Bibucta tubiformis n. sp. (X94), showing the shape of the corallites (black) and mural pores. The system of budding of the corallites at branching is obscure. This diagram was constructed from the specimen in fig. 9, Plate 3. thin, elongate, trumpet-shaped, tubular for nearly three-quarters of their length and then expand towards the aperture. The apertures are round, inclined at approximately 30° to the main stem and have a small lip-like projection on their proximal margins. The diameter of the apertures is 0-4 mm. and the distance between the apertures (on same side of colony) 2-2-5 mm. The arrangement of tabulae in the corallites is unknown. Mural pores occur immediately below the calice of one corallite and on the mid-portion of the other and link the two rows (Text-fig. 4). Branching takes place from the proximal portion of a corallite by the formation of two buds. The new branch always arises from immediately beneath an aperture. REMARKS: The author knows of no other species comparable with Bibucia tubiformis. Text-figure 4 was constructed from a specimen having infilled zooecia and the sclerenchyma dissolved. The specific name tubiformis refers to the trumpet-shaped corallites. OCCURRENCE: This genus and known only from L.86 Lewinsbrook. MATERIAL: F.5366—F.5372. Holotype F.5366, paratype F.5370. species 1s Genus CLADOCHONUS McCoy 1847 TYPE SPECIES: Cladochonus tenumcollis McCoy, 1847, Ann. Mag. Nat. Hist. 20, p. 227, pl. 11, fig. 8. DIAGNOSIS : p. F472). See Hill and Stumm (1956, Cladochonus tenuicollis McCoy Plate 1, fig. 4 REMARKS : C. ¢enuicollis has been revised by Hill and Smyth (1938). This material differs from the type specimens (Hill and Smyth, pl. 23, fig. 1) insofar as the distal portion of the calice in front of the branch on each corallite is shorter. To the best of my knowledge this is the first description and illustration of a reptant ring of Cladochonus tenurcollis. Four proximal corallites forming the reptant ring are compressed and much shorter than those on the branches ; each proximal corallite gives rise to a major branch of the colony. MEASUREMENTS (in mm.) : Branching Corallites Width Length Proximal Rim of calice 12-13 2°5-2-7 Proximal ring corallites Width Length Proximal Rim of calice 9-10 2-5 5 OCCURRENCE: This species occurs at L.215 and L.86 Lewinsbrook, L.50 Gresford Quarry and L.233 Trevallyn. MATERIAL: F.5374. Cladochonus sp. Plate 1, figs. 1-3 DESCRIPTION: The shape of the colony is unknown. Corallites are small, long, slender and trumpet-shaped; they are 0:3-0:7 mm. in diameter in their proximal portions, expanding to 1:5—2-2 mm. at the calice rim. Length of the corallites ranges from 6-12 mm. Corallite stems curve slightly towards the axis of the 8 JOHN ROBERTS colony and then swing abruptly outwards towards the distal regions, so that the apertures are often at 70°-80° to the axis of the stem. The calice of each corallite often projects up to 2-5 mm. in front of the bud of the succeeding corallite. Apertures are round. No traces of septal spines have been observed. Thickness of the external walls of the corallites is slightly less than 0-1 mm. in distal and proximal regions. Corallites are ornamented only by growth annulations. Two branches, not always in one plane, may arise from variable positions on one corallite. The two buds may arise one behind the other on the upper surface of the parent corallite, or the second bud may branch from the front of the parent corallite. MEASUREMENTS (in mm.) : Width of corallite Length of corallite Proximal Rim of calice 12-0 0: 2-0 11-0 0-6 aS He 10-5 0-6 1-75 10-0 0-5 1-5 10:0 0:7 1-8 9-5 0°5 1-8 6-0 0-5 2-0 6:0 0:3 — REMARKS: The corallites of this material are longer and more slender than those of C. crassus McCoy. C.sp. is far more delicate than C. tenu- collas McCoy and in size is intermediate between C. crassus and C. tenuicollis. OCCURRENCE : This species is known from L.215 and L.86 Lewinsbrook. MATERIAL: F.5755—F.5766. The following three polyzoan species described by Crockford (1947) are refigured because of the inadequacy of the original photographs. Polyzoa Order CYCLOSTOMATA Bush 1852 Family HEXAGONELLIDAE Crockford 1947 Genus FISTULAMINA Crockford 1947 TYPE SPECIES: Fustulamina inornata Crockford, 1947. DiaGnosis: See Crockford (1947, p. 28-29). Fistulamina inornata Crockford Plater iaate reo Fistulamina inornata Crockford, 1947, Proc. Linn. Soc. N.S.W., 72, p. 29, pl. 4, figs. 5-6. REMARKS: Several additions can be made to Crockford’s description of the species. (1) Fine longitudinal ridges occur between the apertures on occasional specimens. (2) The outer rim of the apertures is raised into hooded lunaria which are visible only on well preserved specimens. (3) The number of rows of zooecial apertures is more variable than previously realized ; in the Lewinsbrook material the number ranges from 5-10. OCCURRENCE: This species occurs at L.215-— L.217, L.86 Lewinsbrook and L.50 Gresford Quarry. MATERIAL: F.5361—F.5363. Family GONIOCLADIIDAE Nikiforova 1938 Genus GONIOCLADIA Etheridge 1876 TYPE SPECIES: Gontocladia cellulifera Etheridge, 1876, Geol. Mag., 2, p. 522-523. Diacnosis: See Bassler (1953, p. G89-90). Gomtocladia laxa (de Koninck) Plate 1, figs. 6-8 Gontocladia laxa (de Koninck), Crockford, 1947, Proc. Linn. Soc. NeS.We) 727 pze ol pl. 5, figs. 3-5. OCCURRENCE: Gontocladia laxa occurs at L.215—L.217, L.86 Lewinsbrook, L.50 Gresford Quarry and L.233 Trevallyn. MATERIAL: F.5353-F.5360. Order CRYPTOSTOMATA Vine 1833 Family ACANTHOCLADIIDAE Zittel 1880 Genus PTILOPORA McCoy 1845 TYPE SPECIES: Ptilopora pluma McCoy, 1845. DiaGnosis: See Bassler (1953, p. G128). Ptilopora koninckt Crockford Plate 2, figs. 1-2 Ptilopora konincki Crockford, Proc. Linn. Soc. N.S.W. 72, p. 39-41, pl. 6, fig. 5. OcCURRENCE: Ptilopora konincki occurs at L.86 Lewinsbrook and at stratigraphically higher localities listed in Crockford (1947). MATERIAL: F.5364—F.5365. Family FENESTELLIDAE King 1850 Genus FENESTELLA Lonsdale 1839 TYPE SPECIES: Fenestella subantiqua d Orbigny. Diacnosis: See Bassler (1953, p. G120). Fenestella browne n. sp. Plate 2, figs. 3-5 DiaGnosis: Moderately coarse mesh ; branches thin, bearing a broad smooth carina ; fenestrules LOWER CARBONIFEROUS FAUNA FROM LEWINSBROOK, N.S.W. 9 large and irregularly rectangular ; 5-9 apertures per fenestrule ; delicate carina on dissepiments ; at bifurcation a zooecial aperture is always situated on the inner part of the fork of the bifurcation ; reverse surface smooth. DESCRIPTION : Fragments described are from the lower mid-area of the zoarium. Branches are thin, 0:30-0:38 mm. in width and moderately straight; 13-15 branches occur in 10 mm. The branch expands slightly before bifurcation. A broad carina separates the two rows of zooecial apertures. A third aperture is always present in the fork of the bifurcation. Apertures are small, round, sur- rounded by a distinct peristome and are slightly elevated above the branch and inclined towards the top of the zoarium. The aperture plus peristome has a diameter of 0-1 mm. There are 17-18 apertures per 5 mm., and 5-9 apertures per fenestrule, averaging 7. Zooecia alternate and have a regular, elongate, ovoid shape. Fenestrules are irregularly rect- angular, often having rounded or sharply pointed extremities ; the latter occurs near the bifurcation of the branches. Fenestrules range from 0-4-0-5 mm. in width (at their mid-length) and from 1-8-3-0 mm. in length, averaging about 2 mm. There are 4-5 fenestrules per 10 mm. Dissepiments are below the level of the obverse surface and bear a thinner keel than that on the branches; dissepiments have an average width of 0:2-0-3 mm. The reverse side of the colony is completely smooth and rounded. REMARKS: In general appearance and overall dimensions this species resembles F. propinqua de Koninck (Crockford, 1947, p. 35-36, pl. 6, fig. 4), but differs in possessing a broad carina on the branches, a thinner more delicate carina on the dissepiments and in having the third zooecial aperture (at bifurcation) always situated in the fork of the bifurcation. Fenestella oblongata Koenig (1958, p. 132-134, pl. 21, fig. 4, text-figs. le, f) resembles F. browne in the general shape of the colony, branches and fenestrules. However, F. brownei has a much wider keel on the branches, a smaller keel on the dissepiments and a smooth reverse surface. The name is given to honour Dr. W. R. Browne, formerly of the University of Sydney. OcCURRENCE: F. brownei is known only from L.86 Lewinsbrook. MATERIAL: F.5346—F.5352. Holotype F.5346, paratypes F.5347, F.5348. Fenestella gresfordensis n. sp. Plate 2, figs. 6-8 DraGnosis: Fine mesh, thin regularly rectangular fenestrules, with 6 apertures per fenestrule; carina with single row of nodes at spacings of 0:4 mm. ; aperture present at either end of dissepiment ; apertures round and slightly hooded; branches with striate reverse surface. DEscRIPTION: The material is fragmentary. Measurements are from the older portions of the colony. Branches are thin, 0:15-0:30 mm. in width and have an even bifurcation. There are 17-18 branches per 10 mm. The carina is moderately developed, broadly rounded and bears small sharply pointed nodes every 0-4 mm. The nodes have a density of 6 per fenestrule, plus 1 on the dissepiment. Apertures are small, round and alternating; they are generally less than 0-1 mm. in diameter and have a very small peristome which is hooded on the distal portion so that the aperture faces the older portion of the colony. In most cases, two slightly larger apertures, of diameter 0-12 mm., are found on either side of the dissepiments at their junction with the branches. The number of apertures per fenestrule ranges from 5-6, with an average of 6, plus 1 on the dis- sepiment. There are approximately 20-24 apertures per 5 mm. Three apertures usually occur immediately before bifurcation. Fenest- rules are sharply rectangular and regularly developed. Width of the fenestrules varies from 0-2-0-5 mm. and their length ranges from 1-2-3 mm., averaging 1-5 mm. There are 5-7 fenestrules per 10 mm. Dissepiments are short, measuring 0-1-1-15 mm. They are situated slightly below the level of the branch, are acarinate, narrow on their reverse surface and slightly higher than the base of the branches. Zooecia are alternately arranged and irregularly triangular in shape; the apex of the triangle, at the apertures, is rounded, while the base of the zooecium is expanded into a flange. The reverse surface of each branch is finely ornamented by 4-6 high ridge-like striae. REMARKS: No species comparable with F. gresfordensis have been described from the Carboniferous of Australia. Fenestella plebia McCoy, described by Whidborne (1898, pl. 22, figs. 14-15, pl. 23, fig. 1) from the Pilton Beds of England is, as far as can be determined, similar to fF. gres- fordensis, but differs in the absence of larger apertures on the dissepiments. This species has been named after the town of Gresford, N.S.W. branches ; 10 JOHN ROBERTS OCCURRENCE: Ff. gresfordensis is known only from L.86 Lewinsbrook. MATERIAL: F.5335—-F.5339, F.5345. Holotype F.5335, paratypes F.5336, F.5338. Fenestella wilsont n. sp. Plate 3, figs. 10-12 DIAGNOSIS: Fine’ mesh =~ branches “thin, fenestrules rectangular; 3-4 apertures per fenestrule ; obsolete carina bears 3 nodes per fenestrule plus 1 on the dissepiment ; zooecia triangular; branches with striate reverse surface. DESCRIPTION: The material is fragmentary. Measurements are taken from the older portions of the colony. Branches are straight, narrow, 0-15—0-2 mm. in width and have a very distant bifurcation. There are 23-24 branches per 10 mm. The carina is low, obsolete and bears small nodes with a density of 3 per fenestrule, plus 1 on the dissepiment. Apertures are small, circular, 0-07 mm. in diameter, barely raised above the level of the branch and are surrounded by minute peristomes. There are 3-4 (usually 4) zooecial apertures per fenestrule. Fenestrules are sharply rectangular to slightly oval and elongate. Their width ranges from 0-2—0-3 mm. and length averages 0:8 mm., ranging from 0-7-1 mm. There are 12-13 fenestrules per 10 mm. Dissepiments are short, measuring 0-07—0-1 mm., and are lower than the branches on both the obverse and reverse surfaces. Zooecia are triangular on the reverse surface of the colony. The reverse surface of the branches is ornamented with 5-6 fine raised striae. REMARKS: Jf. wilsoni differs from F. acarinata Crockford (1947, p. 36, pl. 6, fig. 3) in possessing a node-bearing carina, sharply rectangular fenestrules, dissepiments which are below the level of both the obverse and reverse surfaces and round apertures, barely raised above the surface of the branch. F. wilsont differs from F. serrulata Ulrich, figured by Koenig (1958, pl. 21, fig. 5, text-fig. 1m, n), in the possession of one more aperture per fenestrule and slightly wider fenestrules. This species is named after Mr. C. H. Wilson, “ Brinkburn ’’, Gresford. OCCURRENCE: F. wilsont is known only from L.86 Lewinsbrook. MATERIAL: F.5340-F.5345. Holotype F.5340 paratypes F.5341-F.5342. The three species of Fenestella described above have their measurements summarized in the following table. They are readily distinguished by the shape of the zooecial infillings. Zooecia Shape ovoid triangular with flange triangular Nodes Number/ Fenestrule 6+1 on dis- sepiment 3+1 on dis- sepiment Number/ 5 mm. 17-18 20-24 not measured Apertures Number/ Fenestrule 5-9 sepiment 3-4 across Crest of Peristome 0:07 Diameter 0:1 10 mm. 4—5 5-7 12-13 Number Measurements (in mm.) on Fenestella Fenestrules Width Length 1-8-3-0 1-:0-2:°3 0:7-1-0 0:4-0°5 0: 2-0°3 Dis- sepiments Width 0:2 -0:3 0-1 -0:15 0-2-0-5 0-07-0-1 Number in 10 mm. 13-15 17-18 23-24 Branches Width 0:3-0-38 0:15-0:30 0-15-0-2 grves- Fenestella brownei (F.5346) fordensis (F.5335) Fenestella wilsoni (F.5340) Fenestella LOWER CARBONIFEROUS FAUNA FROM LEWINSBROOK, N.S.W. aa Brachiopoda Suborder STROPHOMENOIDEA Maillieux 1932 Superfamily ORTHOTETACEA Williams 1953 emend. Stehli 1954 Family SCHUCHERTELLIDAE Stehli 1954 Subfamily STREPTORHYNCHINAE Stehhi 1954 emend. Thomas 1958 Genus STREPTORHYNCHUS King 1850 TYPE SPECIES: Terebratulites Schlotheim, 1816. DiaGnosis: See Thomas (1958, p. 38). pelargonatus Siveptorhynchus spinigera (McCoy) Plate 3, figs. 4-7 Ortis spinigera (McCoy), 1847, Ann. Mag. Nat. iist.,°20, p: 235, pl. 13, fig. 3. DiacGnosis: Shell biconvex, wider than long: pedicle valve with long umbo and very narrow delthyrium ; brachial valve convex anteriorly ; coarse costae in 3 ranks, crossed by thick lamellar flanges, giving rise to spinose projec- tions ; large divergent socket plates and strong median septum in brachial valve. DESCRIPTION: External. The shell is small for the genus, biconvex, wider than long, sub- elliptical and has angular cardinal extremities. Pedicle valve is gently convex and highest at the umbo. The beak is straight, elongate and extends behind the hinge, but does not overhang the cardinal area. The umbo may be distorted due to attachment of the valve. The hinge-line is straight and slightly shorter than the median width of the valve. A sinus is absent. The cardinal area is long, concave and set at an obtuse angle to the plane of the commissure. It is differentiated into primary and secondary regions by a groove running from the apex to a point mid-way between the delthyrium and the cardinal extremities and ornamented with horizontal growth lines. The inner secondary area has additional faint vertical striations. The narrow delthyrium is longer than wide and is covered by a strongly arched pseudodeltidium. Costae are poorly defined on the umbo. Brachial valve is most strongly convex towards the anterior margin and except for a small umbonal convexity the posterior region along the hinge is almost flat. The cardinal area is narrow. The notothyrium is broader than long; it is covered by a convex chilidium of 3 overlapping lamellar plates which project posteriorly from the area and are divided by a small central indentation. A fold is absent. Costae are coarse and less well defined towards the hinge-line; they are arranged in three orders, increasing by regular intercalation. Measured on a valve 12 mm. wide and 8 mm. long, at 3 mm. from the umbo there are 7 primary costae per 3 mm.; at 6 mm. from the umbo— 4 primary costae and 3 secondary costae per 3 mm.; at the anterior margin—2 primary costae, 3 secondary costae and 5 tertiary costae per 3 mm. A variable number of strong laminar flanges form blunt spinose projections, especially from the primary costae. Internal. Pedicle valve. Diductor muscle scars are elongate, usually poorly defined, occur high on the umbo and may be moderately impressed into the shell. Adductor muscle scars are situated on a short posteriorly pointed median ridge. Where pedicle valves are distorted the median ridge and diductor muscle scars are poorly defined. Large teeth occur as thickenings on the sides of the delthyrium. Margins of the valve are marked with impres- sions of the external ornament. Brachial valve. Adductor muscle scars are flabellate, pointed at the umbo, broaden anteriorly and are faintly marked by widely spaced longitudinal striae. The median septum becomes higher anteriorly and extends for one- third the length of the valve. Strong socket plates curve inwards posteriorly and join at the cardinal process. They diverge at approxi- mately 90° and are produced past the sockets forming blunt crural bases. Sockets are rounded, well developed and laterally they flare widely. The cardinal process is large and bilobed, with the external lobes separated by a broad groove containing a sharp median pro- jection near its dorsal surface; each lobe is subdivided by a median channel. MEASUREMENTS (in mm.) : Pedicle valve Length Width Hinge Width ll 14 8 7 6 — Brachial valve Muscle Field Length Width Hinge Width Length Width 12 est. 17 12 — — 11-5 14 ll 4 6 9°5 15 13 — — 9 10°5 8 5) 4 8 10 8 3 3 8 9 7 4 4 REMARKS: S. spinigera (McCoy) bears some resemblance to S. minutum Cummings, described by Weller (1914, p. 70-71, pl. 6, figs. 16-21), from the Salem Limestone, Mississippi Valley, U.S.A. However, S. sfinigera is larger, has a 12 JOHN ROBERTS longer cardinal area, a narrower delthyrium and the pedicle valve does not become concave anteriorly. The brachial valve is almost flat at the umbo and the costae do not bifurcate. As far as can be ascertained no other compar- able species of Streptorhynchus have been described. OCCURRENCE: This species occurs at L.86 Lewinsbrook, L.53 Greenhills and L.233 Trevallyn. Despite’ an Vexhaustive search, | the type locality of S. sfimigera (McCoy) at Dunvegan on the Paterson River, N.S.W., cannot be found. This is probably due to a change in the course of the Paterson River since the last century, when the Rev. W. B. Clarke collected a large fauna from Dunvegan. MATERIAL: F.5250-F.5261. Suborder PRODUCTOIDEA Maillieux 1940 Superfamily PRODUCTACEA Waagen 1883 Family LEIOPRODUCTIDAE Muir-Wood and Cooper 1960 Subfamily PRODUCTININAE Muir-Wood and Cooper 1960 Genus PRODUCTINA Sutton 1938 emend. Muir-Wood and Cooper 1960 TYPE SPECIES : Productus sampsoni Weller 1909, Bull. Geol. Soc? Amer) 20; p: 300; pl. 12, figs. 18-22. REMARKS: Muir-Wood and Cooper (1960) using hypotype material have emended this genus to include forms having an essentially lamellose brachial exterior. Previously, Sutton (1938, p. 551) noted that the brachial valve was costate, while Weller (1914, p. 130) in describing Productus sampsoni, the type species of Pvo- ductina, recorded a brachial valve “‘ marked by radiating costae similar to those of the opposite valve, and also by similar concentric laminae ”’. This material bears a closer resemblance to the revised diagnosis than to Sutton’s original description of the genus. Since hypotype material has been used in its revision, the new concept of the genus is valid. The Lewinsbrook specimens are included in Productina Sutton, emend. Muir-Wood and Cooper on the basis of ornament, shape and the morphology of the brachial valve (Text-fig. 5). The latter differs from the type species only in the strength of the lateral ridges and in the geniculate anterior margin of the brachial valve. Avonia Thomas (1914) is distinguished from this material by its weaker costae, which develop only in older individuals, and injyoau more spinose nature of the pedicle valve. Productellina Reed (1943) is regarded as a “nomen dubium’’ as the type specimen is) unidentifiable and thus cannot be compared with this material. Productina globosa n. sp. Plate 3, figs. 1-3 DIAGNOSIS: Strongly convex pedicle valve with 8-9 costae per 3 mm. at anterior margin : cardinal margins with one spine near umbo and another at lateral extremities ; 6-8 spines in poorly defined band well down on the trail ; brachial valve uniformly concave, ornamented with overlapping concentric lamellae and obsolete costellae; brachial adductor muscle scars on two high platforms are separated by a median ridge which broadens anteriorly ; lateral ridges weak. DESCRIPTION : External. convex and globular. Pedicle valve is strongly convex, with the greatest convexity immediately behind the mid-line. The shoulders are steep and the cardinal extremities flat. Greatest width occurs at the hinge. The umbo is moderately incurved. Cardinal extremities are square to bluntly rounded. Costae increase by bifurcation and have a density of 8-9 per 3 mm. at the anterior margin of the valve. Two large spine bases are present on the cardinal extremities and one spine base occurs on either side of the umbo ; approximately 6-8 smaller spine bases are present as a poorly defined concentric band well down on the trail. Brachial valve is uniformly concave, being deepest towards the centre of the valve. Cardinal extremities are flat. Concentric lamellae are regular, overlapping, increase in length away from the umbo and are crossed by obsolete costellae. The lamellae are absent from the cardinal extremities and the valve is aspinose. Internal. Pedicle valve. Adductor muscle scars with indistinct square outlines are situated high on the umbo and separated by a small elongate pit. Diductor muscle scars are obscure. Brachial valve. Adductor muscle scars are smooth, round to ovoid, situated on high platforms and are separated by a thin median ridge which broadens anteriorly into a well defined median septum and extends for half the length of the valve (Text-fig. 5). Two elongate pits separate the median ridge and the adductor muscle platform. The cardinal process is broadly bifid internally and quadrifid externally. Pustules on the floor of the valve are arranged in an irregular radiate pattern and have a The shell is concavo- LOWER CARBONIFEROUS FAUNA FROM LEWINSBROOK, N.S.W. 13 TEXT-FIG. 5 The brachial interior of Productina globosa n. sp. showing the bilobate cardinal process, median septum, adductor muscle scars and weak lateral ridges. (Approx. xX 4.) density of 5-8 per sq. mm. Lateral ridges are divergent from the hinge-line and are weakly developed. MEASUREMENTS (in mm.) : Pedicle valve Width at Hinge Holotype Length Mid-Line Width 10 10 11 8°5 8 9-5 8 est. 8 9 Brachial valve Paratype Width at Hinge F.5239 Length Mid-Line Width 7 8 est. 7-5 6:5 6 — 6 9 8 REMARKS: The cardinal process of P. globosa resembles that of P. fremingtonensis (Reed) from the Lower Carboniferous Gattendorfia zone (1) of the Pilton Beds, Barnstaple, England, as described by Goldring (1955, p. 404-405, text-fig. 2, no. 5). Goldring’s inclusion of this species in Pvoductina Sutton has not been followed by Muir-Wood and Cooper who have placed it in Productellina Reed. P. sampsont (Weller) from the Lower Missis- sippian of U.S.A., figured by Muir-Wood and Cooper (1960, pl. 123, figs. 1-10), has a marked geniculation towards the front of the brachial interior. A fine radial ornament similar to that on the brachial valve of P. globosa is present on the brachial valves of P. sampsoni figured by Muir-Wood and Cooper. However, P. sampsoni as described by Weller (1914, p. 129-130, pl. 13, figs. 30-35) appears to have stronger costae on the brachial exterior. P. parvulus (Winchell), described by Weller (1914, p. 128-129, pl. 14, figs. 24-25), has a similar shape to P. globosa but it is impossible to make a more detailed comparison because of the lack of internal details. The specific name globosa is an indication of the shape of the pedicle valve. OCCURRENCE: L.86 Lewinsbrook. Campbeil (1958, unpublished Ph.D. thesis) has collected this species from Burindi Mudstones at Keepit Dam, on the Namoi River, approximately 500 feet above the Rangari Limestone and on a comparable horizon in Swain’s Gully, Merlewood Section (Carey, 1937). MATERIAL: F.5235—-F.5248. paratypes F.5236, F.5239. Holotype F.5235, Family ECHINOCONCHIDAE Stehli 1954 Subfamily ECHINOCONCHINAE Stehli 1954 Genus PustuLa Thomas 1914 emend. Chao 1927 emend. Muir-Wood and Cooper 1960 TYPE SPECIES: Pyroducta pustulosa Phillips, 1836. DIAGNOSIS: See Muir-Wood and Cooper (1960, p. 250-251). REMARKS: This material differs from the revised diagnosis of the genus in the following features : (1) The ornament is both rugose and lamellose, but with the former predominating. (2) The median septum varies from a thin ridge to a massive septum which is characteristic of the genus. (3) The adductor muscle scars in the brachial valve are not strongly dendritic. Its assignment to Pustula Thomas is based on the external spinose ornament and the structure of the cardinal process and the lateral ridges in the brachial valve. From Stegacanthia Muir-Wood and Cooper the Lewinsbrook material differs in the features listed below. (1) The spine bases are much shorter. (2) The lamellose ornament, especially in the brachial valve, is subordinate to the rugose ornament. (3) The structure of the cardinal process and lateral ridges is characteristic of Pustula rather than Stegacanthia. Pustula multispinata n. sp. Plate 4, figs. 9-14 Diacnosis: Pedicle valve with obsolete sinus ; fold absent on brachial valve; on median anterior portions of valves there are 15-18 wore 14 JOHN ROBERTS ~ spine bases per 5 mm. and 9-10 concentric lamellae or ribs per 10 mm. ; variably developed median septum and possibly two pairs of small triangular adductor muscle scars present in the brachial valve. DESCRIPTION: External. The shell is small for the genus and wider than long. Concentric lamellae and ribs bear regular rows of short spine bases having a density of 15-18 per 5 mm. on the median anterior portion of both valves. Spine bases are of a generally uniform size and have an average length of 0-3 mm. Spines are fragile, filamentous and extend up to 4 mm. from the anterior margin of the shell. Con- centric ribs and lamellae have a density of 9-10 per 10 mm. on the median anterior portion of the shell and generally maintain that density towards the umbo. Brachial valves occasionally have a greater density, one specimen examined having approximately 20 lamellae and ribs per 10 mm. on the median anterior portion of the valve. Pedicle valve is most strongly convex near the umbo. The umbo is slightly incurved over the hinge line and the greatest width occurs at the mid-line of the valve. The sinus is obsolete to jabsent, Postero-lateral extremities are flattened. Brachial valve is shallowly concave with a small deep concave region at the umbo. A fold is absent. Internal. Pedicle valve. The large flabellate muscle field is situated high on the umbo and extends anteriorly for one-fifth the length of the valve. Diductor muscle scars are poorly defined, squarish, longitudinally striated and are possibly in two pairs. Adductor muscle scars are placed on a narrow ridge separating the diductor muscle scars. The internal surface is marked by concentric bands and pustules. Brachial valve. The muscle field is slightly elevated above the floor of the valve. Adductor muscle scars are divided by a faint antero- laterally directed ridge into median and lateral pairs. The median adductor muscle scars are elongate, narrow, teardrop-shaped and expand laterally. Lateral adductor muscle scars are small, triangular, slightly elevated and are placed towards the posterior portion of the median pair. Both pairs of adductor muscle scars are smooth. The median septum is variable in strength and extends half the length of the valve. Straight brachial ridges originate from the lateral margins of the muscle field and join a pair of flabellate brachial markings in the lateral portion of the valve. The cardinal process has a bifid internal surface and trilobate external surface. The two internal lobes are convex and divided anteriorly by a cone-shaped | alveolus. The lobes curve posteriorly and the external trilobate face consists of the extension of the former two lobes plus a median lobe. The region between the outer and median lobes is deeply concave. Cardinal process is buttressed by two strong rounded ridges running parallel with the hinge-line. MEASUREMENTS (in mm.) : Pedicle valve Length Width 25 27-5 Paratype 23-5 32 F.5221 21-5 25 20 26 19 27 18 23 Brachial Valve Length Muscle Field Length Width Median —————————— Septum Length Width Paratype 25 33 [OF ear. — 8 F.5226 23-5 30 12 est: — — 21-5 ~~ 15 5 6 Holotype "18:ests. 320 8 5 6 Paratype 18 25 — — =o F.5219 16:5 23 9 15 22 — — — 14 20 7 6 7 REMARKS: Pustula multispbinata does not resemble any form previously described from the Carboniferous of Australia. P. abbott Campbell (1956, p. 476-477, pl. 49, figs. 4-6) has a stronger sinus in the pedicle valve, a fold in the brachial valve, a larger median ridge and larger muscle scars in the brachial valve, a stronger cardinal process, 8-10 spine bases per 5 mm. and approximately 5 ribs per 10 mm., measured on the median anterior portion of each valve. P. abbotti larga Cvancara (1958, p. 864-865, pl. 110, figs. 14-19) differs from P. multispinata in all the above features and has a considerably larger size. P. gracilis Campbell (956, pe aii 41g pl. 49, figs. 1-3) has 8 spine bases per 5 mm. and 7-9 concentric ribs per 10 mm. on the median anterior portion of the valves. The spines of P. gracilis are arranged in a quin- cuncial pattern. On external features, the closest named overseas species is P. subpustulosa Thomas (1914, p. 278-281, pl. 20, figs. 1-2) from the Z, and Z, zones of England. The internal features of this form are unknown. LOWER CARBONIFEROUS FAUNA FROM LEWINSBROOK, N.S.W. 15 TEXt-rIG: 6 An illustration of the differences of the cardinal extremitiesLoff.Acuminothyris (x3), A, and Mucrospivifer (xX 2), B. P. chouteauensis Branson (1938, p. 40-41, pl. 3, figs. 23-24) from the Chouteau Limestone, Missouri, is distinguished from this species by its more transverse shape. The external ornament of P. praecedens Stainbrook (1947, p. 312, pl. 46, figs. 24-26) from the Percha Shale, U.S.A., is coarser than that on P. multispinata. The name multispinata refers to the numerous fine spines ornamenting the shell. OCCURRENCE: This species is known only from L.86 Lewinsbrook. MATERIAL: F.5218-F.5233. Holotype F.5218, paratypes F.5219, F.5221, F.5226. Suborder SPIRIFEROIDEA Allen 1940 emend. Muir-Wood 1955 Superfamily SPIRIFERACEA Waagen 1883 Family SPIRIFERIDAE King 1846 Subfamily ACROSPIRIFERINAE Termier and Termier 1949 Genus ACUMINOTHYRIS Nn. gen. TYPE SPECIES : Acuminothyris triangularis n. sp. Dracnosis : Unequally biconvex ; much wider than long ; cardinal extremities acutely angular ; hinge line denticulate; ornament of plicae, regular sub-imbricating concentric lamellae and very faint radial lirae; fold and sinus simple ; pedicle interior with short dental plates and faint myophragm ; brachial interior with short crural plates and low myophragm; _ shell impunctate. REMARKS: Acuminothynis differs from Mucro- spbirifer Grabau in having pointed rather than mucronate cardinal extremities in all but neanic growth stages (Text-fig. 6). In addition it has smaller sub-imbricating concentric lamellae when compared with the coarse lamellae ornamented with fine concentric growth lines in the latter genus. The different growth-trends in a species of each genus are shown in Text-figure 7. The name Acuminothyris is derived from the Latin “ acumino ’’—I sharpen. Acuminothyris triangularis Nn. sp. Plate 5, figs. 1-8 Dracnosis: Shell narrowly triangular, 4-5 times as wide as long; fold and sinus simple ; dental lamellae short; shell thickened at the umbo; crurae well developed; 10-15 plicae on each lateral slope ; fine lamellose ornament with density of 12-14 per 3 mm. at the anterior margin. 16 JOHN ROBERTS ww HLONS31 o 20 WIOTH 40 60 mm TEXT-FIG. 7 Individual ontogenies of Acuminothyris triangularis n. sp. (solid lines) and Mucrospivifer prolificus (Silica Shales, Ohio) demonstrating the differences in growth of the two genera. Measurements on brachial valves. DESCRIPTION: Exterior. The shell is slightly unequally biconvex, narrowly triangular, with acutely angular, flattened cardinal extremities. There are 10-15 low rounded plicae on each lateral slope. The lateral plicae become indistinct on the cardinal extremities. Regular sub-imbricating lamellae, with a density of 12-14 per 3 mm. at the anterior margin, are most prominent in the furrows between the plications and are crossed by a fine micro- ornament of radial lirae. At the cardinal extremities the lamellae become straight due to the obsolescence of the plicae. The shell is thickened at the umbo and around the shoulders lateral to the muscle scars. Pedicle valve. Greatest convexity occurs at the umbo, where the beak is strongly incurved over the cardinal area. Cardinal area is low, concave and is 2 mm. high on a valve 44 mm. wide and 10:5 mm. long. It is ornamented with vertical striations and grooves and _ hori- zontal growth lines. The delthyrium is wide and open, except for a small triangular plate covering the apex. The delthyrial angle is 80°. Simple median sinus is sharply defined by high plicae and extends from the tip of the beak to the anterior margin of the valve. The sinal angle is 20°. Brachial valve. The fold is well defined, rounded and expands slightly anteriorly. The cardinal area is low. Brachial valve is less convex than the pedicle valve. Internal. Pedicle valve. The muscle field is divided down its entire length by a low distinct myophragm. Adductor muscle scars are poorly defined and occur on a ridge in the sinus of the valve. Diductor muscle scars are pointed posteriorly and broaden anteriorly, where they have smooth terminations. Those portions situated on the prominent plications bordering the sinus are strongly marked with longitudinal striations and are deeply impressed into the shell. Dental lamellae are short and are supported by a thickening on the umbonal shoulders. The teeth are well developed. Denticles along the hinge-line are more closely spaced towards the delthyrium and articulate with pits on the hinge of the brachial valve. LOWER CARBONIFEROUS FAUNA FROM LEWINSBROOK, N.S.W. 17 Pallial markings are variable ; vascula genitalia range from 8-9 irregular, non-branching, radiat- ing blade-like trunks arising from the lateral margins of the diductor muscle scars (Text- fig. 8), to prominent genital pits associated with one, or possibly two, anteriorly directed vascula extensions following the grooves in the plications of the shell. Brachial valve. Two pairs of adductor muscle scars occur between the large plications limiting the fold of the valve. The inner pair are long, narrow, pointed anteriorly, blunt posteriorly and occur in a shallow depression on either side of the myophragm. The lateral pair, between the inner pair and the large plications bordering the fold, are sharply pointed posteriorly and blunt anteriorly. A strong myophragm extends the length of the muscle field. Plicae bordering the muscle field are distorted, curve slightly outwards and are sharply defined. Cardinal process has up to 9 small vertical lamellar plates and is situated on a callus between the crural plates. Strong, slightly divergent crural plates are buttressed laterally by socket plates. Sockets are narrow, widely divergent and well defined. MEASUREMENTS (in mm.) : Pedicle Valve Muscle Field (at anterior end) Length Width ———\H¥— Length Width 10 38 4°5 3 Holotype 8:5 42 + 3°5 7-5 46 4-5 3 6 28 4 2 Brachial Valve Muscle Field (at anterior end) Length Width Length Width 13 Ta-est:5 — Paratype Evod aig. .s LO HUSESt.2 —— — Paratype F.5180a .. 10 est. 40 5 3 9-5 40 - 3 9 32 est — -= 9 34 — — 8-5 Souests 92) 3:5 8 39-5 — — REMARKS: The writer is not aware of any comparable species from Australia or overseas. The specific name tviangularis describes the general shape of the shell. OccURRENCE: This species occurs at L.215, L.217, L.86 Lewinsbrook, L.50 Gresford Quarry and L.233 Trevallyn. MATERIAL: F.5170—-F.5184. paratypes F.5172, F.5180a. Holotype F.5170, B TEXT=-FIG. 8 Pedicle interior of Acuminothyris triangularis n. sp. showing vascula genitalia arising from around the muscle field ( x 2-25). Subfamily BRACHYTHYRINAE Fredricks 1924 Genus BRACHYTHYRIS McCoy 1884 TYPE SPECIES: Sfirifer ovalis Phillips, 1836. DIAGNosIs: See Maxwell (1954, p. 26). REMARKS: George (1927), in his definition of the genus Brachythyris, states that dental plates are absent. However, dental lamellae as defined by Browne (1953) are present, but the genus lacks adminiculae (Campbell, 1959). Brachythris elliptica n. sp. Plate 4, figs. 1-4 ? Spirifer pinguis Sowerby, de Koninck, 1876, Pal. Fossils, N.S.W. Mem. Geol. Surv. N.S.W., Palaeontology No. 6, p. 185, pl. 14, figs. 2, 2a. Spirifer pinguis Sowerby, Dun, 1902, Rec. Geol, Surve- N.S, (,°pt. 2, p. 34, pl. 22: figs. 1, 2, 5. Non Shirifer pinguis Sowerby, Benson and Dun, 1920, Proc. Linn. Soc. N.S.W., 45, p. 348, pl. 21, figs. 9-11. Diacnosis: Wider than long; hinge-line approximately two-thirds width of shell; cardinal extremities well rounded, elliptical, flat and usually poorly plicate; unequally biconvex ; pedicle valve much higher than the flat brachial valve ; commissure parasulcate. DESCRIPTION: External. The shell is elliptical, unequally biconvex, with the pedicle valve having the greatest convexity. The hinge-line is straight and constitutes two-thirds the width of the shell. Up to 24 plicae broaden anteriorly, become lower laterally and are almost absent from the cardinal extremities. The plicae are separated by shallow sulci one-quarter the width of one plication and are crossed by weak concentric growth lines. Pedicle valve. Greatest convexity occurs at the sharply pointed umbo. The umbonal tip is incurved over the cardinal area and may point anteriorly. The cardinal area is concave, two- thirds the width of the valve and is 7 mm. high on a shell 50 mm. long and 90 mm. wide. It is 18 ornamented with vertical striations having a density of 3-4 per mm. and horizontal growth lines. Delthyrium is open except for a small arched pseudodeltidial plate at its apex. The calcite of the plate is continuous with that of the shell. The delthyrial angle ranges between 75°-85°. Median sinus is narrow, well defined at the umbo and becomes broader and more shallow anteriorly. Its depth ranges from 1-5-3 mm. at the deepest part. The floor of the sinus is flat to slightly rounded and may bear an extremely faint plication; up to three pairs of simple accessory plicae ornament the sides of the sinus. The sinal angle ranges from I REO oe Brachial valve is flat except for a slight umbonal convexity and the low median fold. The gently rounded fold broadens anteriorly and is more than twice as wide at the front than at the mid-point of the valve. The apex of the fold is ornamented by a well defined furrow arising at the umbo. Up to 3 smaller, more obsolete furrows are present on the sides of the fold, the outer furrow being the shortest. Three furrows are present only in gerontic specimens. A marked flexure at the mid-region of the valve coincides with an increased rate of (anterior) widening of the fold. Internal. Pedicle valve. Long diductor muscle scars are bluntly pointed at the umbo, broaden anteriorly and end with laterally rounded terminations. They are _ deeply impressed at the umbo, become shallower anteriorly and are longitudinally or occasionally MEASUREMENTS (in mm.) : JOHN ROBERTS radially striate. Adductor muscle scars are long, narrow, pointed at both ends, situated in a well defined groove between the diductor muscle scars and are separated in their posterior portions by a short faint myophragm. They commence 3-6 mm. in front of the rear edge, and end 4—11 mm. in front of the termination of the diductor muscle scars. Large teeth are supported on well developed dental lamellae formed by a thickening on the inner edges of the delthyrium. The hinge-line is faintly denticulate. The shell is thickened around the umbo and towards the sides of the muscle field. Pallial markings are varied. Vascula genitalia are restricted to a region adjacent to the muscle field. In some specimens 11 or 12 simple trunks radiate from the muscle field through a pitted area (Text-fig. 11). In others there are no well defined trunks and a network of poorly defined ridges produces a striated appearance on either side of the muscle field. Brachial valve. Adductor muscle scars are in two pairs. The inner pair, separated by a low narrow myophragm, is long, narrow, bluntly pointed towards the umbo, broadens anteriorly, terminates bluntly and is _ longi- tudinally striated. The outer pair is less well defined and occurs on the plicae bordering the fold of the valve. The myophragm arises a short distance from the blunt umbo, becomes less well defined anteriorly and terminates at the front of the muscle field. Strong socket plates enclose large striated sockets. Descending lamellae are attached to the inner edge of the Muscle Field Pedicle Valve Length Width Height of Length Length Width Depth Valve Diductor Adductor Scars Scars Paratype F.5185 50 — 10 13 20 13 4 Holotype 50 87 est. — 12 -— 12 — 4] 74 7:5 10 16 8 2 38 60 a 9 15 7 2:5 35 — — 8 9 8 — 30 56 5 8 12 7 1-5 29 62 7 9 15 a 2-5 25 est. 54 5 8 12 7 2 20 est. 36 — 8 — 6 == 15 39 2°5 5 7 4 — — — — tal 9 6 — Adductor Muscles Brachial Valve Length Width Height of Height of Valve Length Width Fold Holotype 50 87 — — — 2 37 est 70 — oa = = 30 60 — — _ 1 Paratype F.5191 30 50 6 8 5 1-5 28 52 5 dl 6 1-5 24 4] — — — = 9 18 — — = == LOWER CARBONIFEROUS FAUNA FROM LEWINSBROOK, N.S.W. 19 uw Oo 30 ww HLON 37 60 WIDTH mm TEXT-FIG. 9 Scatter diagram of length/width ratios of the pedicle valves of Brachythris elliptica n.sp. (circles) and Brachythris pseudovalis Campbell (plus signs) socket plates. Cardinal process consists of approximately 20 small vertical plates placed on a callus between the socket plates. REMARKS: A comparison of SBrachythyris elliptica with Spirifer pinguis Sowerby, described by Davidson (1857, pl. 10, figs. 1-12), shows that the latter is not as wide, is more convex especially in the brachial valve and that the plicate ornament runs strongly to the lateral parts of the valves. Additional furrows are absent from the fold on the brachial valve. The external ornament of B. suborbicularts Hall, described by Weller (1914, pl. 61, figs. 1-8), from the Burlington and Keokuk Limestones of Illinois, resembles that of B. elliptica. How- ever, the former has smaller dental lamellae and a different length/width ratio. B. willbournt Muir-Wood (1948, p. 45-47, pl. 8, figs. 1-3), from the Lower Carboniferous of Malaya, is more convex and has fewer plicae than B. elliptica, while the sinus on the pedicle valve is ornamented with 5-6 bifurcating or trifurcating plicae. Campbell (1957) recognized that this species differed from B. pseudovalis Campbell (1957, p. 76-78, pl. 14, figs. 10-15) from Babbinboon, being consistently broader, more coarsely plicate and having a weaker umbo. Features of the latter species which differ from B. elliptica are : a cardinal area four-fifths the width of the shell ornamented with vertical striations having a density of 8 per mm.; the largely covered delthyrium with a delthyrial angle of 45°; and the presence of 14 plicae on each lateral slope. Scatter plots (Text-fig. 9) show differences in the length/width ratios for B. elliptica and B. pseudovalis. Length/width plots of B. eluptica show irregularities during the early stages of growth of some specimens (Text-fig. 10). OccCURRENCE: B. elliptica is known from L.215, L.216, L.217, L.86 Lewinsbrook, L.50 Gresford Quarry and L.208 Trevallyn. MATERIAL: F.4803—-F.4809, F.5185—-F.5194. Holotype F.5189, paratypes F.5185, F.5191. Subfamily DELTHYRINAE Waagen 1883, Fredericks 1924 Genus DELTHYRIS Dalman 1828 TYPE SPECIES: Delthyris elevata Dalman, 1828. DIAGNOSIS: Spiriferoid; greatest width at hinge-line ; ornament of few simple plications and concentric lamellae ; cardinal area relatively high ; pedicle interior with well developed dental lamellae and median septum. REMARKS: In this collection only one rather poorly preserved interior of the pedicle valve has been found. Despite the fact that no well developed septum and only poorly defined dental lamellae are present, this material has been provisionally placed in the genus Delthyris Dalman because of the simple plications, lamellose ornament and impunctate shell. ? Delthynis papilionis n. sp. Plate 6, figs. 3-7 Diacnosis : Almost plano-convex ; three strong plicae on each lateral slope; imbricating concentric lamellae with density of 12-15 per 3 mm. on the mid-portion of the shell ; cardinal extremities rounded; fold and sinus well developed; long adductor muscle scars in brachial valve; crural plates short; pedicle valve with poorly defined dental lamellae ; median septum obsolete or absent. DESCRIPTION: External. The shell is unequally biconvex to plano-convex, semi-circular and wider than long, with the greatest width at the hinge-line. It is strongly plicate and has a simple fold and sinus. Three plicae on each lateral slope become lower laterally. The strongly imbricating concentric lamellae are crowded at the cardinal extremities, become longer anteriorly and have a density of 12-15 lamellae per 3 mm. on the mid-portion of the shell. Fine radial lrae have a density of 12-15 per mm. at the anterior margin. The shell material is impunctate. UW WJ 20 JOHN ROBERTS 50 HLONSI1 7) 1e) WIDTH mm TEXT-FIG. 10 Individual length/width ontogenies of four brachial valves of Brachythyris elliptica n. sp. Pedicle valve is convex. Greatest height occurs at the bluntly pointed umbo which does not overhang the cardinal area. The prominent median sinus begins high on the umbo, broadens slightly anteriorly and is flanked by high plicae. The cardinal area is high. Brachial valve is semi-circular and flat to shallowly convex, with the flattest area on either side of the umbo. Greatest convexity occurs at the anterior margin. The valve is TEXT-FIG. 11 Pedicle interior of Brachythris elliptica n. sp. showing branching vascula genitalia originating from the muscle field. slightly elevated at the umbo and compressed towards the rounded cardinal extremities. A weak rounded fold arises at the tip of the umbo and broadens anteriorly. The low cardinal area contains a broad triangular notothyrium. Internal. Pedicle valve! Didgetor muscle scars are longitudally striate, elongate and are situated in the furrows of the plicae bordering the sinus. Adductor muscle scars are elevated on a sharp ridge in the sinus and are divided by a myophragm. MEASUREMENTS (in mm.): Pedicle Valve Length Width 6 10 Paratype F.5308 mas 5 6 Brachial Valve Length Width Holotype Se 4 9-5 12 8-5 11-5 5:5 10 Paratype F.5312 ae 5 9 4 6 Brachial valve. Adductor muscle scars are elongate and extend from one-third to one-half the length of the valve. They are pointed towards the umbo, blunt anteriorly and occur LOWER CARBONIFEROUS FAUNA FROM LEWINSBROOK, N.S.W. 21 on the sides of the fold. Crural plates are short and blunt. Sockets are long, broadly rounded, strongly divergent from the hinge and are supported by strong narrow socket plates. Cardinal process consists of 7-8 small lamellar plates elevated on a callus between the crural plates. The internal surface bears impressions of the external concentric lamellae. REMARKS: ?D. papilionis resembles a number of the specimens referred to D. novamexicana Weller (1914, pl. 36, figs. 12, 13, 14, 20 and 21). These, however, differ in possessing mucronate cardinal extremities and a curved umbo on the pedicle valve. The specific name is derived from the Latin “ papilio’’, a butterfly, the shell resembling the shape of a butterfly. OCCURRENCE: This species is known from L.86 Lewinsbrook and L.50 Gresford Quarry. MATERIAL: F.5305-F.5313. Holotype F.5305, paratypes F.5307, F.5308, F.5312. Subfamily AMBOCOELIINAE George 1931 emend. Vandercammen 1956 Genus THOMASARIA Stainbrook 1945 emend. Vandercammen 1956 TYPE SPECIES: Thomasaria altumbona Stain- brook 1945, p. 58-59, pl. 4, figs. 22-30. DiaGnosis: See Stainbrook (1945, p. 57). REMARKS: The genus Thomasaria was emended by Vandercammen (1956) to include two Belgian species. However, Vandercammen’s emendation is not accepted because of positive differences between the Belgian material and the type species and because the type specimens were not examined when the changes to the concept of the genus were made. The Belgian species described by Vander- cammen, YLhomasaria gibbosa Vandercammen and I. parallela Vandercammen, differ from the type species in the possession of a much lower cardinal area on the pedicle valve and in the presence of two narrow unfused deltidial plates extending along the entire length of the delthyrial margins. The deltidial plates on I. altumbona Stainbrook, the type species, are fused and extend half the length of the del- thyrium, and the remainder of the delthyrial opening is covered by a separate plate. These differences are sufficient to separate the Belgian material from Thomasaria sensu stricto. The species described below resembles the Belgian specimens and is referred to ? Thomasaria. When sufficient material becomes available it should be referred to a new genus. The Belgian material, which appears to be congeneric with ? 7. votseyz, occurs in rocks of Upper Givetian and Frasnian age. ? Thomasaria voiseyt n. sp. Plate 4, figs. 5-11 DiAGNosIs: Shell sub-ovate or pentagonal to sub-brachythyrid ; narrow sinus on_ pedicle valve ; poorly defined fold on brachial valve ; pedicle valve with prominent cardinal area ; ornament of up to 5 indistinct plicae in gerontic individuals, fine radial lrae, well developed concentric ornament and small paired spines ; sub-parallel dental lamellae extend for half the length of muscle field; crural plates small, sub-parallel. DESCRIPTION: External. The shell is small and varies in shape from sub-ovate and pentagonal in younger stages to sub-brachy- thyrid in gerontic individuals. The pedicle valve has the greater convexity. The shell is usually wider than long; greatest width occurs near the mid-line, the hinge-line is approxi- mately two-thirds the width of the shell and the cardinal extremities are well rounded. Ornament in gerontic individuals consists of up to 5 obsolete plications on each lateral slope. Younger specimens are smooth, or have one or two indistinct plications. Growth lamellae are prominent, widely spaced medially, but are crowded at the cardinal extremities. Short spines, approximately 0-2 mm. in length, may arise from the concentric lamellae and appear to have a paired arrangement. Very faint radial lirae are crowded at the umbo and extend to the margins of the shell, their density at the anterior margin being approximately 30 per 1 mm. Pedicle valve is most convex in front of the umbo. The beak is moderately incurved. The median sinus has a rounded floor, contains no accessory ornament, is narrow at the umbo and becomes wider and less well defined anteriorly. The delthyrium is wide, triangular, open and has a delthyrial angle of approximately 80°. Ina shell 17 mm. wide the delthyrium is 4mm. wide and 2 mm. high. The cardinal area is sharply defined, moderately high and ‘is ornamented with vertical striations and_hori- zontal growth lines. Brachial valve has a slight even convexity. The fold is extremely obsolete, broadly rounded and does not extent on to the umbo. The cardinal area is small, with a very shallow notothyrium. 22 Internal. Pedicle valve. Diductor muscle scars are long, narrow and broaden slightly anteriorly. They are pointed towards the umbo, blunt anteriorly, longitudinally striate and are well impressed into the shell. Adductor muscle scars are long, narrow, often poorly defined and are situated’ on the median midge, “In some cases they extend past the anterior termination of the diductor muscle scars. Dental lamellae are narrow, sub-parallel and extend anteriorly for about one-half the length of the muscle field. From beneath the teeth they become rapidly lower anteriorly. Teeth are blunt, divergent and strongly developed. Pallial markings are restricted to a small area lateral to the muscle field. Vascula genitalia range from faint trunks arising near the diductor muscle scars _ to radiating striations associated with numerous pit-like depressions. Brachial valve. Adductor muscle scars are narrow, bluntly rounded posteriorly, widen anteriorly and end in a square termination. They are situated high on the umbo and are slightly impressed and longitudinally striated. An outer pair of adductor muscle scars is very poorly defined. The extremely obsolete myo- phragm is best developed in the median and anterior portions of the muscle field. Socket plates are supported by small slightly divergent to sub-parallel crural plates. Ina valve 16 mm. wide and 13 mm. long the crural plates are 1 mm. long. The cardinal process is triangular, having 5-7 vertical lamellar plates. Faint radial vascula genitalia arise from the muscle field. MEASUREMENTS (in mm.) : Pedicle Valve Muscle Field Length Width Length Width 16 19 5 2 Holotype 14 17 7 3 13 17 rf 2°-5 12 14 4. 2, 12 12-5 5 2-5 11-5 14 4. 2, Il 16 5:5 2 10°5 eZ, — — 10 16 5 2 10 est. 16 5:5 2 8 8 3 1-5 est. Brachial Valve Muscle Field Width Length Width —————————_———___ 0 Length Width Hinge 2 8 Paratype 13 15-5 5 F.5202 Paratype F.5214 12 18 — —_ 10 10 16 — — 7 9 11 3°5 2 5) JOHN ROBERTS REMARKS: ? Thomasaria voiseyt differs from T. altumbonata Stainbrook (1945, p. 58-59, pl. 4, figs. 22-30) from the Independence Shale, Iowa, the latter having a very high cardinal area and a stronger fold in the brachial valve. Strongest resemblance is to ?T7. parallella Vandercammen (1956, p. 26—29, pl. 11, figs. 1-6). ?T. voiseyt is larger, has a more pentagonal brachial valve, stronger concentric ornament and a very fine radial ornament. ? T. parallella occurs in the Frasnian of Belgium. This species is named after Professor A. H. Voisey, Department of Geology, University of New England. OCCURRENCE: ? I. voiseyt is known only from L.215 and L.86 Lewinsbrook. MATERIAL: F.5195-F.5217. Holotype F.5195, paratypes F.5205, F.5214, F.5216. Superfamily ROSTROSPIRACEA Schuchert and Le Vene 1929 Family ATHYRIDAE Davidson 1884 Subfamily ATHYRINAE Waagen 1883 Genus CLEIOTHYRIDINA Buckman 1906 TYPE SPECIES: Sfirifer deroyssu; L’Eveillé, 1835. DIAGNOSIS: See Maxwell (1954, p. 42). Cletothyridina segmentata n. sp. Plate 6, figs. 10-12 Dracnosis: Sub-equally biconvex; lamellar fringe one-third to one-quarter length of valve joining spines around margin of shell in older specimens ; long thin spines in young shells ; strong concentric lamellae; fold and sinus obsolete or absent; teeth long and rounded ; narrow pedicle cavity. DESCRIPTION: External. The shell is small to medium sized for genus. It is sub-equally biconvex, ovate to sub-quadrate in shape and has an approximately equal length and width. Greatest width occurs at the mid-line. The hinge-line is short. Concentric lamellae are broad, irregularly spaced, strongly overlapping and have a spinose fringe. The lamellae are usually closely spaced on juveniles, but become widely spaced in older individuals where growth lines occur between the lamellae. Spines in young shells are thin and sharp, but become thick, flattened and bluntly pointed in gerontic forms. In these forms a thin lamellar extension of the shell joins the spines around the lateral and anterior margins, forming a fringe often one-third to one-quarter the length of the shell. Pedicle valve is more convex than the brachial valve. The umbo is slightly incurved over the LOWER CARBONIFEROUS FAUNA FROM LEWINSBROOK, N.S.W. 23 opposite valve and has a round pedicle foramen at its tip. The sinus is variably developed and is usually absent in young individuals. When present, it commences on the umbo and becomes obsolete anteriorly. Brachial valve is uniformly convex. The fold is obsolete and may form a slightly raised area in the mid-part of the valve. Internal. Pedicle valve. The muscle field is very poorly defined. Dental lamellae bordering the pedicle cavity are short and divergent. Teeth are long, rounded and wider than the dental lamellae. The pedicle cavity is narrow and incurved at the umbo. Brachial valve. Adductor muscle scars extend from near the umbo to the mid-point of the valve. They are pointed posteriorly, become slightly wider anteriorly, end in a pointed termination and are separated by a myophragm in their posterior portions. Two straight vascula media branch from near the posterior tip of the muscle field and extend to the antero-lateral margins of the valve. The hinge-plate is flanked by two broad widely divergent crural plates which form the inner boundary of the sockets. MEASUREMENTS (in mm.) : Pedicle Valve (With Spine (Fringe) Length Width ————H— Length Width 23 2 Paratype F.5323 18 22 24 32 18 20 26 — Paratype F.5322 16 18 23 30 13 14 —- — 10 9 — — Brachial Valve Length Width Holotype see 13 13 Paratype F.5325 14 15 9 10 REMARKS: Cleiothyridina glenparkensis Weller (1914, p. 473-474, pl. 78, figs. 21-24), from the Kinderhook Group, Mississippi Valley, resembles C. segmentata in external features, but has a more convex brachial valve. Its internal details are unknown. The name for this species is the Latin for trimmed or ornamented; the lamellar fringe trims the shell. OCCURRENCE: This species occurs at L.86 Lewinsbrook. MATERIAL: F.5320-F.5328. Holotype F.5320, paratypes F.5321-3, F.5325. Cletothyridina squamosa Nn. sp. Plate 6, figs. 8-9 DiAGNosiIs: Small, ovate to elliptical; sub- equally biconvex; imbricating lamellae with scaly spines having a density of 12 per 3 mm. at anterior margin; pedicle valve with large pedicle cavity, short curving dental plates and long teeth; brachial valve with long median septum commencing in front of the muscle field ; large sockets parallel with hinge-line. DESCRIPTION: External. The shell is small, ovate to transversely elliptical and sub-equally biconvex. It is slightly wider than long, the greatest width occurring at the mid-line. Cardinal extremities are well rounded and the hinge-line is short and straight. Anterior margins of the concentric lamellae are produced into a serrated band of imbricating spines which overlap in a regular manner and produce an indistinct radial ornament. The density of spines at the anterior margin is 12 per 3 mm. Pedicle valve is moderately convex. Cardinal extremities are almost flat. The beak is straight, bluntly pointed and has a round pedicle foramen at its tip. Cardinal area is incon- spicuous. The sinus is shallow and rounded on the umbo, but becomes obsolete before reaching the mid-portion of the valve. Brachial valve is slightly more convex than the pedicle valve. The beak is incurved beneath the opposite valve. Internal. Pedicle valve. The muscle field occurs in front of the pedicle cavity. Adductor muscle scars are bluntly rounded posteriorly, pointed anteriorly, occur on either side of a myophragm and are well impressed posteriorly. Curving diductor muscle scars are elongate and narrow towards the umbo, broadly rounded and extend in front of the adductor muscle field. Vascula media run from the front of the adductor muscle scars to the anterior margin of the valve. The diductor muscle field subtends 2 pairs of vascula genitalia. The outer vascula genitalia originate on the lateral margins of the muscle scars and extend to the antero-lateral margins of the valve. The inner vascula genitalia extend from the front of the muscle field to the anterior margin of the valve. The myophragm separating the adductor muscle scars becomes broader, higher and more rounded anteriorly. The large pedicle cavity is bordered by short curving dental plates. Teeth are long, wide, incurved and parallel with the hinge-line. Brachial valve. Adductor muscle scars are elongate, elliptical and terminate near the mid-point of the valve. They are slightly 24 JOHN ROBERTS impressed towards the umbo and are separated posteriorly by a strong median septum extending one-quarter to one-sixth the length of the valve. The triangular hinge-plate has a foramen at its apex. Crural plates are weak and do not extend to the floor of the valve. Sockets between the crural plates and margins of valve are elongate and parallel with the hinge-line. The interior of the valve bears faint impressions of the external ornament. MEASUREMENTS (in mm.) : Pedicle Valve Length Width Holotype “Ef 10 12-5 Brachial Valve Length Width Holotype : 10-5 1255 Paratype F.5330 10 12-5 Paratype F.5331 8:5 10 REMARKS: C. squamosa does not resemble any previously described species from the Carbon- iferous of Australia. It is distinguished from C. transversa Maxwell (1954, p. 46, pl. 6, figs. 5-6) from Mt. Morgan, Queensland, by its approxi- mately equal length and width. The specific name is taken from the Latin ‘ squamosus ’’, scaly, referring to the ornament of flat overlapping spines. OcCURRENCE: This species is known only from L.215 and L.86 Lewinsbrook. MATERIAL: F.5329-F.5331. paratypes F.5330, F.5331. ¢ Holotvpe F.5329, Suborder RHYNCHONELLOIDEA Moore 1952 Superfamily RHYNCHONELLACEA Schuchert 1896 Family CAMAROTOECHIIDAE Schuchert and Ee Vene 1929 Subfamily CAMAROTOECHIINAE Schuchert and “Le Vene 1929 Genus CAMAROTOECHIA Hall and Clarke 1893 TYPE SPECIES: Aivypa congregata Conrad, 1841. DiaGnosis: See Sartenaer (1961, p. 5-7). REMARKS: As a result of the work of Sartenaer (1961) the concept of Camarotoecha has been restricted and the genus is now confined to a small number of Devonian forms. It should not strictly be applied to the species described below but until the Carboniferous rhyncho- nelloid genera have been revised this material is best referred to “‘ Camarotoechia ”’ ‘“ Camarotoechia”’ sp. A Plate 4, figs. 12-14 DESCRIPTION : External. Shell is rhynchonelli- form, small, sub-triangular to sub-ovate and approximately as wide as long. The greatest width occurs at the mid-line. Lateral margins meet the beak at an angle of 75° and the anterior margin is gently convex or straight. Both the fold and sinus are weak and plicate. Plicae are strong, rounded and ornamented by weak concentric growth lines. Pedicle valve is low, with a slight uniform convexity disrupted anteriorly by the median sinus. The beak is small and straight. The sinus originates at the mid-length of the valve, extends to the anterior margin, contains 3 small plicae and is bordered by two large plicae. Brachial valve has an even convex curvature. A faint fold commences at the mid-line of the valve. There are three to four small plicae on each lateral slope. Internal. Pedicle valve. Muscle scars have not been observed. Dental lamellae are small narrow, sub-parallel to slightly divergent and extend for one-eighth the length of the valve. Brachial valve. Muscle scars have not been observed. The median septum is strong, sharp, extends one-third the length of the valve and divides posteriorly, forming a very small crural trough. The weak sockets are placed at an angle to the hinge. The hinge-plate is obscure. MEASUREMENTS (in mm.) : Pedicle Valve Length Width 9 9 8 8 8 8-5 Brachial Valve Length Width 6-5 8 OCCURRENCE: This species occurs at L.86 Lewinsbrook. MATERIAL: F.5314—F.5319. Pelecypoda Family AVICULOPECTINIDAE Etheridge Jr. emend. Newell 1937 Subfamily STREBLOCHONDRIINAE Newell 1937 Genus STREBLOCHONDRIA Newell 1937 TYPE SPECIES: Aviculopecten sculptilis Muller. Diacnosis : See Newell (1937, p. 80). REMARKS: This material differs from the type species of the genus in having almost sub-equal auricles. The type species, described by Newell (1937), is characterized by a larger anterior auricle. LOWER CARBONIFEROUS FAUNA FROM LEWINSBROOK, N.S.W. 25 Sireblochondria obsoleta n. sp. Plate 6, figs. 1-2 DraGnosis: Slightly opisthocline; auricles sub-equal; anterior auricle on right valve flat to concave and strongly ornamented ; anterior auricle on left valve convex, smooth; very deep anterior auricular sulcus ; costate ornament only on dorsal anterior margin of shell. DESCRIPTION: The shell is orbicular, approxi- mately as high as long, very slightly opistho- cline and moderately convex, with. the right valve having approximately the same convexity as the left. The hinge-line is straight. Auricles are small and sub-equal. The anterior auricle is moderately short with a smoothly rounded lateral termination. It is convex on the left valve and flat to gently concave on the right valve. The posterior auricle is not sharply separated from the body of either valve and has a gently rounded posterior margin continuous with that of the shell. The anterior auricular sulcus is narrow and deeply impressed. Byssal sinus occurs as a long narrow rectangular groove extending almost the entire length of the anterior auricle. The umbonal angle is approximately 75°. The anterior umbonal margin is slightly curved and the posterior margin straight. The resilifer has not been observed. Ornament on the body of the shell consists of an extremely fine lattice formed by the intersection of fine radial costae with over- lapping concentric filae; 12-14 costae present on the dorsal anterior portion of the shell become obsolete towards the ventral margin and are generally absent from the umbonal regions of the shell. Costae are weaker on the left valve. Concentric ornament is pronounced on the body of the shell and passes smoothly en to the posterior auricle. The anterior auricle on the right valve is strongly ornamented with 3-4 well developed costae crossed by very coarse imbricating lamellae. On the left valve the anterior auricle is smooth. The interior of the shell is smooth except for large growth lines bearing traces of concentric ornament. MEASUREMENTS (in mm.) : Length Height Holotype F.5752a_ .. 16 15 Paratype F.5752b.. 13 12-5 REMARKS: The form referred to Aviculopecten ptychotis McCoy by Etheridge and Dun (1906, pl. 15, figs. 5, 6, 7), from near Gresford, N.S.W., has a larger anterior auricle than this species. Etheridge and Dun’s description is apparently based upon the specimen in fig. 5; figs. 6 and 7 have smaller sub-equal auricles and probably belong to a different species. The larger anterior auricles and _ coarser ornament over the body of the shell distinguishes the species of Sitreblochondria described by Newell (1937) from S. obsoleta. S. anisotum (Phillips), described by Hind (1903, p. 104-105, pl. 21, figs. 13-20), resembles S. obsoleta but is distinguished by a larger anterior auricle. The specific name is from the Latin “obsoletus’’, indistinct, and refers to the indistinct ornament on the greater portion of the shell. OCCURRENCE: This species is so far known only from L.86 Lewinsbrook. MATERIAL: F.5752-F.5754. Holotype F.5752a, paratypes F.5752b, F.5753, F.5754. ¢ Arthropoda Sub-Phylum TRILOBITOMORPHA Stgrmer 1944 Class TRILOBITA Walch 1771 Superfamily PROETACEA Salter 1864 Family PHILLIPSIIDAE Oehlert 1886 REMARKS: The form of the glabella and cephalon of this material is similar to that found in the family Pvroetidae Salter 1864, but the distinctive pygidium leaves no doubt of its reference to the family Phillipsidae. This resemblance has been previously noted by Weber WS). Genus CONOPHILLIPSIA n. gen. TYPE SPECIES : Conophillipsia brevicaudata n. sp. DiaGNosIs: Glabella short, tapering anteriorly, usually separated from upturned striate border by a narrow furrow; basal lobes broad and convex; glabella furrow 2p clearly defined, 3p may be absent; fixed cheeks narrow ; facial sutures divergent anteriorly, curve almost to glabella at posterior margin of eyes, cut posterior border at an acute angle; lunate, convex eyes faceted. Free cheeks convex, with elevated striate margin; more coarsely granular than glabella; genal spines present. Number of thoracic segments unknown. Pygidium with 13 axial rings and 11 ribs; axis convex, terminating well in front of posterior border ; ribs run to margin anteriorly, become shorter posteriorly. REMARKS: The affinities of this genus with the Proetidae and the Phillipsiidae have been noted in the remarks on the family. 26 JOHN ROBERTS From Phillipsia Portlock this genus differs in the possession of a short tapering glabella and in the number of axial rings and ribs on the pygidium. Proetus Steininger has a similar cephalon but an entirely different pygidium. Other species which belong to Conophillipsia are Phillipsia woodward: Etheridge and the closely related Russian species, P. Jlabrosa Weber and P. kazakensis Weber. The Russian forms occur in the Lower Tournaisian Kassin Beds (Weber, 1937) and the Transition Beds (Nalivkin, 1937) of Kazakhstan. The precise stratigraphic occurrence of P. woodwardi Etheridge is unknown. The type material from lLewinsbrook is fragmentary, but since elements of the cephalon, portions of the thorax and pygidia have been found within a few millimetres of one another there can be little doubt that they belong to the one species and possibly to the one specimen. The generic mame reters to the chaperor the glabella which is cone-like in section. Conophillipsia brevicaudata n. sp. Plate 6, figs. 13-20 Diacnosis: Glabella sub-parallel, gently tapering, smooth; deep preoccipital furrows ; 2p furrow short, 3p absent ; facial sutures with laterally curving pre-ocular branch; _ post- ocular branch runs parallel with the glabella for a short distance past the eye and then swings abruptly outwards; free cheeks longer than broad and marked with very fine granular ornament ; borders ornamented by concentric ridges. Pygidium with abruptly terminating axis; 13 axial rings and 11 distinct ribs in pleural region ; smooth area between posterior ribs and posterior axial segment. DESCRIPTION: Cranidium. The cephalon is approximately twice as wide as long, convex laterally and longitudinally and semi-elliptical in shape. Viewed from the side the gently convex glabella has a broadly rounded mid-region, a deep occipital furrow and a strongly convex occipital ring. The anterior border and the small pre-glabellar field are abruptly upturned. In plan view the glabella tapers slightly anteriorly and has an evenly rounded termina- tion. Two preoccipital lobes are convex, tri- angular and defined by the strong 1p furrow. The 2p furrow is faintly to moderately developed and runs slightly postero-laterally. The occipital ring is convex and wider than the glabella. Palpebral lobes are well developed near the eyes — and extend posteriorly as very narrow flanges between the glabella and the facial sutures. Facial sutures are close to the axial furrows immediately in front of and behind the eyes ; pre-ocular portions curve smoothly outwards, leaving a wide area of fixed cheek lateral to the front of the glabella; post-ocular portions at first continue in a straight line posteriorly, but then swing abruptly outwards, crossing the © posterior border approximately mid-way between the glabella and the lateral border at an acute angle. The anterior border furrow is deep and well defined. The fixed cheek is flat to slightly convex, extremely narrow in its posterior region and becomes wider at the front of the glabella. Free cheeks are longer than broad. The lateral borders are strongly defined by a deep lateral furrow, are raised above the outer edge of the free cheek and end posteriorly in short genal spines. The border is ornamented with fine concentric ridges. Towards the eyes the free cheeks are convexly rounded and stand above the more depressed areas marginal to the border furrows. Posterior border is less well defined, upturned and also striate. Eyes are large, crescentic, strongly arched and are situated high above the level of the free cheek. They are half as long as the glabella (without the occipital ring). The eyes are holochroal, their surface being covered by minute regular. hexagonal facets having an approximate density of 4-5 per0-1sq.mm. A deep furrow separates the base of the eye from the elevated portion of the free cheek. The glabella is smooth and devoid of ornament, the free cheeks are marked by a fine granular ornament, while the lateral and anterior borders and the outer parts of the posterior border are ornamented by 3-4 terrace lines. The doublure has similar terrace lines. No details of the rostrum or hypostome have been observed. Thorax. The number of segments in the thorax is unknown. The axis is moderately convex and slightly higher than the pleurae. Axial rings are not inflated laterally. The axial furrow is widest in the mid-portion of the axis and becomes more narrow towards the margins. Pleurae are flat towards the axis and are bent downwards in their outer portions. Pleural furrows are deep. Pygidium. Pygidium is semi-elliptical, broader than long, with a prominent abruptly ter- minating axis. In plan view the axis, which is strongly outlined by deep axial furrows, tapers posteriorly LOWER CARBONIFEROUS FAUNA FROM LEWINSBROOK, N.S.W. 27 and ends abruptly in a high square termination well forward of the posterior margin. ‘The anterior end of the axis is approximately the same width as each pleuron. The axis contains 13 distinct axial rings which are inclined forwards and are separated by deep ring furrows. The rings become narrower posteriorly. Convexity of the axial rings decreases towards the axial furrows, resulting in the formation of a flat area along the axial margins. Eleven distinct ribs occur on each pleural region. The ribs are broad, separated by well rounded furrows, gently inclined anteriorly and become slightly broader and lower laterally. The posterior portions of the ribs are high, rounded and much more strongly developed than the anterior portions. All except the first rib curve gently backwards ; rib 1 is normal to the axis for the initial one-third to one-half of its length and then curves abruptly backwards ; ribs 1-3 run to the margin, while the remainder become progressively shorter, leaving a smooth border on the posterior of the pygidium. Pleural furrows are obsolete. Both the ribs and axial ring are marked with a very fine granular ornament. Viewed from the side, at the front of the pygidium, the axis is one and a half to twice as high as the pleural lobes. It becomes gradually lower towards the terminal axial piece where the axis is abruptly truncated. The pleural region is moderately convex and also slopes gradually posteriorly. The convexity of the pleural field obscures all except the most posterior portion of the axial furrow. The smooth border is slightly upturned and posteriorly is separated from the pygidium by a broad obsolete furrow. The doublure is at least twice as wide as the border and is marked by 6-7 terrace lines. MEASUREMENTS (in mm.) : Cranidium Length Width Length of of Glabella Glabella Paratype F.5769c 7:5 6 — 6 4°5 3°5 Holotype 6-5 est. 5 + 5 4 3 5 3°5 3 Pygidium Axis Width Length (An- Width terior) Length (An- terior) Paratype F.5769a 9 10 a 3°95 8 10 7:5 + Paratype F.5776 6 8:5 5:5 3 REMARKS: The majority of Mitchell’s specimens (Mitchell, 1918) of Philipsia woodwardi Etheridge have been examined by the author. That species, now referred to Conophillipsia, is much larger than C. brevicaudata, has a relatively shorter and more convex glabella with a 3p glabella furrow and a more convex pygidium in which the axis is less abruptly truncated and the posterior border is weaker. P. woodward: is known from Crows Nest, Stony Creek at Stanwell and from Trilobite Ridge at Mt. Morgan, Queensland. C. labrosa (Weber), described as a Phillipsia species by Weber (1937, p. 34-35, pl. 3, figs. 32-34), is usually larger, although figure 325 is approximately the same size as the present species. The former is characterized by a more convex glabella, which usually abuts against the upturned brim, and the presence of a 3p lateral glabella furrow. C. kazakensis var. paucicostata (Weber), also described as a Phillipsia species by Weber (1937, p. 36, pl. 4, figs. 6, 8-11), is shghtly smaller than this species, but has a more rounded axial termination, 13-14 axial rings and 9-10 ribs on the pygidium. The specific name brevicaudata refers to the abrupt ending of the axis on the pygidium. OCCURRENCE: This species is known only from L.86 Lewinsbrook. MATERIAL: F.5766—-F.5782. Holotype F.5766, paratypes F.5767-5770, F.5776. References BasscerR, R. S., 1953. In Treatise on Invertebrate Paleontology (Moore, R. C., Editor), part G. Bryozoa. 1-253. 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Kans., 10, 1-123, pl. 1-20. OSBORNE, G. D., 1922. The geology and petrography of the Clarencetown-Paterson district. Part I. Proc. Linn. Soc. N.S.W., 48, 161-198. REED, F. R. C., 1943. Notes jon Scegmins Upper Devonian brachiopods figured by Whidborne. Geol. Mag., 80, 69-78, 95-106, 132-138. ROBERTS, J., 1961. The geology of the Grestord district, N.S.W. J. Proc. Roye-s00;- Nos 95, 77-91. _Rotar, A., 1931. Brachiopods and stratigraphy of the Lower Carboniferous of the Donetz Basin. Trans. Cent. Geol. Prosp. Inst. U.R.S.S.,. 73, 35-144, pl. 1-10. SARTENAER, P., 1961. Etude nouvelle, en deux parties, du génére Camarotoechia Hall and Clarke, 1893. Premiere partie: Atvypa congregata Conrad, éspéce-type (1). Bull. Inst. Nat. Sci. Belg., 37 No: 22; 1-11, pl. 1. SARYCHEVA, T. G., AND SOKOLSKAYA, A. N., 1952. Guide de détermination des_ brachiopodes Paléozoiques de la dépression de Moscou. Tyvudy Palaeont. Inst. Acad. Nauk S.S.S.R., 38, 1-307, pl. 1-71. (French translation.) STAINBROOK, M. A., 1945. Brachiopoda of the Independence Shale of Iowa. Mem. Geol. Soc. Amer., 14, 1-74, pl. 1-6. STAINBROOK, M. A., 1947. Brachiopoda of the Percha Shale of New Mexico and Arizona. J. Paleont., 21, 297-328, pl. 44-47. STEHLI, F. G., 1954. Lower Leonardian Brachiopoda of the Sierra Diablo. Bull. Amer. Mus. Nat. Hist., 105, art. 3, 263-358, pl. 17-27. SUSSMILCH, C. A., AND DAvipiT SW. 2. 920: Sequence, glaciation and correlation of the Car- boniferous Rocks of the Hunter River district, New South Wales. Jj. Proc: Roy. Soc. N.S.W., 53, 246-338. Sutton, A. H., 1938. Taxonomy of Mississippian Productidae. jj. Paleont., 12, 537-569, pl. 62-66. Tuomas, I., 1914. The British Carboniferous Producti. I. Genera Pustula and Overtonia. Mem. Geol. Surv. Great Britain. Palaeontology. 1, no. 4, 197-366, pl. 17-20. Tuomas, G. A., 1958. The Permian Orthotetacea of Western Australia. Bull. Bur. Miner. Resour. Aust., 39, 1-115, pl. 1-22. TotmacuHorFfF, I. P., 1924. Faune du calcaire Car- bonifére du Bassin houiller de Kousnetzk. 1. Mater. Geol. Gen. Appl. Leningrad, 25, 1-320, 1. 1-12. ne ere A., 1956. Revision des Ambo- coeliinae de la Belgique. Bwil. Inst. Sci. Nat. Belg., 32, no. 43, 1-51, pl. 1-2. LOWER CARBONIFEROUS FAUNA FROM LEWINSBROOK, N.S.W. 29 Voces, A., 1960. Die bedeutung der Conodonten fiir die stratigraphie des Unterkarbons I und II (Gattendorfia—und Pericyclus—Stufe) im Sauer- land. Fortschr. Geol. Rheinld. u. Wesif., 3, 197-228. WEBER, V., 1937. Trilobites of the Carboniferous and Permian system of U.S.S.R. Cent. Geol. Prosp. Inst. Palaeontology of U.S.S.R. Mon., 61, 1-160, pl. 1-11. WELLER, J. M., e¢ al., 1948. Correlation of the Mississippian formations of North America. Bull. Geol. Soc. Amer., 59, 91-196. Kinderhook faunal studies. V: Bull. WELLER, S., 1909. The fauna of the Fern Glen Formation. Geol. Soc. Amer., 20, 265-332, pl. 10-15. WELLER, S., 1914. The Mississippian Brachiopoda of the Mississippi Valley Basin. Monogr. Geol. Surv. Ill., 1, 1-508, pl. 1-82. WIDBORNE, G. F., 1898. A Monograph of the Devonian fauna of the south of England. 3. The Marwood and Pilton Beds of north Devon and Somerset. pt. 3. Palaeontogr. (Monogr.), 52, 179-236, pl. 22-38. (Received 14 September, 1961, as revised 15 November, 1963) Explanation of Plates PLATE 1 Cladochonus sp. 1, x4. F.5760. note the concentric ornament. 2, branching in a different manner. Cladochonus showing reptant ring. 40. the colony. 5b, x4:-5. small lunaria. Goniocladia laxa (de Koninck). of colony. 7, x5. F.5354. 3, X2°5. tenuicollis McCoy. 4a, Fistulamina inornata Crockford. 5a, F.5368. 0, 02" 2. Rubber cast showing zooecial apertures. Rubber cast showing corallite with two branches ; x4. F.5761. Rubber cast showing two buds F.5766. Rubber cast. «x1-5. F.5374. Rubber cast of colony The opposite side of the colony. x3. F.5363. Rubber cast of portion of Rubber cast showing zooecial apertures and F.5353. Rubber cast of observe surface 8, X22. F.5355. Rubber cast of reverse side of colony ; note smooth surface and distinct carina. PLATE 2 mel eZ: surface of colony ; Rubber cast of reverse surface. Fenestella browne: n.sp. 3, X4. of the zooecial infillings viewed from the reverse side ; paratype. Rubber cast of reverse side of colony ; paratype. Piilopora konincki Crockford. 1, x2-5. F.5365. Rubber cast showing obverse note the dissepiments. 2a, obverse surface of colony showing zooecial apertures on main stem. F.5364. Rubber cast of 2b, x4. F.5364. x 4. -F.5347. Mould of colony showing the shape 4, x3. F.5348. 5a, X3. F.5346. Rubber cast of obverse side of colony showing zooecial apertures, carinate branches and dis- sepiments ; holotype. holotype. Figs. 6-8. 5b, x8. F.5346. Rubber cast of obverse side of colony ; Fenestella gresfordensis n.sp. 6, X8. F.5335. Rubber cast of obverse side of colony ; note the slightly larger apertures at the ends of the dissepiments ; holotype. 7, X6. F.5338. Mould of colony showing shape of the zooecial infillings viewed from the reverse side; paratype. oy OILS F.5345. Rubber cast of reverse side of colony showing faintly striate branches. 30 Figs. Figs. Figs. Figs. Figs. Figs. Figs. Figs. 4—7, 8-9. 10-12. 5-11. 12-14. 1-8. JOHN ROBERTS PRATE GS Productina globosa n.sp. la, x3. F.5239. Rubber cast of brachial interior ; paratype. 16, x3. F.5239. Mould of brachial exterior; panatypemmee <3: F.5236. Rubber cast of pedicle exterior; paratype. 3, x3. ‘F.52353Mould o1 pedicle interior ; holotype. Streptorhynchus spimigera (McCoy). 4a, X2:-8. F.5251. Rubber cast of the brachial exterior and cardinal area of pedicle valve. 4b, x2. F.5251. Rubber cast of pedicle exterior. 5, x3. F.5259. Internal mould of pedicle valve. 6, x2. F.5260. Internal mould of pedicle valve. Ta, x2. F.5250. Internal mould of brachial valve. 7b, x2. F.5250. Rubber cast of brachial exterior; note the chiidium. 7c, x9. F.5250. Rubber cast of cardinal process showing the external face. Bibucia tubtformis n. gen. and sp. 8, X2-°5. F.5370. Rubber cast of fragments of colonies showing branches and general shape of corallite apertures ; paratype. 9, x5. F.5366. Internal mould of colony showing infilled corallites ; holotype. Fenestella wilsont n.sp. 10, x12. F.5340. Rubber cast of obverse side showing zooecial apertures ; holotype. 11, x12. F.5341, Mould showing shape of zooecial infillings ; paratype. 12, x12. F.5342. Rubber cast of striate reverse surface of colony ; paratype. PLATE 4 Brachythyns elliptica n.sp. 1, X1. F.5185. Internal mould of pedicle valve showing muscle field and radiating vascula genitalia; paratype. 2, x1. F.4803. Internal mould of pedicle valve; slightly distorted. 3, x7. F.5191. Internal mould of pedicle valve; paratype. 4a, x1. F.5189. Rubber cast of brachial exterior and cardinal area of pedicle valve ; note the small arched pseudodeltidium ; holotype. 4b, x1. F.5189. Rubber cast of pedicle exterior ; holotype. Thomasaria voiseyin. sp. 5, X2. F.5216. Rubber cast of pedicle interior showing the well developed dental lamellae; paratype. 6, 1-5. F.5195. Internal mould of pedicle valve ; gerontic specimen with weak plications ; holotype. 7, x2. F.5216. Internal mould of pedicle valve ; note the strong dental lamellae ; paratype. 8, x2. F.5204. Rubber cast of pedicle exterior; young individual. 9, x1-5. F.5214. Rubber cast of brachial exterior; paratype. WO) x7 ©5205: Internal mould of brachial valve; paratype. 11, x2. F.5217. Rubber cast of cardinal area of both valves. “ Camarotoecma’’ sp. A. 12, X2. F.5319. Internal mould of brachial valve. 13, x2. F.5319. Rubber cast of brachial exterior. 14, x2. F.5314. Rubber cast of pedicle exterior. PLATE 5 Acuminothyris triangularis n. gen. and sp. 1, X1-5. F.5180a. Internal mould of brachial valve; paratype. 2, x1-5. F.5178. Internal mould of brachial valve ; note the slender myophragm. 3a, 1-5. F.5183. Rubber cast of brachial exterior. 3b, x4. F.5183. Rubber cast of brachial exterior showing lamellose ornament. 4, 1-5. F.5172. Rubber cast of brachial exterior; paratype: 5, 1-5. F.5170. Rubber cast of pedicle exterior ; holotype. 6¢@) X Astr. Nach., 253, 277. The abbreviated form of the title of this ms hf Proc. Roy. oc. N.S.W. \ Gabeione of Figures and Plates should be _ typed: in numerical order on a ‘separate sheet. - Line Diagrams. ‘Line - ‘diagrams, fully. : lettered, should be made with dense black ink on either white bristol board, blue linen or pale-blue ruled graph paper. Tracing paper is “unsatisfactory because it is subject to attack by ‘silverfish and also changes its shape in sympathy with the atmospheric humidity. The thickness of lines and the size of letters and- numbers _ should’ be such as to permit photographic My -reduction without loss of detail. -Dye-line or “photographic copies of each diagram should be sent so that the originals need not be sent to referees, thus eliminating — possible damage to ane caprams while in the S mail. | | ’ Photographs. Cision ceed be in- — cluded only where essential, should be glossy, preferably mounted on white card, and should | . Show as much contrast as possible, since contrast is lost in reproduction of half-tone blocks. - Particular attention should be paid to contrast in. photographs of distant scenery and_ of -» geological subjécts.. When several photographs are to be combined in one Plate, the photographs should be mounted on a sheet of white bristol board in» the arrangement desired for\ final | Bie aaa Geological Papers. Except. in special circumstances, authors submitting manuscripts in which new stratigraphical nomenclature is — proposed must also submit the letter of approval of or comment on the new names from the appropriate nomenclature sub- -committee of the Geological Society of Australia. Reprints. Authors who are members of the Society receive 50 copies of each paper free. Additional copies may be purchased provided they are ordered by, the author when returning ry if Observatory during 1962. W. ace of Devo ecial re ew South Wales. A ‘HL , an and Carbonifer II: The Selection of Rock ference to New South Wales. as a D , eriodical NOTICE TO AUTHORS » General. Manuscripts should be addressed to the Honorary Secretaries, Royal Society of New South Wales, 157 Gloucester Street, Sydney. Two copies of each manuscript are required : the original typescript and a carbon copy; together with two additional copies of the abstract typed on separate sheets. Papers should be prepared according to the general style adopted in this Journal. They ‘should be as concise as possible, consistent with adequate presentation. Particular attention should be given to clarity of EADIGSAOn and good prose style. The typescript should be double-spaced,~ preferably on’ quarto paper, with generous side margins. Headings should be typed without underlining ;. if a paper is long, the headings should also be given in a. table of contents typed on a separate sheet, for the guidance of the Editor, ~~ The approximate positions of Figures, Plates and: Tables should be indicated in the text between parallel ruled lines. Captions of Figures and Plates should be typed on a separate sheet. The author's institutional or residential address should be given in the title of the paper, the relevant. author's initials being attached in brackets to the appropriate address in cases of papers written jointly. Abstract. An informative abstract should be provided at the commencement of each paper for the guidance of readers and for use in abstracting journals. ; Tables. Tabular matter should be type- written on separate sheets, arranged for the most economical presentation on the printed page. Column lines should zot be ruled in. - Units of measurement should always be indicated in the headings of the columns or rows to which they apply. Tables incorporating both text and line diagrams (including dotted lines and shading) should be submitted in a form suitable for direct reproduction by pee rae line blocks. References, the text by giving the author’s name and the year of publication, e.g.: Vick (1934); at the end of the pods they should be arranged ‘THE AUTHORS OF PAPERS ARE ALONE RESPONSIBLE FOR THE . Ss ef Muses fe STATEMENTS MADE AND THE OPINIONS EXPRESSED THEREIN. FO References are to be ated in. alphabetically giving the aang = name’ Cand initials, the year of publication, the title of the’ i paper (if desired), the abbreviated title of the 4 journal, volume number and pages, thus : f VICK, CE , 1934. Asiv. Nach.., 253, On7. ies sbbtesiaiad form of the title of this journal “4 : J. Proc. Roy. Sot: NSW. a Captins of Figures and Plates ships be q typed in numerical order on a separate sheet. ae Line Diagrams, Line diagrams, “fully: lettered, should be made with dense black ink -= on either white bristol board, blue linen or | pale-blue ruled graph paper. Tracing paper is — unsatisfactory because it is subject to attack by — silverfish and also changes its shape in sympathy — with the atmospheric humidity. The thickness | of lines and the size of letters and numbers — should be such as to permit photographic — reduction without loss of detail. ¥ Dye-line or photographic copies of each 7 diagram should be sent so that the originals © need not be sent to referees, thus eliminating ~ possible damage to the diagrams while in ae mail. Photographs. puotéecinns sie be in- cluded only where essential, should be glossy, } preferably mounted on white card, and should . show as much contrast as possible, since contrast — is lost in reproduction of half-tone blocks. Particular attention should be paid to contrast in photographs of distant scenery and OER geological subjects. . When several Soca are to be combined in one Plate, the photographs ~ should be mounted on a sheet of white bristol board in the obi ae desired for final. 2 bial eh, Shits aap = as me dL lesinat reproduction. g : Sees te a ce Geological Papers. oe ‘ine ‘special — circumstances, authors submitting manuscripts — in which new stratigraphical nomenclature a proposed must also'submit the letter of approval ~ x of or comment on the new names from the ~ appropriate _ nomenclature ‘sub-committee - of 4 the Geological Society of Australia. ENG ara e & . Reprints. Authors who are sno of the Society receive 50 copies of each paper’ free. - Additional copies may be purchased ‘provided. they are ordered by the author. yas. eae Boe eke PA gee Sree foe ee t7 ane bse ‘pe aaa gf ee Oi =} F i Journal and Proceedings, Royal Society of New South Wales, Vol. 97, pp. 33-40, 1964 Minor Planets Observed at Sydney Observatory During 1962 W. H. ROBERTSON Sydney Observatory, Sydney The following observations of minor planets were made _ photographically at Sydney Observatory with the 9-inch Taylor, Taylor and Hobson lens. Observations were confined to those with southern declinations in the Ephemerides of Minor Planets published by the Institute of Theoretical Astronomy at Leningrad. On each plate two exposures, separated in declination by approximately 0’-5, were taken with an interval of about 20 minutes between them. The beginnings and endings of the exposures were automatically recorded on a chronograph by a contact on the shutter. Rectangular coordinates of both images of the minor planet and three reference stars were measured in direct and reversed positions of the plate on a long screw measuring machine. The usual three star dependence reduction retaining second order terms in the differences of the equatorial coordinates was used. Proper motions, when they were available, were applied to bring the star positions to the epoch of the in order to provide a check by comparing the difference between the two positions with the motion derived from the ephemeris. The tabulated results are means of the two positions at the average time except in cases 1329, 1335, 1365, 1380, 1413, 1421, 1444, 1456, 1457, 1497, 1505, where each result is from only one image, due to a defect in the other exposure or a failure in timing it. No correction has been applied for aberration, light time or parallax but in Table I are given the factors which give the parallax correction when divided by the distance. The serial numbers follow on those of a previous paper (Robertson, 1963). The observers named in Table II are W. H. Robertson (R), K. P. Sims (S) and H. W. Wood (W). The measure- ments were made by Miss J. Hawkes and Mrs. Y. Lake, who have also assisted in the computation. Reference RoBERTSON, W. H., 1963. J. Proc. Roy. Soc. N.S.W.., plate. Each exposure was reduced separately 96, 31. Sydney Observatory Papers, 43. TABLE I Ravas Dec. Parallax eee Hlanet let (1950-0) (1950-0) Factors h m S O° / wu S wW 1313 10 1962 Sep 1383-53692 21 49 10-34 —08 43 15-0 +0:08 —3:7 1314 63 1962 Jul 25 - 64690 21 27 06-45 —20 16 51-3 +0:04 —2:-1] 1315 63 1962 Aug 16-60637 21 04 49-68 —20 37 50-8 +0:15 —2-1 1316 88 1962 Mar . 20-68292 13 45 46-80 —18 49 38-2 +0:07 —2:3 1317 88 1962 Apr 18-57056 13 23 42-30 —17 02 22-0 +0:01 —2:5 1318 104 1962 Jun 28-62110 19 23 02-34 —25 38 25:4 0:00 —1-2 1319 105 1962 Mar 01-56961 11 06 17-30 —10 04 41-6 —0:10 —3:5 1320 105 1962 Mar 26-53638 10 47 43-32 —03 00 35-2 +0:05 —4:-5 1321 106 1962 Apr 30-56138 14 04 42-34 —09 29 56-6 0-00 —3:6 1322 110 1962 Sep 10-63208 00 31 51-57 —05 38 09-5 0-00 —4:-1 1323 110 1962 Oct 24-52727 23 58 02-95 —O7 37 00-5 +0:12 —3-9 1324 114 1962 May 08-60665 15 29 19-80 —l11 13 47-2 +0:038 —3:4 1325 114 1962 May 22-61427 15 17 11-84 —10 19 48-9 +0:19 —3-6 1326 115 1962 Apr 18-69160 15 37 41-15 —36 29 56-4 +0:12 +0°3 1327 115 1962 May 22-55458 15 02 08-99 —35 02 57-8 +0:05 +0-2 1328 128 1962 May 31-70325 18 23 00-54 —24 58 05-2 +0:16 —1-5 1329 128 1962 Jun 21-61164 18 04 52-41 —25 50 36-1 +0:09 —1-2 1330 134 1962 Apr 26:-62790 15 09 28-21 —33 47 57-6 +0-04 0-0 1331 134 1962 May 23-55737 14 41 00-02 —32 49 16-3 +0-10 —0-2 1332 135 1962 Jun 28-66680 19 44 29-32 —25 15 41-4 +0O-11 —1-4 1333 135 1962 Jul 18-57638 19 26 32-40 —25 41 36-4 +0:03 —1-3 1334 138 1962 May 30:50555 14 43 45-75 —15 47 03-9 0-00 —2:7 1335 138 1962 May 31:48403 14 42 59-82 —15 45 15:3 —0:06 —2-7 1336 160 1962 Mar 26-60086 12 41 51-08 —04 32 30-9 0:00 —4:3 34 W. H. ROBERTSON TABLE I—continued Planet Usk R.A. lay 500) Ss 160 1962 Apr 25-52688 TZ SSE 22 72 1962 Mar 27-67320 14 04 44 172 1962 Apr 25-56530 13235 51 185 1962 Oct 23:-65597 03 25 38 185 1962 Nov 05-56740 03 16 10 186 1962 May 23-64647 17 34 18 186 1962 Jun 21-54591 16 57 48 192 1962 May 15-62918 VO2Z20e a0 192 1962 Jun 21-51152 15 40 52 201 1962 Jul 17-54198 18 22 38 240 1962 Jul 24- 60273 20 21 38 240 1962 Aug 01-60034 20 14 07 246 1962 Sep 27-65148 02 02 56 246 1962 Oct 23-59432 Ol 44 08 250 1962 Jun 14-62985 18 28 Ol 250 1962 Jul 26-47960 17 51705 253 1962 Jul 04: 62970 19 38 35 258 1962 Apr 30-52480 13 36 03 266 1962 May 03-64952 15 37 45 266 1962 May 23-58678 15 27 Yt 278 1962 Aug 09-66208 22 48 06 278 1962 Aug 22-65272 22 37 46 O50 1962 Sep 27-57819 23: 52 23 357 1962 Jun 25-62736 19 04 06 357 1962 Jul 25° 52847 18 41 35 358 1962 Apr 30:56138 14 04 18 360 1962 May 31-62616 Lira 208 360 1962 Jul 04:-47665 16 45 49 380 1962 Aug 28-62961 23 09 10 380 1962 Sep 11-57681 22 57 55 382 1962 Aug 30-52006 2 ZA OL 382 1962 Sep 04-51769 ZA 209 385 1962 May 23-64647 17 41 15 385 1962 Jun 21-54591 i 09s3a2 393 1962 Mar 06-60456 11 14 06 393 1962 Apr 03-53210 LOT53202 394 1962 May 24-63622 17 34 25 394 1962 Jul 03 - 53282 16 57 O07 395 1962 Apr 30:69542 16 19 26 395 1962 May 29-60780 15 55, 55 400 1962 May 02-60807 14 34 32 400 1962 May 24-51570 14 16 33 400 1962 May 29-53025 14 13 31 402 1962 Aug 28-62961 26) 10 10 402 1962 Sep 11-57681 22 58 49 404 1962 Jun 26-65929 20 17 41 404 1962 Jul 18-60134 19 57 53 412 1962 Jun 21-67651 19 26 58 412 1962 Jul 26-55248 18 56 32 417 1962 Jul 02-59882 18 19 14 417 1962 Jul 24-48478 18 03 10 418 1962 May 24-59668 16 17 34 418 1962 Jun 13-52664 15 59) 21 419 1962 Mar 12-56751 11 42 29 419 1962 Mar 26-57068 11 30 02 422 1962 May 08-64044 16 30 31 422 1962 May 31-58616 16 04 47 425 1962 May 03-64952 15 42 20 425 1962 May 23-58678 15 24 58 438 1962 Apr 30:69542 16 16 42 438 1962 May 29-60780 15 49 08 443 1962 Apr 30:56138 14 00 46 451 1962 Jul 16- 65634 21 19 42 451 1962 Aug 16:58436 20 55 11 458 1962 Aug 29-65035 23 36 33 Dec (1950-0) -46 —02 40 20-5 -22 —26 10 07:3 -14 —25 49 15-4 -66 —16 50 22-5 -02 —18 44 20:3 -53 —43 22 45-9 -10 —45 23 12-3 -86 —32 16 59:7 -03 —30 31 52-8 -50 —15 21 27-5 -82 —19 53 57-1 “19 —20 24 17-5 -44 —02 44 08-0 -83 —06 34 25-2 -72 —39 42 12-7 -66 —39 43 22-9 -36 —09 09 08-7 -92 —09 00 32-0 -92 —20 40 08:7 -98 —18 34 56-4 -32 —20 11 23-2 -62 —21 23 35:8 -78 —05 58 28-9 - 84 —09 26 18:3 -05 —ll 41 25-4 -46 —O08 58 36:7 -32 —09 04 01:9 -14 —09 33 57-9 ‘Ol —15 50 49-5 °31 —17 16 03:6 -93 —13 34 21-6 - 24 —13 41 30:8 -95 —43 55 43-2 -34 —43 48 57-5 -70 —10 55 39:7 -46 —O7 08 29-5 oh —24 48 15-0 -78 —25 59 40-2 -62 —23 31 58-4 -78 —21 57 06-0 -60 —31 53 19-2 -10 —30 27 38-0 - 04 —30 02 24:8 -90 —15 26 10:0 -25 —17 22 01-3 -07 —26 47 17-5 -91 —30 16 20-0 -58 —20 29 21-0 -46 —24 08 45:5 -51 —13 15 53-2 -60 —13 43 38-7 “49 —22 05 17-2 -06 —20 29 55:3 - 26 —03 53 41-9 -32 —02 19 50-6 - 23 —28 47 27-5 -03 —28 52 34-4 -86 —18 39 39-8 -69 —18 08 12-2 -06 —22 43 50-8 :87 —23 19 10-2 -87 —06 57 26-6 -90 —29 46 21-1 -52 —33 09 23-9 - 36 —13 23 16-9 Parallax Factors S Ww +0:08 —4 +0:06 —l1 +0:03 —1 +0:07 —2 —0:08 —2 +0:Ol1 +1 +0:03 +1 +0:05 —O +0:09 —O +0:05 —2 +0:04 —2 +0:12 —2 +0:01 —4 +0:09 —4 +0:04 +0 —0:01 +0 +0:04 —3 —0:05 —3 +0:10 —2 +0:11 —2 +0:05 —2 +0:15 —2 +0:06 —4 +0:04 —3 +0:03 —8 0:00 —3 +0:06 —8 —0:06 —3 +0:06 —2 +0:04 —2 —0:03 —8 +0:01 —3 —0:01 +1 —0:01 +1 +0:03 —8 +0:09 —3 —0:02 —1 +0:09 —I1 +0:14 —1 +0:16 —1 +0:11 —0O +0:04 —0O +0:15 —0O +0:06 —2 +0:04 —2 —0:02 —1 +0:04 —0O +0:1l1 —2 +0:09 —I1 +0:10 —3 —0:03 —3 +0:03 —1 +0:02 —2 —0:09 —4 +0:06 —4 0:00 —0O +0:09 —O: +0:09 —2 +0:10 —2 +0:14 —I1 +0:17 —1 +0:01 —83: +0:01 —O: +0:12 —0O +0:07 —3: KD DOTORWOIDRODOH OREM NDOINROUDBROBRADOCOADAARAUWAHOHWONURMOOCOTNHHAUMUNANWANNE (1950-0) -( MINOR PLANETS OBSERVED AT SYDNEY OBSERVATORY DURING 1962 TABLE I—continued Planet 458 465 465 465 478 478 483 483 498 498 498 501 501 510 510 522 522 528 528 546 546 558 558 566 566 570 570 579 579 584 584 596 596 599 599 607 618 618 626 626 628 628 638 638 640 640 666 666 674 674 674 675 675 684 684 684 704 704 712 712 722 722 740 740 742 1962 1962 1962 1962 1962 1962 1962 1962 1962 1962 1962 1962 1962 1962 1962 1962 1962 1962 1962 1962 1962 1962 1962 1962 1962 1962 1962 1962 1962 1962 1962 1962 1962 1962 1962 1962 1962 1962 1962 1962 1962 1962 1962 1962 1962 1962 1962 1962 1962 1962 1962 1962 1962 1962 1962 1962 1962 1962 1962 1962 1962 1962 1962 1962 1962 Sep May May Jun May May Sep Oct Aug Sep Sep Aug Aug Apr May Jun Jun Jul Aug Aug Aug Sep Oct Jul Aug Jul Aug Sep Nov Apr May May May Jul Aug Feb. Jul Jul May May Jun Jul Aug Sep Apr May Jun Jul Jul Aug Aug May Jun Jat Jul Aug Apr May Apr May Aug Sep May Jun Jul - 64042 - 70252 -67099 -58743 - 64952 - 58678 -61759 - 55965 -67278 -58491 -58162 - 63469 -55115 -66615 -59871 -59734 -52084 -60708 -51770 - 63469 -55115 -61376 -46987 - 64690 - 55234 - 63508 - 52287 - 64908 -48034 - 60004 -53726 - 70252 °67099 - 66160 -54900 - 65294 - 63130 - 56943 -61435 -55219 -60120 -51044 -57966 -59868 -63471 -50555 - 62736 * 52847 - 66896 -61166 *56056 -61621 -51301 -70973 -58690 -57037 -69160 -58916 -63471 -50555 -65168 -58029 -62616 -56922 -59743 h 23 18 18 17 15 15 O1 00 23 Dee 23 22 21 16 15 17 16 20 20 22 21 23 23 21 21 21 21 Ol O01 14 13 18 18 20 20 12 i) 19 15 14 17 iy 22 22 15 14 19 18 21 20 20 15 15 20 20 20 15 15 15 14 00 23 17 16 18 R.A. (1950-0) 21+ 22 25 02 20 WANE RAWWDON SHOWN OSHHDNNWUIMNOTUWNOOTNAMRE TNE DODHEWHROWHOOCWNONUITBRRWWHODEDOMHO Parallax Factors Ss “ +0-10 —3: +0:18 —1 +0:09 —1 +0:11 —! +0:12 —2 +0:03 —4 +0:-10 —4 +0:-10 —2 —0:07 —l —0:05 —0O —0:02 —0O +0:04 —3 +0:01 —3 +0:O1 —2 0-00 —2 +0:06 +0 +0:05 +0 —0:02 —0O +0-01 +0 +0:-13 —3 —0:01 —3 +0:05 —: +0:04 —1 +0:02 —3 +0:O1 —2 +0:05 —4 —0:07 —3 +0:02 —0O —0:02 —1 +0:18 —l1 +0:10 —O +0:°138 +2 +0:09 +2 —0:02 —2 +0:07 —2 +0:09 —1 +0:08 +3 +0:16 +2 +0:05 —2 +0:05 —2 +0:-O01 —2 +0:15 —2 +0:04 —1 —0:0l1 —2 +0:04 —3 +0:05 —3 +0:02 +0 +0:14 +0 +0O:1l1 +0 +0:-16 —l —0:04 —1l +0:19 —l1 +0:03 —1 +0:06 —I1 +0:12 +0 +0:15 +0 +0:05 —2 0-00 —: +0:01 —8 +0:07 —838 +0:08 —3 +0:05 —38 +0:12 —0O WWW DONWNAR RR WNWWNOHE HE RAOODHUOWOWOHONDOONHONSHHE ARN N TENE OMHEWIRHODOS 35 36 WH KOBERTSON TABLE I—continued Planet 742 757 757 760 760 762 762 767 767 771 vik 776 776 820 872 877 877 893 906 906 926 926 952 952 968 972 972 975 976 976 1005 1005 1018 1018 1021 1021 1034 1034 1034 1069 1069 1096 1096 1196 1196 1200 1200 1245 1245 1382 1382 1424 1426 1585 1585 1594 1603 1603 1607 1607 1607 1941 UF 1962 QK 1962 OK R.A. Wee (1950-0) heim Ss 1962 Jul 24-51924 18 07 52-00 1962 May 29-66508 18 O1 38-44 1962 Jun 28-56476 17 27 45-85 1962 Jul 05: 59272 18 35 52-22 1962 Jul 26:-51375 18 17 41-39 1962 May 29-66508 17 58 41-01 1962 Jun 28-56476 17 31 24-49 1962 Jun 28-62110 19 16 49-06 1962 Jul 26: 55248 18 53 30:97 1962 Feb 28-61514 10 51 00:79 1962 Mar 27:°52647 10: 32° 15-56 1962 Sep 06- 63672 00 35 35-80 1962 Sep 13:61898 00 30 34-39 1962 Aug 29-56401 21 52 52-20 1962 Apr 30-56138 14 04 12-93 1962 Sep 06: 60010 Yap, Saya MOO TAS) 1962 Sep 26- 52085 22 37 05-20 1962 Sep 24-65108 00 45 50-11 1962 Sep 03 - 64606 00 59 19-53 1962 Sep 26-61514 00 41 58-64 1962 May 03-64952 Wapesloy fata 765) 1962 May 31-53048 15 08 32-96 1962 Jul 24- 64392 21 06 49-98 1962 Aug 02-60569 20 58 19:37 1962 Mar 01-60710 11 16 09-67 1962 May 08-68138 16 35 52-03 1962 Jun 05: 55223 16 12 20-40 1962 Aug 30-64150 23 45 36-20 1962 Mar 12-63746 12 34 59-83 1962 Mar 27-59414 12 24 48-79 1962 Aug 28-57966 22 22 44-32 1962 Sep 04-59868 22, 15-53-10 £962, Jul 26-67080 21 59 24-01 1962 Aug 27:-55078 Palle SPT iors | 1962 jul 02- 59882 18 16 30-28 1962 Jul 25-49035 17 56 49-69 1962 Jul 24:-60273 20°22, Mealy 1962 Aug 01-60034 20 15 21-93 1962 Aug 23-49710 20 02 47-03 1962 Jun 25-62736 18 55 38-28 1962 Jul 25- 52847 18°33 31229 1962 Oct 25- 60152 O01 49 11-18 1962 Nov 05:52467 01 39 25-20 1962 Aug 22-69585 23 03 50-40 1962 Sep 27+ 54273 22 38 20-09 1962 Jun 05-59734 7 1A3 WW-29 1962 Jun 28-52084 16 55 20-00 1962 Jul 04: 66823 20 06 18:64 1962 Aug 07:-55856 19 38 56-69 1962 Apr 30-69542 16 16 34-51 1962 May 29-60780 15 50 20-02 1962 Jul 04:59743 18 22 14-41 1962 May 02-60807 14 48 39-53 1962 Aug 27-61893 23 12 06-67 1962 Aug 30-60421 23 10 17-56 1962 May 31-67099 18 O07 57-85 1962 Aug 29-56401 21 48 37:57 1962 Sep 03:-52747 21 44 57-63 1962 Jul 03 - 65329 19 00 17-67 1962 Jul 24-55847 18 40 11-36 1962 Jul 30: 52903 18 35 30-81 1962 Aug 27-65989 00 00 50-93 1962 Aug 30:56112 22 10) 21-21 1962 Sep 06-55162 22 04 47-87 SAawitOSoreNUANOTMUNDOK POO OPROAWEK AW P ORK RE DON WUPWARK NODA QGMNIOWE PNHNOANOSCNWK OOS Parallax Factors S “Ww +0:-08 0 +0:07 +0 +0:09 +0 +0:09 +0 +0:06 +0 +0:08 +0 +0:08 +0 +0:02 —1 +0:10 —1 +0:07 —2 +0:06 —3 —0:03 —0O —0:02 —0O +0:03 —: 0:00 —3 +0:08 —3 +0:04 —2 +0:02 —3 +0:08 —4 +0:06 —83 +0:11 —2 +0:03 —l1 +0:08 —O +0:05 0 0:00 —3 +0:13 —0O 0-00 —0O +0:03 —4 +0:01 —2 +0:03 —3 0:00 —2 +0:14 —2 +0:06 —l +0:02 —1 +OQO-1ll —2 +0:01 —2 +0:04 —2 +0:-12 —2 +0:01 —2 +0:05 —83 +0:05 —3 +0-12 —4 —0:01 —4 +0:26 —0O +0:13 +0 +0:-01 —2 +0:-01 —2 +0-ll —2 +0:-12 —Il1 +0-14 —1 +0:17 —l +0:13 0 +0:08 —0O +0:01 —83 —0:01 —3 +0:09 —I1 +0:04 —2 +0:03 —2 +0:-19 —2 +0:-12 —2 +0:09 —2 +0:03 —4 —0:01 —0O +0:04 —O SDD WHT W PRE OR NDA WUADMNURPOTOIWAWNRE OOTP NH DOWD WAC DE OCrPOCANANAMAOLOINWWAANH SO MINOR PLANETS OBSERVED AT SYDNEY OBSERVATORY DURING 1962 37 TABLE II No. Comparison Stars Dependences 1313 Yale 16 7845, 7847, 7861 0: 26844 0: 34186 0-38970 WwW 1314 Yale 13 I 9190, 9201, 9215 0+ 25206 0: 45340 0+ 29454 5 1315 Yale 13 I 9048, 9052, 9073 0-46591 0+ 20490 0-32919 5 1316 Yale 12 II 5824, 5831, 5846 0-32376 0-37177 0: 30447 S 1317 Yale 12 I 5073, 5088, 5094 0-36123 0-31545 0: 32332 Ww 1318 Yale 14 13500, 13527, 13535 0- 15357 0- 36492 0:48151 Fe 1319 Yale 11 4194, 16 4199, 4222 0-37089 0-52265 0- 10646 S 1320 Yale 17 4126, 4139, 4152 0: 36075 0: 24804 0-39121 Ww 1321 Yale 16 5001, 5013, 5014 0: 39426 0- 12581 0-47993 S 1322 Vale 16 98, 105,:116 0: 22638 0- 40442 0- 36920 WwW 1323 Yale 16 8437, 8457, 8462 0-41098 0+ 35094 0- 23808 W 1324 Yale 11 5407, 5430, 5432 0-35819 0: 14403 0-49778 WwW 1325 Yale 16 5348, 11 5355, 5373 0-55780 0+ 22447 0-21773 S) 1326 Cape 18 7704, 7741, 7746 0- 23505 0-43934 0-32560 WwW 1327 Cape 73 7368, 7397, 17 7811 0: 40150 0-30301 0- 29550 S) 1328 Yale 14 12749, 12762, 12790 0+ 26086 O-saugg 0-36715 WwW 1329 Yale 14 12464, 12496, 12556 0-37413 0-46991 0- 15596 WwW 1330 Cape 17 7848, 7888, 7889 0-30991 0: 27688 0:41321 R 1331 Cape 17 7582, 7589, 7605 0-17739 0+ 40605 41656 S 1332 Yale 14 13766, 13791, 13798 0-27109 0: 23792 049099 R 1333 Yale 14 13561, 13565, 13576 0- 40974 0+ 38246 0-20780 . R 1334 Yale 12 I 5480, 5456, 5459 0- 15595 0-53426 0-30979 WwW 1335 Yale 12 I 5489, 5447, 5456 0: 10343 0-49645 0: 40012 W 1336 Yale 17 4664, 4665, 4674 0: 21321 0:54221 0+ 24457 WwW 1337 Yale 17 4551, 4554, 4563 0-17411 0- 24041 0+ 58548 R 1338 Yale 14 10236, 10247, 10280 0:37842 0: 28076 0-34082 Ww 1339 Yale 14 10011, 10015, 10021 0- 56441 0: 24782 0:18777 R 1340 Wale 2/1 913, 916, 920 0-52470 0:31520 0- 16009 Ww 1341 Malem iZ-1 907; 913, 929 0- 10239 0: 44092 0-45669 S 1342 Cord. D 12628, 12692, 12701 0-31950 0:30133 0-37917 Ss) 1343 Cord. D 11995, 12019, 12092 0: 35267 0-38095 0+ 26639 Ww 1344 Cape 17 8524, 8535, 8564 0: 39361 0: 27036 0-33603 R 1345 Cape 17 8113, 8138, 8151 0-35759 0-35491 0:28751 Ww 1346 Yale 12 I 6725, 6748, 6750 0-19773 0: 36474 0-43753 ise 1347 Yale 13 I 8732, 8738, 8768 0: 48424 0: 20519 0-31056 5 1348 Yale 13 I 8670, 8676, 8709 0+ 36464 0-29117 0- 34420 w 1349 Yale 17 491, 494, 509 0: 42435 0-31090 0+ 26474 S 1350 Yale 16 359, 363, 378 0-13514 0-47907 0+38579 Ww 1351 Cape 18 9521, 9531, 9534 0- 10869 0:30121 0-59009 S) 1352 Cape 18 9058, 9067, 9119 0- 43590 0:31726 0- 24684 w 1353 Yale 16 6854, 6882, 6883 0: 28022 0: 35870 0- 36108 S 1354 Yale 16 4849, 4864, 4877 0+ 27924 0-38227 0: 33849 > 1355 Yale 13 I 6471, 6485, 12 II 6500 0+ 28070 0-51863 0- 20067 S 1356 Yale 12 II 6348, 6371, 6374 0-18593 0:46195 0-35212 S) 1357 Yale 13 I 9613, 9638, 9651 0+ 35247 0: 31838 0-32915 R 1358 Yale 13 I 9569, 9589, 14 15319 0+ 36195 0-42849 0+ 20956 Ww 1359 Yale 16 8413, 8432, 17 8166 0- 18649 0-54185 0- 27166 S 1360 Yale 16 6553, 6561, 6593 0+ 32642 0: 41666 0: 25692 R 1361 Yale 11 6409, 6419, 6434 0- 22162 0-51925 0- 25912 S 1362 Yale 16 5000, 5007, 5013 0: 34377 0+ 23348 0:42275 Ss) 1363 Yale 16 5859, 5869, 5875 0:32498 0:62991 0-04510 Ww 1364 Yale 16 5777, 5788, 5790 0-12571 0- 61646 0- 25782 R 1365 Yale 12 I 8570, 8576, 8600 0: 22851 0-53195 0+ 23954 ix 1366 Yale 12 I 8517, 8537, 8542 0-39127 030464 0-30408 Ww 1367 Yale 11 7574, 7580, 12 I 8068 0-37551 0: 25613 0- 36836 R 1368 Yale 12 I 8032, 117 7559, 7574 0+ 28938 0-35691 0-35370 > 1369 Cord. D 12747, 12829, 12867 0- 23231 0-61489 0- 15280 S) 1370 Cord. D 12198, 12236, 12260 0- 25761 0: 40938 0-33302 Ww 1371 Yale 11 4225, 4240, 4248 0-48954 0- 23142 0+ 27904 w 1372 Yale 16 4129, 4140, 4154 0- 22581 0:55274 0: 22144 R 1373 Yale 14 12076, 12111, 12113 0-46763 0-33193 0+ 20044 Ss 1374 Wales 124 11737, 11743, 11771 0+ 28428 0: 38280 0- 33292 > 1375 Yale 14 11423, 11450, 11462 0: 22414 0-19819 0-57767 S 1376 Yale 13 I 6587, 6606, 6608 0-45748 0: 18929 0+ 35322 w 1377 Cape 17 7512, 7532, 7545 0-14714 0:45177 0-40109 S 1378 Cape 17 7333, 7348, 7357 0-41430 0+31249 Q- 27321 Ss 38 : W. H. ROBERTSON TABLE I[I—continued No. Comparison Stars Dependences 1379 Yale 13 II 8993, 9020, 9028 0- 21593 0-36123 0-42284 1380 Yale 12 I 8570, 8576, 8600 0-37937 0-067938 0-55270 1381 Yale 12 I 8517, 8537, 8542 0- 23672 0- 22058 0- 54269 1382 Yale 14 14087, 14139, 13 II 13392 0-19982 0- 28762 0-51256 1383 Cape 17 10886, 10898, 10916 0- 21097 0-40675 0- 38228 1384 Yale 13 I 8316, 8332, 8356 0-30196 0-19033 0-50772 1385 Yale 14 13169, 13205, 13211 0- 27955 0-52021 0- 20024 1386 Yale 11 6240, 6265, 6277 0- 19286 0- 53622 0- 27092 1387 Yale J//1 6146, 6164, 6174 0-11540 0- 54642 0-33818 1388 Yale 13 I 6733, 6756, 14 11443 0- 20764 0- 25915 0- 53320 1389 Yale 13 I 6601, 6638, 12 II 6621 0- 46833 0-31842 0+ 21325 1390 Yale 17 4391, 4410, 4416 0-42766 0- 29861 0- 27372 1391 Yale 21 3263, 3270, 17 4329 0- 14753 0-46121 0-39126 1392 Yale 13 II 10339, 10347, 10390 0-37241 0-32954 0- 29806 1393 Yale 13 II 10094, 10118, 10119 0-31072 0-33894 0: 35034 1394 Yale 12 II 6499, 6517, 6521 0-35697 0-33134 0-31169 1395 Yale 12 I 5668, 5671, 5684 0- 40992 0:34377 0- 24630 1396 Yale 14 11423, 11431, 11452 0-43423 0-33327 0- 23250 1397 Yale 14 11161, 11181, 11201 0- 36037 0-51950 0-12013 1398 Yale 16 4977, 4990, 4998 0- 27607 0-54534 0-17859 1399 Yale 13 II 14012, 14050, Cape 17 11670 0-30186 0- 40930 0: 28884 1400 Cape 17 11422, 11424, 11469 0-19106 0-38793 0-42101 1401 Yale 11 8233, 8241, 12 I 8723 0-41148 0: 26435 0-32416 1402 Yale 12 I 8695, 8696, 8714 0- 44666 0- 12839 0-42495 1403 Yale 13 II 11660, 11669, 11731 0- 26000 0- 19730 0-54270 1404 Yale 13 II 11636, 11651, 11713 0- 20569 0-33047 0- 46384 1405 Yale 13 II 11265, 11275, 11303 0-38047 0- 35985 0- 25968 1406 Yale 12 II 6449, 6464, 6471 0- 30967 0- 28750 0- 40283 1407 Yale 12 II 6348, 6374, 12 I 5639 0- 29402 0: 27258 0-43341 1408 Yale 17 229, 243, 21 203 0: 39325 0-37648 0- 23027 1409 Wales) 7 7165, ai ose sO 0-33078 0-17194 0-49728 1410 Yale 13 I 9847, 9870, 9871 0-50331 0-39716 0-09953 1411 Yale 13 I 9819, 14 15703, 15743 043762 0-27782 0: 28456 1412 Yale 14 15647, 15655, 15665 0: 23447 0- 44827 0-31726 1413 Cape 17 12128, 12142, 12149 0- 09057 0- 23886 0-67058 1414 Cape 17 11909, 11913, 11935 0- 21081 0- 45688 0-33231 1415 Yale 11 5567, 5587, 5590 0- 27939 0-31673 0- 40388 1416 Yale 1/1 5507, 5524, 16 5526 0- 19323 0-47246 0-33431 1417 Yale W272 1L 7065, 7078," 7079 0: 20577 0- 26158 0-53265 1418 Yale 12 II 6943, 6953, 6959 0- 36583 0- 36584 0- 26833 1419 Cape 18 10597, 10633, 10638 0-48988 0- 29584 0- 21428 1420 Cape 18 10408, 10422, 10459 0- 13088 0-50956 0- 35956 1421 Cape 17 12020, 12051, 12060 0- 23086 0- 52646 0- 24268 1422 Cape 17 11818, 11832, 11849 0- 25512 0- 44950 9- 29538 1423 Yale 16 8446, 8449, 8463 0-19573 0-57930 0- 22497 1424 Yale J1 8244, 8254, 8255 0- 23964 0- 46485 0- 29551 1425 Yale 7/3) 1 918i (9190) 9214 0- 36278 0-33038 0-30684 1426 Yale 14 14585, 14604, 14609 0 - 22956 0- 45924 0-31120 1427 Yale: 1" 7980;7 7611) 17616 0-37582 0-38719 0+ 23699 1428 Yale 12 17907, 7930, 7938 0-32122 0- 30258 0-37620 1429 Yale 16 329, 332, 341 0- 36904 0- 28470 0- 34626 1430 Yale 16 228, 229, 234 0- 45526 0-42231 0- 12242 1431 Yale 13 II 8907, 8914, 8953 0-38598 0- 26717 0- 34685 1432 Yale 13 II 8766, 8805, 14 10142 0-44128 0- 34666 0- 21206 1433 Yale 13 II 11660, 11669, 11731 0- 25796 0-53626 0- 20578 1434 Yale 13 II 11636, 11651, 11713 0-38566 0-48073 0:13361 1435 Cape Zone 19092, 19108, 19130 0-52471 0-14428 0-33101 1436 Cape Zone 18826, 18830, 18867 0-50808 027997 0- 21194 1437 Yale 12 II 5389, 5411, 12 I 4782 0- 29535 0: 28724 0-41741 1438 Yale 13 I 8388, 8398, 8424 0-38768 0- 28959 0-32272 1439 Yale 14 13436, 13484, 13485 0- 29362 0- 36465 0-34173 1440 Cape 19 5774, 5804, 5833 0-33748 0-38464 0-27788 144] Cape 19 5574, 5583, 5605 0- 16647 0-49610 0-33743 1442 Yale 11 6034, 12 I 6346, 6379 0- 30995 0-21819 0-47186 1443") “Valé® 72.1 G81 6195.) 6201 0- 36670 0- 36286 0- 27044 1444 Yale 13 I 9478, 9489, 9492 0- 24578 0-48019 0- 27403 AAMNNNNNNDSSNSNNDANNNDODSSMNDDADADSSVSSVNNNDSSVODAMNANSMNuNVN ss serANnsennsnnans MINOR PLANETS OBSERVED AT SYDNEY OBSERVATORY DURING 1962 39 TABLE I]—continued No. Comparison Stars Dependences | 1445 Yale 13 I 9450, 9456, 9474 0- 40980 0- 29210 0- 29809 S) 1446 Yale 13 I 6313, 6315, 6323 0- 64126 0-21144 0-14730 R 1447 Yale 12 I 5461, 5483, 5485 0- 16640 0- 60006 0+ 23355 WwW 1448 Yale J/ 6567, 6581, 6588 0- 22790 0- 35969 0-41241 R 1449 Yale J/ 6345, 6376, 6382 0- 36930 0-46475 0- 16595 S 1450 Cape 18 10906, 10931, 10932 0-30207 0- 12209 0-57584 > 1451 Cape 18 10813, 10823, 10833 0- 28183 0- 22078 0-49739 R 1452 Cape 18 10730, 10738, 10760 0- 45854 0-16901 0-37244 W 1453 Yale 2#f 11101, 11116, 11154 0- 29266 0-32910 0-37824 Ss) 1545 Yale 14 11027, 11028, 11057 0- 33096 0- 29289 0-37615 R 1455 Yale 174 14261, 14303, 14318 0- 40642 0- 28301 0-31057 S 1456 Yale 14 14043, 14046, 14076 0-40431 0- 26926 0+ 32643 S 1457 Yale /4 13984, 18985, 14012 0-35297 0-33318 0-31385 W 1458 Cape .15" 7766, 7767, 7793 0- 45660 0- 25241 0- 29099 WwW 1459 Cape 18 7498, 7499, 7523 0-41562 0-21812 0- 36626 S 1460 Yale 12 II 6294, 6303, 6307 0-43473 0- 30927 0- 25600 R 1461 Yale /2 I 5430, 5456, 5459 0-49818 0-19873 0-30310 WwW 1462 Yale J/ 3, 4, 14 0-19762 0-30163 0-50075 R 1463 Yale JJ 8243, 8249, 8258 0- 27848 0-59189 0-12962 §§$ 1464 Yale J/ 5831, 5845, 5851 0-25717 0- 33220 0- 41062 Ww 1465 Yale 11 5786, 5791, 5809 0- 23085 0- 54386 0+ 22529 S 1466 Cape 17 9947, 9975, 9983 0-39885 0-19708 0-40407 Ss 1467 Cape 17° 9729, 9730, 9773 0- 27364 0- 28025 0-44610 S 1468 Cape 17 9658, 9660, 9691 0-25119 0-38808 0- 36072 W 1469 Cape 18 8742, 8764, 8784 0- 29677 0: 26067 0: 44256 R 1470 Cape 18 9579, 9609, 9642 0- 24182 0-39096 0: 36722 S 1471 Cape 18 9374, 9410, 9420 0- 25979 0-46381 0- 27640 S 1472 Cape 18 9145, 9195, 9202 0-32438 0: 30366 0-37196 WwW 1473 Cape 17 9292, 18 8798, 8838 0-49912 0- 22835 0-27252 R 1474 Yale 14 13414, 13445, 13469 0- 25343 0-35119 0-39539 R 1475 Yale 14 13146, 13169, 13178 0- 53926 0- 27441 0- 18632 S 1476 Yale 12 I 4326, 4347, 11 4109 0- 22823 0- 23754 0+ 53423 S 1477 Yale 16 4013, 4017, 4030 0- 27608 0- 29788 0- 42604 Ww 1478 Walew io if 198; 215, 231 0-35405 0- 28831 0-35764 S 1479 Yale 13 II 164, 183, 194 0-41911 0- 08285 0- 49804 W 1480 Yale 12 II 9348, 9367, 12 I 8213 0-31752 0- 42580 0- 25669 R 1481 Yale 16 5000, 5003, 5022 0- 25233 0-42224 0-32544 S 1482 Yale 11 8044, 8057, 8063 0-47558 0- 21858 0- 30584 S 1483 Yale 12 I 8421, 8434, 8435 0-18252 0-17456 0- 64292 S 1484 Yale 12 I 196, 210, 17 154 0-50268 0- 28865 0- 20868 Ss 1485 wale 16. 197, 211, 213 0- 25660 0-34621 0-39719 S 1486 Yale 16 145, 146, 155 0-20770 0- 49348 0: 29883 S 1487 Yale 12 II 6464, 6471, 6500 0- 27640 0-47396 0- 24964 ss) 1488 Yale 14 10821, 13 I 6284, 6304 0- 24565 0- 49052 0- 26383 WwW 1489 Cape 17 11543, 11553, 11573 0-52036 0- 30429 0-17535 ) 1490 Cape 17 11464, 11465, 11506 0-54730 0- 23685 0- 21585 WwW 149] Yale 16 4249, 4255, 4256 0- 18428 0-49749 0-31823 ) 1492 Yale 13 II 10399, 10417, 10440 0-37968 0- 30724 0-31308 WwW 1493 Yale 13 II 10181, 10183, 10194 0- 20681 0- 21303 0-58015 R 1494 Yale 17 8136, 8141, 8146 0-15011 0- 40732 0: 44256 R +1495 Yale 12 I 4822, 4842, 17 4583 0- 29495 0- 40186 0-30319 R 1496 Yale 1/1 4519, 4531, 4535 0-37682 0- 29431 0-32887 Ww 1497 Yale 13 I 9490, 9515, 9516 0-34217 0-37088 0+ 28694 R 1498 Yale 13 I 9456, 9474, 9482 0- 23082 0-32504 0-44414 S) 1499 Yale 1/4 15032, 15046, 15068 0- 34326 0- 24379 0-41295 S 1500 Yale 14 14808, 14836, 14838 0- 35050 0- 30090 0- 34860 R 1501 Yale 12 I 6651, 6673, 6701 0-41409 0-19528 0- 39063 S) 1502 Yale 12 I 6455, 6470, 6487 0- 25637 0- 2291) 0-51451 ) 1503 Yale 13 I 8732, 8738, 8768 0-37942 0- 16666 0- 45392 ) 1504 Yale 12 II 8676, 8692, 8699 0-19311 0-51248 0- 29442 Ww 1505 Yale 12 II 8598, 8600, 8622 0- 32052 0- 49992 0: 17957 Ww 1506 Yale 16 6468, 6476, 6495 0+ 25756 0-50765 0- 23478 R 1507 Yale 11 6345, 6376, 6382 0- 21294 0-33461 0- 45245 S 1508 Yale 17 419, 423, 441 0- 39866 0-30523 0- 29611 Ww 1509 Yale 17 383, 396, 402 0-44619 0- 26018 0- 29362 S) 1510 Cape 17 12462, 12466, 12487 0- 25429 0-46191 0- 28380 Ww 40 W. H. ROBERTSON TABLE II—continued No. Comparison Stars Dependences 1511 Cape 18 11610, 11623, 11656 0- 20155 0-31924 0-47921 =) 1512 Valeve/2) 1.6157, 68797 (6193 0-17347 0-41965 0- 40689 R 1513 Yale 12 I 6047, 6066, 6078 0-18981 0- 40656 0- 40363 R : 1514 Yale 12 I 7562, 7573, 12 II 8620 0- 23986 0-41745 0- 34269 S ; 1515 Yale 12 II 8408, 8448, 8450 0- 25475 0-13217 0-61308 R 2 1516 Yale 14 11418, 11437, 11450 0-46181 0- 25273 0- 28545 3) 1517 Vale 72 2i16U) Tesi 20! 0-10414 0-48152 0-41433 W q 1518 Cape 17 9914, 9925, 9955 0-35713 0-42255 0- 22032 S i 1519 Cape 17 7647, 7675, 7677 0- 22695 0- 49603 0- 27702 S 1520 Yale 1/7 8130, 8155, 12 I 8598 0- 40740 0- 20238 0-39022 R 1521 Yale 12 I 8577, 8597, 8598 0-51308 0- 23006 0- 25685 R 1522 Yale 14 12505, 12570, 13 II 11717 0- 27183 0-51876 0- 20940 W 1523 Yale 12 II 9323, 9326, 9343 0- 43392 0- 24065 0-32543 R 1524 Yale 12 II 9298, 9300, 9326 0-38495 0- 34645 0- 26860 S) 1525 Yale 12 I 7044, 7047, 7067 0- 68392 0- 15558 0- 16050 S) 1526 Yale 12 II 7840, 7848, 7881 0-32209 0-39896 0: 27895 S) 1527 Yale 13 I 7797, 7820, 7843 0-50750 0- 36605 0- 12645 W 1528 Vale: 17-8190; 81919 0-11164 0-43965 0-44872 R 1529 Cape 17 12061, 12064, 12078 0- 28211 0: 25984 0- 45805 R 1530 Cape 17 12001, 12021, 12038 0- 21024 0-27765 0-51211 S) (Received 24 May 1963) Journal and Proceedings, Royal Society of New South Wales, Vol. 97, pp. 41-53, 1964 Depositional Environments and Provenance of Devonian and Carboniferous Sediments in the Tamworth Trough, N.S.W. KeitH A. W. CRooK Department of Geology, A.N.U., Canberra ABSTRACT—Data from sedimentary structures, sediment textures, chemical characteristics of sediments, and fossils, suggest that much of the Tamworth and Parry Groups accumulated in a turbidity current-dominated environment, probably in deep water. The upper part of the Parry Group and part of the Drik-Drik Formation apparently accumulated in shallow water. Conflicting evidence on depositional environment from the Yarrimie Formation suggests lateral variations in depth of water, with shallow, tranquil conditions in the north and south where coralline limestones and fine terrigenous turbidites coexist. A generalized map shows the various lithosomes and biosomes recognized. Directional structures in the sediments and isopach data suggest that the Tamworth Trough was elongated along a 340°-160° axis, with a shoreline to the southwest. It appears to have maintained its overall shape throughout the period of sedimentation, deriving most of its sediment from the southwest, a little from the southeast, while more travelled along the axis, from a source at the northeast end of, or marginal to, the trough. Introduction The Tamworth Trough sequence in the Tamworth-Nundle district of N.S.W. consists of two major units, the Tamworth and Parry Groups (Crook, 1961a, 19615). An outline of their stratigraphic subdivision is given in Table 1. The former consists of volcanic lithic gray- wackes (Crook, 1960a) and rudites, with appreci- able radiolarian cherty argillite in the upper parts. Coralline limestone is developed on two horizons, and penecontemporaneous spilite and keratophyre is locally prominent. The Parry Group consists chiefly of mudstone with some prominent developments of volcanic lithic graywacke and sandstone (Crook, 1960)) and polymictic conglomerate. Depositional Environments These two units record a range of depositional and biological environments. Most of the environments appear to have been of deeper water type, but the upper part of the Parry Group apparently records a gradual change to shallower water, passing eventually into terrestrial conditions in the overlying Kuttung eGroup ’. Data of environmental significance from the Tamworth Trough sequence are at present rather limited. Several potential sources of information remain uninvestigated, and no source has yet been investigated exhaustively. Sufficient is known, however, to justify a statement of our present understanding of the problem. Data of significance are available from (a) sedimentary structures, (b) sediment textures, (c) chemical characteristics of the sediments, (d) fossils. SEDIMENTARY STRUCTURES Packham (1954) has recognized two distinct associations of structures which he considers reflect distinct environments, one characterized by traction currents (generally shallow water) and the other by turbidity currents (generally deep water). Lenticular sedimentation units and large-scale cross-stratification are particu- larly characteristic of traction current deposits. Graded bedding, convolute bedding, pull-aparts, sole markings, and extensive sedimentation units with parallel bounding surfaces are characteristic of turbidity current deposits (turbidites). The distribution of various types of sedi- mentary structures in the Tamworth Trough sequence is shown in Table 1. Units including and above the Gowrie Sandstone Member, and including and above Member 7 of the Pyramid Hill Arenite (these being equivalent parts of the sequence), exhibit the characteristics of Packham’s traction current deposits. In addition Members 5 and 7 of the Pyramid Hill Arenite exhibit some features of turbidity current deposits, particularly in the finer units. From below Member 7, and below the Gowrie Sandstone Member, to the base of the Yarrimie Formation, the sequence is characterized by structures suggestive of turbidity current activity. Data from older parts of the sequence 42 KEITH A W. CROOK TABLE 1 Stratigraphic subdivisions of the Tamworth and Parry Groups Eastern and Southern Regions Western and Northern Regions Visean (not preserved) "Lower Kuttung Group" (CK) -Boiling Down Sandstone Member (Clbs) Tournaisian GRO UP -Gowrie Sandstone Member (Clgs) Lower Carboniferous Pyramid Hill Arenite Members (Clp) -8 -9 -10 Goonoo Goonoo Mudstone (Clg) Goonoo Goonoo Mudstone (Clg) PeASh Ray -Turi Graywacke Member (Clt) -Benama Graywacke Member (Clbg) -Garoo Conglomerate Member (Clgc) -Wombramurra Formation (Clw) -Scrub Mountain Conglomerate Member -Scrub Mountain Conglomerate (Cls) Member (Cls) -Hyde Graywacke Member (Clh) -Kiah Limestone Member Upper : : Baldwin Formation (Dub) Baldwin Formation (Dub) Devonian ea te a Pe Yarrimie Formation (Dmy) Yarrimie Formation including Middle Levy Graywacke Member (Dmlg) Devonian Silver Gully Formation (Dms) Silver Gully Formation (Dms) GERBOe Ua. Wogarda Argillite (Dlw) Drik-Drik Formation (Dld) Seven Mile Formation (Dls) Lower Cope's Creek Keratophyre (Dlc) Devonian Pipeclay Creek Formation (Dlp) TAMWORTH Hawk's Nest Beds (Dh) (Strati- graphic position unknown) DEVONIAN AND CARBONIFEROUS SEDIMENTS IN TAMWORTH TROUGH 43 v + & + O + X (Op) an Q a 7 af Ye) A LJ 4 + + a Oe A. e+ fe) Lu Ti exe) Cen (Om o oe A ++e A N oO @ ; on O 85 +O0x A I a x4 424 A ay 4 @® e rs A A A = Xa Oe O ++06 oO A. [= —s + X & A D ‘ x xX lJ 2, OO # 4% xaen a A o A z +4 ‘ M = aay y a a& XX VES -_ ny Ox @ do yi. a O xxa AS A FIG | Be Nae as x A Ax A 2 3 4 5 6 7-891 2 3 4 5 6 78910 THICKNESS (in inches) - OVERLYING FINE BEDS Fic. 1 Plot of thicknesses of paired coarse and fine sedimentation units Symbols: ©O-—Locality 1; @—Locality 2; +—Locality 6; A—Locality 7 x—Locality 3; A—Locality 4; [J—Locality 5; Details of Localities in Appendix I also suggest turbidity current activity but are less definite. Bed-thickness Data: The mudstones of the Parry Group are characterized by alternating coarse and fine layers. The ratio of the thickness of each coarse layer to the immediately over- lying fine layer (the CF ratio) was calculated for several pairs of beds in a series of outcrops. Figure 1 shows variations in the CF ratios. The mean CF ratio for successions at various localities ranges from 0-21 to 2:73 (see Appendix I). The thickness of coarse units increases with creasing CF ratio (Fig. 2). Thus those successions with high mean CF ratios will contain relatively more coarse material, in thicker beds, than successions with low mean CF ratios. If the coarse material is contributed by turbidity currents and the fine by settling from suspension (pelagic sedimentation), the turbidity current contribution will be dominant in those successions with high mean CF ratio. The thicker beds of these successions also imply larger turbidity currents than elsewhere. It is therefore significant that those succes- sions with high mean CF ratios (>1-0) are in close proximity to conglomerates, while the remainder are remote from conglomerates. One would expect conglomerates in_ turbidite sequences only where slumping and turbidity current activity were intense. The relationship between mean CF ratio and turbidity current activity postulated from the above data receives independent support from the distribution of conglomerate units. If the postulate is valid, a broader study of bed- thickness relationships might be expected to yield valuable information on variations of depositional environment. 44 KEITH A. W. CROOK wo f£ nm THICKNESS of COARSE BED (in inches) oi é e) EG. 2 Cr | RATIO“ 9 a Plot, for each pair of sedimentation units, of the thickness of the coarse unit vs. the CF ratio of the pair SEDIMENT TEXTURES Grainsize : Grainsize distribution features of the Tamworth Trough sediments may be of environmental significance. However, the qualitative data obtained from thin-section study reveal no striking trends. Most arenites are moderately to well sorted, with little matrix C<10o7\ Diamictites (Flint, e¢ al., 1960)—“ non-sorted, essentially non-calcareous sediments consisting of sand and/or larger particles dispersed through a muddy matrix’’—are not common. The most prominent diamictites consist of rounded igneous pebbles and cobbles scattered through a mudstone matrix, which is generally non- laminated. Vertically and laterally, by increase in clast content, the diamictites pass into conglomerates. In the Scrub Mountain Con- glomerate Member the diamictites are associated with arenites exhibiting graded bedding and load-cast structures. Mudstones underlying the diamictites, both there and in the Garoo Conglomerate Member, are much disturbed by large-scale slumping. All the diamictites are in the vicinity of conglomerates, chiefly those of the two members mentioned above. Both are thought, on internal evidence, to be in part the result of submarine slumping (Crook, 19610, p. 201). In grainsize, sedimentary features, and associa- tions, the diamictites are akin to the pebbly mudstones described by Crowell (1957) from California. An origin by the down-slope slumping of gravel deposited by turbidity currents on water-saturated mud, postulated by Crowell, would hold equally well for the Tamworth Trough examples. Grain shape: In the lower part of the Drik- Drik Formation, grain shape appears to offer significant information on depositional environ- ment. The keratophyre breccia characteristic of this unit is remarkable in containing clasts up to 5 cm diameter of highly irregular shape and extreme angularity (Crook, 1960a). This indicates a negligible distance of fluvial transport, and in conjunction with other features of the unit, suggests a shallow water marine or a terrestrial depositional environment. CHEMICAL CHARACTERISTICS Chemical and biochemical sedimentation was | an important factor in the genesis of some parts DEVONIAN AND CARBONIFEROUS SEDIMENTS IN TAMWORTH TROUGH = 45 of the Tamworth Trough sequence. The Kiah Limestone Member is a slightly recrystallized lithographic limestone (micrite) lacking terri- genous detritus. It is of wide distribution despite its extreme thinness (generally about 3’) (Crook, 1960, 19610), and appears to be of chemical origin. This limestone represents an unusual episode in the history of the trough, in which the supply of terrigenous detritus was temporarily suspended, allowing a_ purely chemical sediment to accumulate. Oolites, presumably also of chemical origin, form a minor component in parts of the Drik- Drik Formation (Crook, 1960a), and imply a shallow water origin for these rocks. In the Parry Group and the Yarrimie Forma- tion argillaceous limestone occurs as con- cretions. Their features, and particularly their poor compaction (Crook, 1960a, 1960) ; 1961a, p. 185; 19610, p. 197), suggest that they are of early diagenetic origin and developed close to the water-sediment interface. The occurrence of these calcareous materials, and of coralline limestones (biolithites and biorudites) in the Tamworth Group (Crook, 1961a) all indicate that calcite was a stable phase in the depositional environment. The Parry Group, Drik-Drik Formation, Yarrimie Formation and limestone-bearing parts of the Silver Gully Formation then, were apparently deposited in water less than 15,000 ft deep (Sverdrup ef al., 1942). Biochemical silica is prominent in the Yarrimie Formation, in the form of siliceous argillites and radiolarian and spicular cherts (Crook, 1960a), which are similar to the cherts of the Monterey Formation of California. Pelagic sedimentation is indicated (Campbell, 1954, p. D17), and a relative absence of terrigenous detritus. Deep water is not a necessary corollary (Riedel, 1959). However, a low energy environment with negligible turbulence appears to be necessary for the accumulation of biogenic siliceous rocks (Bramlette, 1946). This suggests that much of the Yarrimie Formation accumu- lated in quiet water, more or less cut off from sources of terrigenous detritus. The lower part of the Drik-Drik Formation— breccia, arenite and silty shale—is bright red to purple-red. This is presumably due to anhydrous ferric oxide pigment which was developed in the detritus under terrestrial or littoral conditions. The preservation of the colour indicates a maintenance of oxidizing conditions within the sediment during and after burial. This suggests terrestrial deposition, or rapid deposition in a marine environment. The Hawk’s Nest Beds (Crook, 1961a) accumulated in a euxinic environment. The rocks are dark, the shales being black and pyritic. Plant fragments, carbonized and simulating graptolites, are common. FOssILs Coralline biolithites (i.e. biohermal limestones) occur in both the Yarrimie and the Drik-Drik Formations. Hill (1956, p. F255) considers that Palaeozoic compound rugose corals lived in environments of similar depth and possibly similar temperature to those in which modern colonial corals occur. Rather shallow, probably well aerated, warm water is therefore suggested for the deposition of the Moore Creek, Crawney, Timor, and Nemingha Limestones. The Loomberah Limestone, being a biorudite with abundant terrigenous clasts, probably reflects a different environment. In the top few hundred feet of the Parry Group, a typical shallow water benthonic fauna with abundant brachiopods and bryozoans is common (Fig. 3). Similar faunas occur at Babbinboon (Campbell, 1957) and Merlewood (Carey, 1937). Benthonic forms also occur sporadically in the red shales of the Drik-Drik Formation. Fossils in all of these assemblages are not worn and can therefore be used as environmental indicators. At three points: between Members 6 and 7 of the Pyramid Hill Arenite on Wiles Gully ; immediately above the Turi Graywacke on Boiling Down Creek; and above the Gowrie Sandstone on Spring Creek ; shelly benthos has been encountered. In all occurrences the fossils are either worn or occur in slumped or graded beds, and thus appear to be _ re- sedimented. These fossils are of little value for environmental reconstructions. Trails, especially Chondrites, occur in the mudstones and siltstones of the Parry Group (Crook, 19616). A — soft-bodied — benthos apparently was able to live under the conditions of deposition of parts of the sequence. Much of the sequence, however, is barren except for pelagic forms, chiefly Radiolaria, suggesting water too deep for benthonic forms to survive. A death-assemblage flora occurs in the Goonoo Goonoo Mudstone between the Kiah Limestone and Baldwin Formation. It consists mainly of Leptophloewm and related forms, and is locally quite abundant (Crook, 19615). While not significant from the _ standpoint of depositional environment, it probably records significant events in the source area. 46 KEITH: Av Ws CROOK | BIOSOMES & LITHOSOMES IN THE TAMWOR TROUGH SEQUENCE LIMIT OF TAMWORTH A GROUP ° es, \\ eta oe EUXINIC aaa e siti) LITHOSOME Py? r TERRES (eee LITHOSOMES ==) NERIWG =| LITHOSOMES —------| TRANSITIONAL oe Sear LITHOSOME TURBIDITY | |CURRENT LI THOSOME REEF. | BIOSOME SHALLOW WATER BE LIMIT OF BALDWIN FORMATION + + + Seer aad REESE EE SSH eee eee e eee eet SEES ESE SHEE e eee eed test Shee EEE EME eee eee ete ee eeerrerrrtes ptt eh te + + p+ 3G ee en; Py oe SEE EEEE EE EEE ee eee eee etree ania fH i ae LIMIT OF TAMWORTH GROUP « dp pe dlig ys Q 0 Tel GRG »H HA qd TH ay, r EEE E EES EH HH EE © te, ¢ | SESE Ee eee tee en | SHH ieee ee ee eee te eets iH i qr Pe tee ee ete eeete + : 1 HH ds far LH DPR wall TM HHS ERT Dg ih cH i t+ tt + + + s ean! ut rH d i HH en ee eV TAREE” VAMC EET a ETE Shee eee eee te eee eee? “TU H Pr LOE POOL GUS Uo PHS Fie. 3 Biosomes and lithosomes in the Tamworth Trough sequence. Outcrop limits of Turi Graywacke, Baldwin Fm., Tamworth Group, Kuttung and Tertiary are shown DEVONIAN AND CARBONIFEROUS SEDIMENTS IN TAMWORTH TROUGH 47 TABLE 2 Stratigraphic Distribution of Sedimentary Structures Shallow Deep Water Structures Ambiguous Structures Water Structures Stratigraphic 3 ao os * a = Z 5 Unit* on § a). o © o) O 2 HS es” Ss F ies eee oe a ene B= 8 ae pee Oh gp 4 Sag £ = 3 F Sete ee ee ) n wi Y nt Pa & om) 3 ® = n 3s a iS 9 a = O HR we ese Sh «@ 8h # fF 2 § A gape F Oo 8 g ee Gee are huey ek | Fe o Css ne se ee See a EG eee OS NO OL Ge rg ® Am as = ais OMe 1A pe eo. ie Be mi Glve: ely oe On © o9 © 8 HAM Tw xg = ic a =) = = = u Qy uy Q 7 (OO S — =, re = a » a Comes oe ere eee eee eo Ft See Ss OS Ue Ut eS oS Soot ia gn eS Soe Ss aoe mn oO & « aan Clp, x Clp, x x Clbs ee x x Clg to Clp,... f x x mip, .: Se t x xX xX t x ae «4 Glp, .. ae r x x x1 1x cigs, .. x Xx xX -% xX Clg to Clp, ei wi x x x ae aX x Clpr ae x Clpu 1 Clpv x Clp, x x x x x x x Clp, aT xe xX Clp io x Clit ie, x x Clbg 4 Clw eal FI Less 96 CT 981 12 G9Z : : ES OST oO8T C6 an 66 an ce ce CCG ANG FI 9LZ qemjs-x dj Axojeq: << GLI ‘¢¢g ‘Z110Y II G9G poom ®djg saoqe “‘ LGU LO &Z MNN OL OFS sjuefq %djQ mojeq ‘ 022 606 09 0ZZ yerys-X Adj[Q saoqe ‘‘ OLT yys ‘Z110Y OT 09% ASeS o9uig. 8Sd. se | GES oGSG 0g as og GL duintS Sd[9 mojeq ‘‘ Og dip oni} cI OST 9 OST qemjs-xX —*djg eaoge © O9L ‘Ore ‘Z110Y GI 0&s SWC em le) ae OFS o0SS OF S LE 00Z dumjS= =idjs, O61 ‘OT ‘Z110Y £3 082 syue[g Se ae ie 98 ‘'99Z F8 S FZ ZLZ poom dig Mojeq 819 = eG, tone Gahvay elu o OL 0 1V Soyer a a’ 5 Olt 5 90INOS WIOI} J0R WOT} sdiq ad AT, UOI}eW ION yuouodur07) suas UOT} ROUrT dip ‘ddy—}e13s-x IO s}soI9 souenbas DID [DUOUIIALP-JUIAAN) A I] XIGNddady 53 DEVONIAN AND CARBONIFEROUS SEDIMENTS IN TAMWORTH TROUGH 8G 866 £9¢ L «+ LST O€1 -O1€ 5 901n0S o6PEG OVE o0LT Wor} qyuouodwo7 ee LSI Q Las Gg rE sulppeq ‘diod i, SoOeFINS GE J 8¢ col Bg Ls O8Z i tPF 61€ ey, Le GGT SE J9 Ls See L0Z eV. 6 OF Sal Say JOeH dip -ddy—ye1}s-xX S M N NM H MS MS HS O¢ CFI OL AS N MN H PL IIT GT OOT 0G ads GY op Sb WIOI} asues DIV [DU0UYIAALP-JUAAAND) panuyuoI—jJ XIGNAddV Gg a duin{s ‘ 89 9G yerys-X . 0Z-ST MN G C9Z sjur[q mt N 8 O8Z orddry : OL GuE ye148-X a 08 Z8Z dunjs ud ag a ay O81 , : 8 MS Z9 O81 . og cl ras) OST ojddry i 06 AN L9 Gol - LG M G9 CFI 1 rere) AN 8G GI ‘[OAUOD) ‘ 06 AS SF StI . CF S OL CVG duin[s - it MN 08 GEZ ms a 09 ‘Z110Y ajddry ie 8 MS #g 8% = SysvO 94NPT 0ZZ ‘TOAUOD i‘ O&Z aiddry 2 cal 0ZZ yerys-X Aud ‘Z110Y 8 Ch atddny - #8 S SL 0G¢g syseo 93n[ % 9G 99 i. qnqd 9g OF 4 MTD OT GZ nt S ST O9T yeI}s-X a} @) LOT ‘Z1IOY sjseo o4npT ce O1g ‘Z110Y POOMm s peq OZE ES ‘Z110Y ‘[OAUOD é °dI9 Q OST squrtd edia) FE M i 0&Z aiddrny a 0Z MN 0z 6G3 syur[q dio GI 0GZ ee cal yeIys-X *dI9 ‘Z110Y POOM 8rdI9 BLN. soyey a ay BAL —-— sdiq odd UOI}EWIIO uOT}eCOUTT IO s}soI9 souenbas Journal and Proceedings, Royal Society of New South Wales, Vol. 97, pp. 55-63, 1963 Petrology in Relation to Road Materials | Part II: The Selection of Rock for Road-making in Australia, with special reference to New South Wales E. J. Minty Central Testing Laboratory, Department of Main Roads, N.S.W., Milson’s Point, N.S.W. AgBstTRAcT—Three factors affecting the selection of rock for use in road-making are discussed, namely distribution, workability and quality. The conclusions are considered to apply to most of Australia. The laboratory test results for over 3,000 specimens have been examined in the Dept. of Main Roads, N.S.W., records, and from typical examples the average test results for 17 types of ageregate have been assessed to decide what types of rock most consistently supply aggregate conforming substantially with specifications. The answer given is 83° compliance for Dolerite, 76% compliance for Basalt and Quartzite, 75% for Microdiorite and 70% for Microgranite, Slag and Limestone. gravel. However, Limestone is rated in this paper as the best for use as artificial road- A modification of the existing approach to specifications is discussed. Introduction The suitability of a rock deposit for use in road-building whether it is intended to be used in the base course or surface course is decided by (i) its position relative to the proposed work, (ii) the workability of the deposit, and (i) the quality of the rock for the specific purpose. It is suggested by the present author that in attempting such an assessment the aim should be to select rock that will give the best service on the road measured in pounds (currency) per cubic yard of pavement with such costs determined not merely on initial cost but rather on the cost spread over a ten-year period including maintenance, the cheapest available material being selected on this basis. Road-building authorities charged with the administration of public funds tend to be over- cautious and accept arbitrary specifications in many cases imported from overseas that are unsuited to Australian conditions in the opinion of the present author. It is true, of course, that the various State Road Authorities are tackling this problem and the Universities show some interest, but at this time the Australian Speci- fications are frequently just echoes of British and American specifications, sometimes out of context, e.g. the Los Angeles test method given in the Australian Standard A77/1957. Some allowance must of course be made for these shortcomings since a start must be made somewhere, and it is only in the last few years that a university has recognized the need for a BB Chair in Highway Engineering, that an Australian Road Research Board has been established, and an Institute of Highway Research started. Graduates of many different kinds are needed to tackle the problems existing, and all of them should have a practical know- ledge of road-building in order to make intelligent contributions, whether they be engineering chemists, engineering geologists or highway engineers. Factors in Selection Relative to the Distribution or Mode of Occurrence of Different Rock Types (1) Aggregate. It is pertinent to consider at this stage what types of rock find the most frequent use and why. In New South Wales the distribution of the principal rock types used for aggregate is set out on the accompanying map (Fig. 1). The most common rock type (quarried basalt) is not the one covering the greatest area. Quartzite, limestone and micro- diorite are the next most commonly used types in that order (Minty, 1960). Basalt is probably more often selected as aggregate on account of its historical use than for any other reason ; but since most basalts in New South Wales are Tertiary residuals, they are usually perched on top of high ground in convenient positions for the establishment of quarries. Geologically older rocks would fre- quently require the removal of overburden in excessive proportions. 56 EA MINTY <= ~~ @WENTWORTH Ae Acknowledgement iw This map is based on the Burecu of Mineral Resources J Geological Map,1952 and the Department of Mines, N.S.W. Tectonic Map, 1960 SN Mainly alluvium. Tertiary River and lake deposits deep leads, diatomaceous earth, etc. h Cretaceous Surface outcrops are mainly sandstone Jurassic Porous sandstone in many areas, shale efc. Triassic Shales and interbedded sandstone. Permicn Moiniy sandstone and conglomerate with interbedded shcles and coal. Carboniferous Tuffs with interoedded lava and conglomerate Devonian Much quartzite and sandstone with interbedded conglomerate and thale,etc. BO Al Silurian Mildly metomorpnosed fine grained sedimentary rocks interbedded with limestone, tuff and lava. fe GZ Ordovician Mainly slote ond quartzite with some Pp pas limestone, tutf and agglomerate. To Proterozoic Metamorphosed sediments of the Tarrowangee Tb series. sp GEOLOGICAL euoG ies SyMe0u TYPE OF ROCK Willyama complex gneisses, granite gneiss etc. Granite ane Grenodiorife. Porphyry Andesite. (Tertiary) Soma Parmian Pa. Basalt (Tertiary) Some Jurassic Jb. Serpentine. PETROLOGY IN RELATION TO ROAD MATERIALS. 8 eae =< e ~ © & CmmOl 10) | 01 N&O eS e cc a fe} fe} ° ° oa oO (oye ?-S. sto} ° fe = pues 0 ° —— Do ° 4 ° ° ° 9-2 5 ——— ORAS. Sai ‘i A ee V4 2 a =< = ~~) ° 2 f S == = a cA o ° re —— é © TEWCASTLE y g = = - x 9 = x fo} GEOLOGICAL MAP OF N.S.W. 50 SCALE OF MILES lice! II 57 58 E. J. MINTY Similarly, quartzite enjoys popularity as aggregate on account of the well exposed outcrops in many parts of the State. The selection of limestone as aggregate is not so frequently due to good exposure. In fact some limestone quarries are in difficult positions subject to the ponding of water, as most limestone in New South Wales is inter- bedded with other Ordovician, Silurian or Devonian rocks. Difficulty occurs when the dip is steep in country of low relief. River gravel is the most common type of aggregate used in New South Wales but is usually of mixed rock types, hence its exclusion from the foregoing discussion. (2) Road Gravel. By “‘road-gravel”’ the engineer means a mixture of gravel, sand, silt and clay in such proportions that the smaller sizes fill the voids between the larger particles, resulting in a dense pavement when compacted. With the exception of limestone, the kinds of rock finding use as “ aggregate ’’ seldom crush to give a well graded mixture of high com- pressive strength such as that required for “ road-gravel’’. On this account and because of the immense quantities of road-gravel required to build an average road, a great variety of naturally-occurring soils find use for this purpose. However, resources of the latter kind are dwindling and other materials are being used. Cement and lime stabilization have extended the range of soils that can be used, but fine-grained soils require the addition of relatively large amounts of cement or lime and therefore do not compete with locally crushed rock for road-making if the winning and crushing costs for local rock are reasonable. This is especially true in the central west of New South Wales where, as shown on the map, rock outcrops are quite extensive. It is possible to see the broad trends in distribution of the various types of road-gravel by examination of the materials map (Fig. 1). These areas may be described briefly as follows : Alluvium—For the most part the areas so described are a wasteland from an engineering viewpoint, containing as they do much “ black ”’ clay soil. However, in the Riverina there is a remarkable system of old streams (David, 1932; Langford Smith, 1960; Butler, 1956) no longer flowing but containing enormous resources of sandy loam suitable for road- building. Some useful deposits of this kind have also been found between Warren and Collie, Warren and Nyngan, out from Nyngan and Forbes, and near Coonamble. In most cases where they have been rivers fine wind-blown sandhills derived from these sediments are found nearby. In “Soils of the Macquarie Region” the C.S.I.R.O. (1955) has described the soils of the plain through which the Macquarie River wanders. Another soil survey (Water Conserva- tion and Irrigation Commission) supplies some useful information near Nyngan. Shale—While true shales only outcrop extensively in the Wianamatta basin, they are interbedded with other sedimentary types in the basins of Devonian, Carboniferous, Permian and Jurassic age. Their use for roads depends firstly on the outcrop being reasonably free of overburden. Sometimes they are exposed in the saddles of Devonian hills or on the escarp- ment of Devonian, Carboniferous and Permian strata. Thus, on the map the areas shown as mainly sandstone and mainly quartzite will be found to contain shale which may be of use in road works. Sandstone—Although Telford base courses are a thing of the past, sandstone crushed to about 4 in. size has been used in road construction in recent years near Gosford. (It can be handled just as road-gravel and is reduced to a Macadam- like grading simply by rolling.) Sandstones sometimes are found broken down to a good road-gravel through soil forming processes, but around Sydney the sandstone is too even grained to produce well graded soils. Somewhat gritty sandstone soils and partly decomposed sandstone have been used along the Hume Highway in Wingecaribee Shire, near Mt. Victoria on the Great Western and north of Dubbo on the Newell Highway. These beds all outcrop near the edge of sandstone areas and are basal beds once fed by vigorous streams. Although there is some conglomerate rock in these areas many of the pebbly gravels used for road-gravel such as those near Robertson and Mittagong are alluvium eroded from the basal beds and redistributed by river action, later covered by basalt flows and only now exposed in part by erosion (Plate I). Quarizite—Quartzite is widely distributed, particularly in the Upper Devonian, but seldom provides road-gravel. Such deposits however are not unknown in areas where the topography is conducive to the formation of deep colluvium such as the area between Rylstone and Cudgegong. Conglomerate —- Suitably decomposed _ con- glomerate of various geological ages finds use PETROLOGY IN RELATION TO ROAD MATERIALS. II 59 as road-gravel in widely scattered areas of the State. Limestone—When used, limestone is generally crushed but sometimes gives rise to Kunkar, which finds use as road-gravel near Gunning- bland, Wentworth and between Menindee and Broken Hill. Crushers at Marulan, Ilford, Molong, Forbes, Galong and elsewhere have supplied good artificial road-gravel. Slaty Rocks—A variety of rock types is embraced by this description. By slaty is meant any metamorphosed sedimentary rock which has closely spaced cleavage, joints and bedding arranged in different planes such that angular fragments are derived on disturbance of the rock. Slaty rocks have been much used as road-gravel in New South Wales and their use will certainly increase as they are not only widespread but supply deep deposits, of both colluvium and rock. Granites and Porphyries—Amongst this class only granite soil or regolith is normally used for road-gravel and not the rock, the porphyries rarely find use because they tend to form erratic deposits. Tuffs—Are not much used, although tuffaceous slates are used. Basalts and other basic igneous rocks are crushed and used as road-gravel but do not form deposits of good natural road-gravel. In fact basalt more often spoils than provides good gravel. Such spoiling is of course due to the formation of rich soils (usually red). Dolerites and Miucrodiorites—Decomposed rocks of these types have been used in rare cases, but could not be regarded as good road-gravels. Pebbly Alluvium—Whilst much used for road- gravel, when suitably graded, this class of material is difficult to record on a generalized map. Laterite—This material also supplies extensive road-gravel deposits, notably along the coast, but being superficial has not been shown on the map. Factors in Selection Relative to the Workability of Rock (1) For Aggregate. The ease of winning and the ease of crushing are the principal factors. River gravels are won simply by digging or dredging. However, winning generally means drilling, blasting, loading and transport to the crusher. Hard rocks are the more costly to drill except that very open joints filled with soft decomposition products can provide a hazard in rock of any hardness. Blasting is generally assisted by incipient joints but is hampered by open joints. Loading and transport are primarily assisted by the quarry face being above the crusher, and secondarily by the size of the blocks dislodged by blasting being of optimum size. The latter is governed by the closeness and pattern of jointing in the rock as well as the pattern and type of charge. So it is that the difficulty of winning the more commonly used rocks is on the average in the order microgranite, microdiorite, granite, quartzite, dolerite, basalt and limestone, assum- ing that all are situated in similar topographic locations. However, there are some cases (Plate I) in which the jointing is so well developed that the rock can be dislodged from the face with a power shovel, thus saving drilling and blasting and also speeding up loading. This is a similar category to river gravel and has applied to weathered conglomerate, slaty lmestone and extremely jointed basalt in certain New South Wales quarries. It is to be expected that some quartzites and cherty slates would fall into this category. The difficulty of crushing (W) is probably proportional to the product of the size of blocks (S) won from the deposit and the load (fF) required to produce 10% of fines (D.5.1R., 1959) from rock of the type being crushed, divided by the average size (a) of aggregate produced. That is, Wecla ls} where c is a constant. (2) For Road-Gravel. The natural road-gravels are of course the cheapest to win and require little or no crushing. In the rocks used as artificial road-gravel there is a gradation from the aggregates discussed above into types only suitable for use as road-gravel. Jointing, bedding, shear planes and grain size all influence workability. The ideal materials are those which are sufficiently fissile to be quarried by machine (ripper or shovel) and such that the blocks are not above 9 in. on the largest dimension of the maximum sized pieces, with an average of 3 in. or less (Plates II and III). Usually such material can be broken down to an artificial road-gravel by special rollers (grid or cleated). The slaty rocks frequently follow this pattern. Shales, sandstones and conglomerates are more difficult, shales and sandstones generally on E. J. MINTY e[qeIIsep 9-0 pue ‘uljy ®& se F-0 Sszos (‘3suq MTS) sey ynq poydope 304 ‘sods ‘ysny ON quavayfao9 aunts PaYystjod pee SaG ysysug 60 VSN ane: 08-0 Yo = 0F-0 %oG peyrey aaey oulOs (489) $-0 %9 = 0-0 Yo ay %8 as % I =a L¥-0 “oF oe £6 -0 = % I 1F-0 = 70% (Q0UspIAZ PIey uo gg-o0) 9F-0 = Ye UeY} SSO] = Ye ULY} SS] aa %8 Ae = Ioyyne oy} Aq poses %OT -8ns %c¢ 4ynq UINUWITXP IL osn Ur wor} -eoytoeds ON SUOT}IPUOD (patquinsz9 %) Sag cd Yn awsarssap payvos suysa Aq ssaupunos ewisI}x9 Iopun uUuoysIAy 0 quaryffao7D ell (umopyeoiq %) ssaupunos aqwwydjns UntposS %OE UINUWIIXP I (%0% ueqy sso] OUuIOS) , * 40 (OF-0Z 95UeI) BZ a fd %001 (68-€1 e5ue1) ZZ — (ezep yuetoygnsut) (¢Z) a % % 86 (SI-€I osue1) ET % ‘e « JSP (8Z-8I os8ueI) EZ a ie %00T (6E-1€ esueI) FE — (ezyep yUoToysFnsut) (PF) e i $6 (Zo-FI o8ue1) LT fa s %E8 (OF-ZI osueI) EZ i. gE & YoSL (¢Z-§I osueI) [Z es - %00T (FP-FZ odueI) OF A “ « Jo89 (IZ-6 osuUeI) CT - sa %8F (GZ-gI asue1) [Zz a S GL (GI-II esue1) GT is %00T (LI-GIT o8ue1) 9] ie Gs % 66 (ZZ-9I osueI) BT re} YIM pozeoo-o1d =ssajun %oQOT (Gh-9[ osueI) Ze sada I. %0Z UINWIXP] (soootd Ayep jo %) xXapuy SSOULYD] + BRIS JoArin I9AIl poysnig 4STYIS eINIDIG OIUPITO A, oU0SOWITT leyuny axyoemAdIry S[oJUIOFT 9}1zj1eNC) 9}P1S zj1eNC) y[eseq ahah 8c) (oq | 9}IOTPOTOTIAT oy [oAyYy IPIULISOIONL opUeID yIoYy snowy sof synsay ysazt qooday 9}91NUO0N UT osn Jo oyjel} YS] Io} Gg Jo “xeW=9 LZ JO -xeW=q SUOT}IP -u090 OUJe1} ssuap IO} 0G JO “XPW=V (ustIN}IG 0} o10Yype 0} sprey yorum) sat surddiys avid (uoIseiqy pure qoedwiy Aq sso7%) sajasup sot STUTT: uoyvoy19adS 109044 sa. suoywoyivadsS ypim papsvrquon sada y yooy juasaffigq sof synsay jsaz word ] ATAVL PETROLOGY IN RELATION account of being of too large a dimension when quarried but breaking down too much during rolling, conglomerates because they tend to resist rolling unless the cobbles are of glacial origin and consist of sandstone, slaty or shaly rock. Porphyries (microgranite, microdiorite, etc.) are sometimes jointed well enough to find use, but are not usually easy to win. Thus fissility, not hardness, is the guide to relative workability. Size and Uniformity of Depost A deposit of fissile rock should only be considered if more than 10,000 cu. yds. of relatively uniform material is available, since the cost of transporting heavy plant could otherwise make the cost per ton excessive. Well tried sampling procedures are available, e.g. Dept. Main Roads Manual No. 3. Factors in Selection Relating to Quality It is necessary to differentiate first according to the purpose for which the rock is required, because the qualities for aggregate are quite different from the qualities required for road- gravel. Aggregate Whilst aggregate may be used with either bitumen or cement, it is the good all-round aggregate which must be given the highest merit, as shown in Tables 1 and 2. It is not easy to give a simple answer on the question of aggregate quality because many of the specifications set are conflicting. Also, nature does not allow all rock types to conform equally with man-made requirements. However, the following table (Table 1) has been devised by the present author with the intention of attempting to point the way to selecting the best available aggregate in an area when establishing a new quarry. The averages are based on an examination of the records for over 3,000 aggregate specimens, data for a selection of typical samples being set out in a thesis by the present author (Minty. 1960) and in a recent paper by West and Ross (1962). By rating the average test results for aggregate types as set out in Table 1 for each property of interest to the engineer so that complete compliance with typical specifications scores one unit for each test and_ proportional compliance is similarly rated, the following sequence (Table 2) is obtained for the rock types TOTROAD MATERIALS. If 61 most frequently quarried in New South Wales but omits some which are not available or are not now quarried, in New South Wales. The author considers the present specifications are illogical. For example, a basalt having a Los Angeles loss of 27° is an inferior material even though it complies with the specification for bituminous surfacing aggregate to be used on roads carrying moderate traffic densities in New South Wales and Victoria. It is inferior because any respectable basalt belongs in the class interval 9 to 21 Los Angeles loss (Minty, 1960). Classes of rock suitable for use on a State highway carrying a certain volume of traffic could replace the blanket figure and a specification could be set for each rock type. This is not as complicated as it sounds. TABLE 2 List of Aggregate Types in Order of Quality Assessed on the Average Test Results in Lable i 20, Rock Type Compliance with Specifications Dolerite 83% Quartzite 10%, Basalt Microdiorite 75% Microgranite Slag 10%, Limestone Granite 67% Slate Crushed River Gravel 64% Volcanic Breccia 52% Hornfels 48% Quartz 40% Kunkar 21°, In regard to the polishing of aggregate, the anomalous behaviour of “ high class ”’ aggregate is serious when the latter judgment is made on the Los Angeles Test result, since the 20% maximum figure for Los Angeles loss tends to exclude many rocks which are less prone to polishing than the tough fine-grained materials such as basalt, which are most prone and which in the main pass the 20% limit. Fortunately remedial measures and alternate methods of use are now available (West and Ross, 1962) as foreshadowed in Part I of this paper (Minty, 1959). It is hoped that these comments will lead to specifications being set in such a way that a better balance between conflicting limits is obtained. For use in bituminous surface treatment a better balance between aggregate performance 62 E. J. MINTY and specifications could be obtained by putting the main emphasis on the susceptibility of the rock to polish so that the specification would become : Heavy Traffic Conditions Los Angeles Loss—Microdiorite, Dolerite, Quartzite 25°, maximum on B grading or equivalent one sized counterpart. Coefficient of Friction after 12 hours laboratory polishing (wet)—0-45 minimum (as per West and Ross, 1962). Siripping to be curable by the use of pre- coating agents such as creosote or tar, with not more than 2% of stones crumbling during the stripping test. (D.M.R. method.) Flakiness Index—25°, max. Normal Traffic Conditions Los Angeles Loss—(B grading or equivalent one sized) Basalt max. 20% Slag max: 25%, Volcanic Breccia max. 20% | In addition Limestone max. 28% | to the Granite max. 3d% above Crushed River Classes Gravel max. 25% Slate max. 25% Coefficient of Friction after 12 hours polishing— Laboratory result not to be less than 0-4. Siripping to be curable as above, or with dehydrated tar in the bitumen. Crumbling when being removed during stripping test, TINA ONY Ge Flakiness Index—max. 30%. Light Traffic Conditions Any rock type having a Los Angeles loss of not more than 45° providing stripping can be cured with precoating or additives in the bitumen and having a flakiness index less than 35% and accelerated polishing coefficient of friction more than 0:3. The foregoing proposals for a specification are intended to apply to aggregate for use in bituminous surface treatment work. For bituminous mixtures (sometimes described as asphaltic concrete) it is not necessary to place the emphasis on the tendency of the aggregate to polish as revealed by tests for the coefficient of friction. Aggregate as specified for either heavy or normal traffic would be satisfactory providing sharp quartz sand was included in the mix and the latter tested to give not less than 0-45 coefficient specified for heavy traffic. Actually in respect of skidding accidents legislation to require suitable fillers in tread rubber of motor tyres would be more beneficial than stringent specifications for aggregate, as shown by Table V in Part I of this paper. In Portland cement concrete, aggregate should, in the author’s opinion, comply with the Los Angeles, flakiness index and soundness requirements of either heavy or normal class aggregate for bituminous surface treatment and in addition should be reasonably free of opal, chalcedony or similar minerals likely to affect cement-alkali reaction. Road-Gravel The specifications for this type of material, which finds use in the base course of roads or on unsurfaced roads, usually call for a granular mixture of different sized particles such that each succeeding size just fills the void space in the preceding size and having as the terminal member of this series sufficient material finer than 0-:0135 mm. diameter to act as a binder. To avoid lack of stability due to excess lubrica- tion by the silt-clay fraction, limits are set for consistency tests whilst to ensure adequate dry cohesion a minimum dry compressive strength test figure for compacted road-gravel is laid down (Britton, 1947). , Apart from natural mixtures of gravel-sand- silt and clay finding use as road-gravel, crushed rock is now finding increasing use. When the crushing is done by a stationary crushing plant it is usually done in conjunction with the production of aggregate from fresh rock so that the product usually lacks sufficient cohesion. Taking into account rock quarried by ripping or similar techniques followed by crushing with road-plant such as cleated or grid rollers (Plate III) the type of rock usually yielding the best quality product is limestone. However, slate, volcanic breccia and some dolerites and basalts are also worth considering, providing due care is taken to blend in cohesive material to fill the voids in the sand sizes without increasing the plasticity too much. Acknowledgement The author wishes to thank Mr, Javagel: Shaw, Commissioner for Main Roads, for permission to utilize the Department’s records in the preparation of this paper. Thanks are also due to Mr. N. W. West, Mr. T. Ross and many of the Department’s geologists for useful discussion of the subject matter, and to Mr. F. Mullin for reading the manuscript. 7 - JOURNAL ROYAL SOCIETY N.S.W. MINGY, PLAT Eat r . i Fe JOURNAL ROYALE SOCTE EY IN SW Ee ae te ees MINTY, PA MOORNAE ROYAL SOCIETY N.S.W. VEEN TT YOR PEA ie 2h of . “aie % a PETROLOGY IN RELATION TO ROAD MATERIALS. II 63 The opinions expressed are those of the author and do not necessarily reflect the views of the Department of Main Roads, New South Wales. References Britton, A. T., 1947. Design of Non-Rigid Pave- ments. Hwy. Res. Bd. (U.S.A.). ButT._er, B. E., anD Mutton, J. T., 1956. Parna in the Riverine plains of South Eastern Australia and soils thereon. Aust. Journ. Agric. Res., 7, 556-563. : C.S.I.R.O., 1955. Soils of the Macquarie Region. Soil. Pub. 4. Davip, T. W. E., 1932. Explanatory notes to accompany a new Geological Map of the Common- wealth of Australia. C.S.I.R. publication. DEPARTMENT OF MAIN Roaps, 1951. Manual No. 3. DEPARTMENT OF SCIENTIFIC AND INDUSTRIAL RESEARCH (ENGLAND), 1959. Roadstone Test. Data prc- sented in tabular form in Road Note No. 24. LANGFORD-SMITH, T., 1960. The Dead River Systems of the Murrumbidgee. Geog. Fev., 1, 3, 368-389. Minty, E. J., 1959. Petrology in Relation to Road Materials. Part 1. The Rock Types used to produce ‘Aggregate’. J. Proc. Roy. Soe. N.S.W., 93, 27-37. Minty, E. J., 1960. ‘‘ The Physical Properties of Aggregates used for roadworks in N.S.W. in relation to their petrological characteristics.” Thesis, University N.S.W. WEsT, N. W., AND Ross, T., 1962. Surfaces in N.S.W. Aust. Conference. Polishing of Road Road Res. Bd., Ist (Received 8 October 1962) Ex planation of Plates PLATE I 1. Pebbly alluvium of Tertiary age exposed by landslip erosion, between Mittagong and Robertson. 2. Columnar basalt, Mt. Tomah. flannel flowers in the top right-hand corner. Note the separation of the joints by weathering. Scale is denoted by the PLATE II 1. Well developed joints in slaty rock on the South Coast. 2. Anticlinal structure in Ordovician rock west of Forbes, N.S.W. Note the power-shovel used for winning the interbec ded slaty rocks (limestone and slate) and the relatively large size of fragments in the foreground. PLATE III 1. Devonian red shaly sandstone from Speck’s Gap, Jemalong Shire, won by ripping with a Michigan ‘dozer. Experimental work by Jemalong Shire in 1961. 2. This shows the result of four passes of a grid roller on the large blocks in the picture above. foreground had received eight passes of the roller. The lane in the Journal and Proceedings, Royal Society of New South Wales, Vol. 97, pp. 65-72, 1964 The Geology of the Carroll-Keepit-Rangari Area of New South Wales A. H. VotsEy AND K. L. WILLIAMs* Department of Geology, The University of New England ABsTRACT—The rocks comprising the Belvue Basin which lies on the same synclinal axis as the Werrie Basin in the western part of the orogenic belt of north-eastern New South Wales, have been mapped, and defined in terms of the Australian Code of Stratigraphical Nomenclature. In particular, the Tulcumba Sandstone Formation with its important Rangari Limestone Member at the base of the Carboniferous section has been recognized and described. Introduction This paper is the outcome of work done by K. L. Williams as part requirement for the degree of Bachelor of Science with Honours at the University of New England during 1954 under the supervision of A. H. Voisey. Mapping was carried out in the first instance on parish maps. The information was later transferred to aerial photographs and mosaics supplied by courtesy of the New South Wales Department of Lands. It has since been augmented by further field work done by the senior author and members of the Geology Department. B. A. Engel and J. W. Pickett mapped the adjacent area to the north. K.S. W. Campbell examined some of the sections and collected a number of fossils, the descriptions of which will be published elsewhere. The area embraces the country between the Baldwin Range, west of Manilla and the southernmost extension of the Nandewar Range. It includes portions of the counties of Nandewar, Darling and Buckland and is covered by the photographic mosaics (Gunnedah _ sheets B and D, Attunga sheets A and C, and Boggabri sheet D). The northernmost part of the Werrie Basin was included so that the formations might be defined in relation to those mapped so well by S. W. Carey (1934 and 1937). One of the authors (A. H. Voisey) was shown over the Werrie Basin by Carey in 1933 and was aware of the fact that he had mapped boundaries of * Now at the School of General Studies, The Australian National University. rock formations in a manner not at variance with the principles set down by the Code of Stratigraphical Nomenclature which was later introduced (Raggatt, 1956). To give formation names now to replace the old serial ones surely should not depend upon remapping the whole of what has been regarded as the most accurately mapped Carboniferous area to which the old names of Burindi and Lower and Upper Kuttung serial names were applied. In fact, although the boundaries of rock units made originally on parish maps were checked in a number of places in the field, changes in Carey’s map are few. The writers would claim to have been sufficiently well acquainted with the rocks in the field to qualify them to apply new names based upon the places where the units were originally recognized. One of the writers (A. H. Voisey) has had the mapping of the Werrie Basin revised using the units now being defined to produce one inch to the mile map sheets of the areas south of the map in this paper. Carey’s descriptions of the units have been sufficient for the writers to recognize them in the field and to map them in the adjacent areas. It was thought unnecessary to repeat descrip- tions of the various units since these were originally given by Carey. Moreover, use of his papers assists workers to place their units in relation to the local time-rock terms such as Burindi and Kuttung and brings new work into line with the old. The structures lie in the Western Belt of Folds and Thrusts and are adjacent to the Border Thrusts of the New England orogenic belt (Voisey, 1959, p. 192). 66 A: H. VOISEY AND KY Laie erAMs COLUMNAR SECTION SHOWING CARBONIFEROUS ROCK UNITS IN| THE WERRIE ~ BELVUE BASINS FORMATION NAME SECTION FEET DESCRIPTION CAREY'S SERIAL NAME UPPER Tillites GLACIALS Conglomerate INTER CURRABUBULA eect | GLACIALS KUT TUNG Vorves FORMATION LOWER Tillites GLACIALS UPPER Gritty Tuffs Conglomerate ON ON RA Conglomerate with Boulders DUR! ANDESITE MEMBER Andesites and Felsites Gritty ond Pebbly Tuffs HILL 60 MEMBER Oolitic Grits ond Conglomerates Gritty Tuffs MERLE WOOD SWAINS GULLY SSTONE MBR [2c ussnicoo nr nn Sondstones WOODLANDS ANDESITE MBR ees | Biotite Tuff and Andesite B KUT TUNG FORMATION BABBINBOON CONGLOM. MBR Coarse Conglomerate Pebbly and Gritty Tuffs LOWER Coarse Conglomerates Pyroxene Andesite Tuffs and Conglomerates | NAMOI | FORMATION | | | TULCUMBA SANDSTONE RANGARI LIMESTONE M BR COLUMN = 12,110 FEET. wie, II GEOLOGY OF CARROLL-KEEPIT—RANGARI AREA, N.S.W. 67 The earliest references to the geology of the area followed visits by Professor T. W. E. David and the Government Geologist E. F. Pittman early in the century. H. I. Jensen (1907) made a study of the Nandewar Mountains and assigned most of the strata to the Carboniferous, Devonian rocks not having been recognized in the vicinity at the time. The foundation upon which later work has been based was laid by W. N. Benson (1913 ef seg.), who mapped the area between Warialda and Nundle. A. C. Lloyd (1933) conducted a reconnaissance of the area and S. W. Carey (1934, 1935, 1937) dealt with the stratigraphy of the Werrie Basin which lies immediately to the south. F. N. Hanlon (1948) included the western portion of the area in Part VI of his “‘ Geology of the North Western Coalfield ”’. Since completion of the mapping the Keepit Dam has flooded a large part of the country approximately in the centre of the map (Fig. 3). Devonian Stratigraphy MANILLA GROUP The division of the Upper Devonian sequence or “‘ Barraba Series ”’ (David, 1950, pp. 251-252) has been discussed recently by K. A. W. Crook (19615, p. 192) and B. C. Chappell (1962, pp. 66-69) following Voisey’s interpretation of W. N. Benson’s divisions in the Manilla-Barraba region (1958), pp. 209-210). The relationships between the units in the Manilla Group are different on the opposite sides of the Belvue Syncline. As the results of field work, at present in progress throughout the Nundle-Warialda belt, are required before the problem can be resolved, the Manilla Group is marked as “ undiffer- entiated ’’ on the map (Fig. 3). The Keepit Conglomerate and Borah Limestone are tentatively regarded as members of the Mandowa Mudstone. One or both could assume formation status later. Although it is possible that the lowest parts of the Devonian sequence could extend below the base of the Manilla Group into the Tamworth Group (Crook, 1961a, p. 176), final confirmation is required from T. B. H. Jenkins, who is concerned with detailed mapping of the area west of Keepit Dam. Keepit Conglomerate Member. From the Merlewood Section, Carey (1937, p. 349) described the Upper Devonian beds as becoming progressively more bouldery and culminating in a very variable bed about 800 teet thick, best described as an agglomerate. Some phases, however, are true conglomerates with well-worn boulders of andesitic lava. In places the matrix is entirely tuffaceous. This horizon can be traced to the Keepit Dam and for some miles north of it where it gradually breaks up and the conglomerate phase disappears. This unit is here defined as the Keepit Conglomerate member. It is separated from the Tulcumba Sandstone by a variable thickness of mudstone which is characterized by abundant specimens of Leptophloeum australe. This mudstone is well exposed, in the gutter on the north of the road west of the Keepit Road turnoff from the Oxley Highway, where it is 200 feet thick. The Borah Limestone has not been found within this part of the sequence. Borah Limestone Member. The Borah Limestone was named by J. W. Pickett (1960, p. 237) after its occurrence in the valley of Borah Creek, near the bend in the road shown in the north-east corner of the map (Fig. 3). Unfortunately faulting prevented him from placing it in position in a sequence in the type locality, but it is the same limestone which has been found at intervals along the broken eastern limb of the Belvue Basin. It occurs below the mudstones which underlie the Tulcumba Sandstone and above somewhat similar mudstones rich in Leptophloeum australe. Its position is thus near the top of the Upper Devonian Manilla Group. The limestone is fine-grained, blue grey in colour, weathering to white and it contains crystallized radiolarian tests and _ euhedral crystals of an unknown mineral which has been replaced by a mosaic of albite and calcite. The bed in the type area is only 3 to 4 feet in thickness. Pickett described a new species of clymeniud, Cymaclymenia borahensis which has been found abundantly in the northern occur- rences of the limestone. Carboniferous Stratigraphy The Carboniferous rocks of the Werrie Basin were excellently mapped by S. W. Carey (1934, 1935, 1937) before the Australian Code of Stratigraphical Nomenclature was introduced. It is proposed here to give names to the units which he mapped which conform to the Code, and to define them in relation to the sections which he measured. Consequently, this publi- cation should be read in conjunction with Carey’s papers on the Werrie Basin. The names used for the formations have been chosen from geographical names mentioned by him and are indicated on the columnar section (Fig. 1). 68 A. H. VOISEY AND K. L. WIELTAMS WEST Bie: The legend of Carey’s Geological Map of the Werrie Basin should be amended as below and the units shown on it will then conform to the Code. Carey’s Legend Proposed Amendment Alluvium Werris Creek Coal Measures Werrie Basalts Willow Formation Currabubula Formation Merlewood Formation Namoi Formation together with Tulcumba Sand- stone Manilla Group Coeypolly Conglomerate Acid Lavas Hornblende Andesite Pyroxene Andesite Warrigundi Intrusives Tertiary Basalt Alluvials Upper Coal Measures Werrie Traps Lower Coal Measures Glacial Stage Lower Kuttung Burindi Series Barraba Series Porphyry Boulder Horizon Acid Lavas Hornblende Andesite Pyroxene Andesite Warrigundi Intrusives Tertiary Basalt The same units as far as they have been recognized are shown on the present map (Fig. 3), which extends knowledge of their outcrops to the north-west of the Werrie Basin. The Merlewood Formation has a number of important rock units, some of which are shown on Carey's map (1937, plate XVIII). These are (in descending order) : Duri Andesite Hill 60 Member Swain’s Gully Sandstone Member Woodland’s Andesite Member Babbinboon Conglomerate Member Myall Camp Conglomerate Member. K . aE. CK. =) i ale WELL CK. SKETCH SECTION 9 The Myall Camp Conglomerate and Babbin- boon Conglomerate can be seen beside the andesites in the south. The Woodlands Andesite peters out to the north with the Babbinboon Conglomerate. The Swain’s Gully Sandstone and Hill 60 Member are stippled. The Duri Andesite is more prominent on the eastern limb of the Werrie Basin and can be recognized as being the major pyroxene andesite which shows ~ prominently on Carey’s map (1934, plate XVII). The stratigraphical units will now be defined in the manner suggested by the Australian Code of Stratigraphical Nomenclature (Raggatt, 1956). TULCUMBA SANDSTONE Derivation: Parish of Tulcumba, County of Nandewar. Type Section: Swain’s Gully, described as Merlewood section by Carey (1937, p. 350). Lithology : Cross-stratified felspathic sand- stones, conglomerates, dark blue marly mudstones, tuffs and oolitic limestones. Thickness : Type-section 700 feet is in Swain’s Gully and includes 400 feet of Carey’s “basal series’’ and 300 feet dark blue marly mudstone sand tuffs. RANGARI LIMESTONE MEMBER Derivation: Rangari Station, parish Rangari, County Nandewar. Type Section: Along Manilla-Boggabri road, one mile east of Rangari Homestead. \ GEOLOGY OF CARROLL-KEEPIT-RANGARI AREA, N.S.W. 69 BELVUE BASIN. ACROSS THE BELVUE BASIN. Vert. Sc. | Hor. Sc. | Fic. 2—continued Lithology: Oolitic limestone clastic. Thickness : Type-section 15 feet, lensing south- ward and not reaching the type-section of the Tulcumba sandstone at Merlewood. in part bio- The basal unit of the Carboniferous sequence, the Tulcumba Sandstone, differs considerably from the underlying Devonian mudstone con- taining Leptophloeum australe and regarded as typical of the Manilla Group. In the type section Carey noted that the unit started with a basal conglomerate with boulders of granite, hornfels and porphyrite measuring as much as ten inches in diameter. The overlying buff- coloured sandstones are current-bedded—a characteristic which enables the Tulcumba Sandstone to be recognized for many miles to the north. The typical sandstone consists almost entirely of quartz and feldspar, the latter predominating. In addition, there are fragments of felsitic rock and occasional flakes of biotite. The cement is mostly clay but in some places calcite is important. Sorting and rounding of the fragments is good. The presence of the gritty phase is mostly due to the felsitic rock fragments which attain a maximum diameter of 2 mms., whereas the mean diameter of the sandstone phase is seldom greater than 0-5 mm. The Rangari Limestone member which has not been found in the Swain’s Gully section is well exposed on either side of the Tamworth- Gunnedah road near the Keepit Dam turnoff. Here it is 15 feet thick and is 20 feet below the top of the sandstone formation. It outcrops continuously to a short distance beyond the northern boundary of the map. K. S. W. Campbell (verbal communication) remeasured the Swain’s Gully section and has extended the thickness of the Tulcumba Sandstone unit to 700 feet including the Cladochonus tenuicollis and Phillipsia sp. bed. The Tulcumba Sandstone thins northward and beyond the Wean-Manilla road (north-east of Rangari Homestead) it is only 250 feet thick. The Rangari Limestone, here is 10 feet in thickness and commences 50 feet from the base of the formation. Another limestone lens 15 feet thick, composed largely of bioclastic materials and containing 2 feet of very fossil- iferous siltstone, occurs near the top of the sandstone. In thin section the Rangari Limestone is seen to consist largely of detrital feldspar or felsitic rock fragments. Quartz is absent or poorly represented. The feldspar is in the ADgo-Angg to Ab,z-Ang, range and is mostly Ab,,-Ang, in composition. The oolitic portions consist of minute nuclei and accretionary calcite set in a dominantly crystalline calcite matrix. The nuclei are, for the most part, small fragments of euhedral feldspar or fossil debris. Namo! FORMATION Synonymy : Burindi Series (in part) (Benson, 19156), Lower Burindi Group (in part) (Voisey, 1952). 68 A, H. VOISEY AND K. L. WILLIAMS KELVIN Fic. The legend of Carey's Geological Map of the Werrie Basin should be amended as below and the units shown on it will then conform to the Code. Carey's Legend Proposed Amendment Alluvials Upper Coal Measures Werrie Traps Lower Coal Measures Glacial Stage Lower Kuttung Burindi Series Alluvium Werris Creek Coal Measures Werrie Basalts Willow Formation Currabubula Formation Merlewood Formation Namoi Formation together with Tulcumba Sand- stone Manilla Group Coeypolly Conglomerate Acid Lavas Hornblende Andesite Pyroxene Andesite Warrigundi Intrusives Tertiary Basalt Barraba Series Porphyry Boulder Honzon Acid Lavas Hornblende Andesite Pyroxene Andesite Warrigundi Intrusives Tertiary Basalt The same units as far as they have been recognized are shown on the present map (Fig. 3), which extends knowledge of their outcrops to the north-west of the Werrie Basin. _ The Merlewood Formation has a number of important rock units, some of which are shown on Carey's map (1937, plate XVIII). These are (in descending order) : Duri Andesite Hill 60 Member Swain’s Gully Sandstone Member Woodland’s Andesite Member Babbinboon Conglomerate Member Myall Camp Conglomerate Member. SKETCH SECTIQl 2 The Myall Camp Conglomerate and Babbit boon Conglomerate can be seen beside tle andesites in the south. The Woodlands Andesite peters out to the north with the Babbinbow Conglomerate. The Swain's Gully Sandstott and Hill 60 Member are stippled. The Dun Andesite is more prominent on the eastern lim of the Werrie Basin and can be recognized # being the major pyroxene andesite which shol® prominently on Carey's map (1934, plate XVII) The stratigraphical units will now be define! in the manner suggested by the Australias Code of Stratigraphical Nomenclature (Raggatt 1956). TuLcuMBA SANDSTONE Derivation: Parish of Tulcumba, County o! Nandewar. Type Section: Swain’s Gully, described ® Merlewood section by Carey (1937, Pp. 4 I Lithology: Cross-stratified felspathic 4" stones, conglomerates, dark blue mal mudstones, tuffs and oolitic limestones: Thickness : Type-section 700 feet is in Swai Gully and includes 400 feet of Cate) “basal series” and 300 feet dark blue m4 mudstone sand tuffs. RANGARI LIMESTONE MEMBER Derivation; Rangari Station, parish Range County Nandewar. caf Type Section: Along Manilla-Boggabri 1°’ one mile east of Rangari Homesteae \ GEOLOGY OF CARROLL-KEEPIT-RANGARI AREA, N.S.W. - 69 BASIN. BELVUE ACROSS THE BELVUE BASIN. Vert Se I Hor. Sc. | Fic. 2—continued Lithology: Oolitic limestone clastic. Thickness : Type-section 15 feet, lensing south- ward and not reaching the type-section of the Tuleumba sandstone at Merlewood. in part bio- The basal unit of the Carboniferous sequence, the Tuleumba Sandstone, differs considerably from the underlying Devonian mudstone con- taining Leptophloeum australe and regarded as typical of the Manilla Group. In the type Section Carey noted that the unit started with a basal conglomerate with boulders of granite, hornfels and porphyrite measuring as much as ten inches in diameter. The overlying buff- coloured sandstones are current-bedded—a characteristic which enables the Tulcumba Sandstone to be recognized for many miles to the north. The typical sandstone consists almost entirely of quartz and feldspar, the ‘ater predominating. In addition, there are fragments of felsitic rock and occasional flakes Of biotite. The cement is mostly clay but in Some places calcite is important. Sorting and Tounding of the fragments is good. The presence of the gritty phase is mostly due to the felsitic Tock fragments which attain a maximum diameter of 2 mms., whereas the mean diameter ee sandstone phase is seldom greater than *D mm. a The Rangari Limestone member which has Hot been found in the Swain’s Gully section Well exposed on either side of the Tamworth- ‘mnnedah road near the Keepit Dam tumoff. Here it is 15 feet thick and is 20 feet below the top of the sandstone formation. It outcrops continuously to a short distance beyond the northem boundary of the map. K. S. W. Campbell (verbal communication) remeasured the Swain’s Gully section and has extended the thickness of the Tulcumba Sandstone unit to 700 feet including the Cladochonus tenurcollis and Phillipsia sp. bed. The Tulcumba Sandstone thins northward and beyond the Wean-Manilla road (north-east of Rangari Homestead) it is only 250 feet thick. The Rangari Limestone, here is 10 feet in thickness and commences 50 feet from the base of the formation. Another limestone lens 15 feet thick, composed largely of bioclastic materials and containing 2 feet of very fossil- iferous siltstone, occurs near the top of the sandstone. ; In thin section the Rangari Limestone is seen to consist largely of detrital feldspar or felsitic rock fragments. Quartz is absent or poorly represented. The feldspar is in the Abgp-Anyo to Abyo-Ango Tange and is mostly Abgs-Angs in composition. The oolitic portions consist of minute nuclei and accretionary calcite set in a dominantly crystalline calcite matrix. The nuclei are, for the most part, small fragments of euhedral feldspar or fossil debris. Namor FoRMATION Synonymy : Burindi Series (in part) (Benson, mt 19150), Lower Burindi Group (in part) (Voisey, 1952). 70 A. H. VOISEY AND K.-L.) WIELIAMS Type Section: Swain’s Gully, described as Merlewood Section by Carey (1937, p. 350) as “typical Burindi facies ’’. Lithology : Mudstones, limestones, sandstones and conglomerates. Thickness : Type-section 2,100 feet. In the type-area of Swain’s Gully the Namoi Formation consists of olive-green mudstones with lenses of sandstone and oolitic limestone. Further north more sandstone beds and some heavy conglomerate lenses are conspicuous. Because of the great variety of rock types the name “‘formation’’ was chosen in preference to “ mudstone ’’, though this rock is dominant in most parts of the sequence. J. W. Pickett (unpublished thesis) has described some sandstone bands, grey or greenish grey in hand-specimens. They are usually less than a foot in thickness, but are quite variable for they may exceed ten feet in places, apparently thickening from west to east. Microscopically, they are seen to contain very little quartz—usually less than 5 per cent, but with feldspar and/or rock fragments often comprising three-quarters of the rock. The matrix is nearly always in excess of 20 per cent. The rock fragments are almost invariably lavas, of acid and intermediate types. There is a wide range in the composition of the feldspars. Chlorite replaces many lithic frag- ments, epidote is in small crystals elongated and lying in the cleavage traces, while calcite occurs in small islands of irregular shape in the plagioclase grains. Carey (1937, p: 350) stated that the Burindi Series was more than 2,500 feet thick. K.S. W. Campbell has a measured thickness of the Namoi Formation in the Swain’s Gully-Bab- binboon area of just over 3,000 feet. MERLEWOOD FORMATION Synonymy: Lower Kuttung Series (Carey, 1937). Derivation : Merlewood Homestead. Type Section: Merlewood Section (Carey, 1937, pp. 350-351). Lithology : Lithic sandstones and conglomerates. Material often current-bedded and largely of volcanic origin. Lavas, commonly pyroxene andesite, are interbedded. Thickness : Type-section 3,350 feet. The Merlewood Formation is adequately described by Carey as the “ Lower Kuttung Series’. His map (plate XVIII) shows a number of rock units which are here given the status of members of the formation. These are listed below. Carey’s descriptions of the rocks appear to be adequate and as they were not examined in detail in the Belvue Basin they will not be dealt with further. Outcrops in the Belvue Basin are discon- tinuous and poor but pebbles are widespread and apparently come from the lower beds of the formation. None of the members apart from the conglomerates was recognized. MEMBERS OF MERLEWOOD FORMATION All defined from Swain’s Gully or Merlewood Section (Carey, 1937, pp. 350-351). (1) Myall Camp Conglomerate Member Derwation : Myall Camp Gully. Lithology : Coarse conglomerates with boulders of pink granite and porphyry, lithic sand- stones. Thickness: Type-section 200 feet. (2) Babbinboon Conglomerate Member Derivation : Parish of Babbinboon, County of Buckland. lithology: Thick conglomerates with granite and andesite boulders up to 2 feet in diameter and coarse lithic sandstones. Thickness: Type-section 460 feet. (3) Woodlands Andesite Member Derivation : Woodlands Station. Lithology : Pyroxene Andesite. Thickness : Type-section 20 feet but thickening elsewhere to 300 feet. (4) Swain’s Gully Sandstone Member Derwation: Swain’s Gully, Parish of Bab- binboon, County of Buckland. Lithology: Pebbly and coarse gritty lithic sandstone with plant fossils. Thickness : Type-section 200 feet. (5) Hill 60 Member Derivation : Portion 60, Parish of Babbinboon, County of Buckland. Lithology : Conglomerate with grey quartzite pebbles and volcanics in a matrix containing a variable amount of oolitic limestone. Thickness : Type-section 270 feet. | ed @ e\, aN = PYROXENE ANDESITE | . Td OMERTON ce lm S| AMOI FORMATION Esa | / ORE £2 “ww PLAINS pe | TULCUMBA SANDSTONE A 4 RANGARI LIMESTONE M'BER [_——ar DEVONIAN. MANILLA GROUP (UNDIFF.) BORAH LIMESTONE MEMBER Lawad KEEPIT CONGLOMERATE M'BER GEOLOGICAL BOUNDARIES —— ROADS. ESTABLISHED FAULT. mmm CREEKS.—< PROBABLE FAULT. =m om GEOLOGICAL MAP OF THE CARROLL — KEEPIT —RANGARI AREA OF NEW SOUTH WALES. ALG IEEM () NEHOMSEUON BGG |: , 8 i = o 2 = poe up 4 | : HUM] ge eee 5 ee y oO a gl 4 VA ie i q = —S re) ——[S= < 4 ; NP EX ak WXs Rss QW . sf IIS Ee f f Gre SUT Sh { = —_— SS =~ GEOLOGY OF CARROLL-KEEPIT-RANGARI AREA, N.S.W. ve (6) Duri Andesite Member Derivation : Duri Peak. Lithology : Volcanic rocks principally pyroxene andesites, felsites and tuffs. Thickness : Type-section 340 feet, but thickens to 1,000 feet elsewhere. COEYPOLLY CONGLOMERATE Synonymy : Porphyry Boulder Horizon. Derivation: Coeypolly Creek, County of Buckland. Type Area: Royston Section (Carey, 1937, p. 348). Lithology : Coarse conglomerate with boulders of granite and a distinctive pink porphyry. Thickness : Type-area 150 feet. This “ Porphyry Boulder Horizon’ was described by Carey as the basal conglomerate of the Upper Kuttung Series. His mapping of it round the Werrie Basin seems sufficient for it to be regarded as a formation. CURRABUBULA FORMATION Synonymy : Glacial beds of Upper Kuttung. Derivation : Village of Currabubula. Type Section : Woodlands section Werrie Basin (Carey, 1937, pp. 343-344), but well exposed and easy to observe in creek through Currabubula village. Lithology : Tillites, conglomerates, varves and tuffs with some flows of acid lava. Thickness : Type-section 5,000 feet. The beds of the Currabubula Formation, described by Carey (1937, p. 344), are regarded as overlying the coarse basal Coeypolly Con- glomerate and with it comprising what he called the ‘“‘ Upper Kuttung Series ”’. Rocks of the Currabubula Formation were found in the ranges running north-westward from Carroll to Wean Gap. The varves and associated beds are exposed along the creek through the Gap. Permian Stratigraphy NANDEWAR GROUP F. N. Hanlon (1948, p. 256) divided the Nandewar Group into the Wean Formation and the overlying Vickery Conglomerate. The Wean Formation, of fresh-water origin, was tentatively correlated with the Greta Coal Measures, in the north-west corner of the map west of the Border Thrusts and lying almost horizontally upon the cratonic block. In suggesting the alteration in the Permian portion of the legend on Carey’s 1934 map (plate XVII) it is considered that the “ Werris Creek Coal Measures’’ is a name which is a suitable rock term. The name of “ Werrie Basalts’”’ is preferred to ‘‘ Werrie Traps” because the word “trap’’ is now rarely used for basalt in New South Wales and furthermore local New England usage includes a variety of rocks other than basalt and granite. It is here recommended that the rocks out- cropping widely throughout the Werrie Basin and to the south, regarded by Carey (1934) as probably of “‘ Lower Coal Measure” age, and taken to comprise the “ Lower Stage”’ of the “ Willow Series ’’ by Hanlon (1947, p. 281) be called the Willow Formation, of thickness 300-350 feet, with the type section at Curra- bubula in Currabubula Creek. IGNEOUS ROCKS A number of intrusions of basic rock related to those described by Carey (1934, pp. 369-372) occur along the line of the main faults on the inner side of the Border Thrusts. They have not yet been studied in detail. Small outliers of Tertiary basalt occur sporadically throughout the area mapped. Structural Geology The area is within the Western Belt of Folds and Thrusts and includes the Border Thrusts of the Upper Palaeozoic Orogenic Belt of north-eastern New South Wales (Voisey, 1959) and is south-west of the Manilla Syncline (Voisey, 19585). Chappell (1962) has mapped the structures immediately to the east. The western cratonic areas with Permian and Mesozoic rocks lying with very gentle westerly dips on the stable block have been mapped by Hanlon (1947 e¢ seq.). The most important controlling structure is the synclinal axis with its reverses of pitch which gave rise to the Werrie Basin (Carey, 1934) in the south and the Belvue Basin which is shown in the central portion of the map (Hie 2:3). The Belvue Basin is asymmetrical—the eastern limb dipping west generally at angles of from 10° to 15° and the western limb dipping east generally at about 40° (Fig. 2). Faults occur in the closure portions at both the northern and southern ends of the basin, the actual extent of the fracturing being greater than the map indicates as a large number of minor faults occur in the soft mudstones of the 12 A, H, VOISEY ANDUK. 2 WILEEAMS Namoi Formation. These are difficult to portray adequately. An extraordinary feature of the pattern is the continuity of the Tulcumba Sandstone, which deviates little from its position on the western limb of the Werrie Basin to take up a similar one in the Belvue Basin. On the other hand it is extensively broken and displaced along the eastern limb of the latter. North of Somerton there is the suggestion that it occupies the extensively fractured core of an anticline. Fragments of what is probably the Rangari Limestone member are displaced from one another and dip in various directions. A large number of faults can be traced through competent units of the Manilla Group to the east, giving rise to a pattern similar in style to that in the neighbouring Manilla Syncline. The major thrusts are south-south-east to north-north-west in their trend and roughly parallel to the Border Thrusts and main axes of folding. The minor faults between them have displaced the useful marker bed—the Borah Limestone—in a number of places. The frag- ments of this bed can be traced from this area past Somerton to the south of Tamworth, where it has been mapped by Crook (1961a. 19616) as the Kiah Limestone. Two main thrusts and a number of minor ones belong to the Border Thrust zone and are continuations of those (the Mooki Thrusts) noted by Carey in the south. An elongated area between the thrusts is composed almost entirely of Currabubula Formation (Upper Kuttung) and forms a prominent physiographical feature. Carey (1934, pp. 359-369) discussed the tectonics of the western part of the Werrie Basin and his remarks apply similarly to the Carroll-Wean belt. It is noteworthy, however, that the Currabubula Formation between the thrusts in the south is folded into an anticline. Conclusion The material in this paper has been assembled as part of a major project, shared by a number of workers, aimed at mapping the Devonian and Carboniferous strata throughout the New England region. The identification of mappable units has been closely related to the recognition of the structures. Use of aerial photography has shown that faulting is far more widespread than was formerly believed and selection of places where sections can be measured with confidence is a major difficulty. Consequently, earlier stratigraphical work carried out without this advantage has of necessity been critically examined. We wish to thank Dr. K. S. W. Campbell of the School of General Studies of The Australian National University and Dr. G. M. Philip of the University of New England for assistance in reading of the manuscript. In connection with the field work we much appreciated the hospitality of Mr. and Mrs. Bruce Dowe, Mr. and Mrs. G. Gordon and family, Mr. and Mrs. R. Perrott, and Mr. and Mrs. C. Nicholls. References Benson, W.N., 1913. The Geology and Petrology of the Great Serpentine Belt of Nis We bare Introduction. Proc. ~ Linn. Soc., -N.S.W., 38, 490-517. CAREY, S. W., 1934. The Geological Structure of the Werrie Basin. Proc. Linn. Soc. N.S.W., 59, 351-374. CaREY,S.W. 1935. Note onthe Permian Sequence in Ibid., 60, 447-456. The Carboniferous Sequence in the Werrie Basin. TIbid., 62, 341-376. CHAPPELL, B. W., 1962. The Stratigraphy and Structural Geology of the Manilla-Moore Creek District, N.S.W. ‘J:s"Proc: Voy, 0c. Neo Wye the Werrie Basin. CAREY, S. W., 1937. 95, 63-75. Crook, K. A. W., 1960. Petrology of the Parry Group, etc. J. Sedimentary Petrology, 30, No. 4, 538-552. Crook, K. A. W., 196la. Stratigraphy of the Tam- worth Group, etc. J. Pyoc. Roy: Soc. Nes We 94, 173-188. Crook, K. A. W., 1961b. Stratigraphy of the Parry Group, etc. Ibid., 189-207. Davip, T. W. E., 1950. The Geology of the Common- wealth of Australia. Edward Arnold, London. Hanton, F. N., 1947. Geology of the North-Western Coalfield. Part I. Geology of the Willow Tree District. J. Proc. Roy. Soc. N.S.W., 81, 280-286. HANLON, F. N., 1948. Geology of the North-Western Coalfield. Part VI. Geology of the South-Western Part of County Nandewar. Jbid., 82, 255-261. Jenson, H. I., 1907. Geology of the Nandewar Mountains. Proc. Linn. Soc. N.S.W., 32, 842. Litoyp, A. C., 1933. Gunnedah-Manilla District. Ann. Rept. Dept. Mines N.S.W. 89. PICKETT, J. W., 1960. A Clymeniid from the Wock- lumeria Zone of New South Wales. Palaeont., 3, 237-241. RaGcatt, H. G., 1956. Australian Code of Strati- graphic Nomenclature. Aust. J. Scr., 18, 117. VoisEy, A. H., 1952, 1953. The Gondwana System in N.S.W. Jn Symposium of Nineteenth Internat. Geol. Cong., Algiers, pp. 50-55. VoisEY, A. H., 1958a. Further Remarks on the Sedimentary Formations of New South Wales. J. Proc. Roy. Soc. N.S.W., 91, 165-189. VoisEY, A. H., 1958b. The Manilla Syncline and Associated Faults. Ibid., 209-214. VoisEy, A. H., 1959. Tectonic Evolution of North- Eastern New South Wales. Ibid., 92, 191-203. AUSTRALASIAN MEDICAL PUBLISHING CO. LTD. SEAMER AND ARUNDEL STS., GLEBE, SYDNEY B.SC.Agr. cB. ‘SMITH-WHITE, ALA ee spe * 4 z ‘ : , Th. —————————————e ee 83. bet 3 x sad a ¢ 5 ; ; a - re =e Sune 8, ena Mig ven saad Fatal Si 85 oper eae — 2 \ 3 Th Be = { paper, SF |. NOTICE TO AUTHORS ee ie Si q General.. Manuscripts should be addressed to the Honorary Secretaries, Royal Society of New ‘South Wales, 157 Gloucester Street, Sydney. Two copies of each. manuscript are required: the original typescript and a carbon copy; together with two additional copies of the abstract typed on separate sheets. Papers should be prepared according to the general style adopted-in this Journal. They should be as concise as possible,tconsistent with adequate presentation. Particular attention should be given to clarity of expression and good prose style. The typescript. shouldbe double-spaced, preferably on quarto paper, with generous side margins. 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When several photographs. are to.be combined in one Plate, the photograpk should be mounted on a sheet of white briste board in the pgeccare! ii rok for pene E reproduction. ; oe Geological Papers. . Cees in ‘speci a circumstances, authors submitting manuscripts = in which new stratigraphical nomenclature — proposed must also submit the letter of approv +t whe Geological Society of Australia. ott 2 eee Reprints. ‘Authors who. are _ members of. galley: proofs. > <= Journal and Proceedings, Royal Society of New South Wales, Vol. 97, pp. 73-79, 1964 The Eclogite-bearing Basic Igneous Pipe at Ruby Hill near Bingara, New South Wales J. F. LOVERING Department of Geophysics, The Australian National University, Canberra ABsTRACT—The Ruby Hill pipe, 12 miles south of Bingara, N.S.W., intrudes Upper Devonian Baldwin sediments and is composed of basic breccia intruded by several alkali olivine-basalt dykes. A palaeomagnetic study suggests a Mesozoic age for the intrusion. Of particular petro- genetic interest is the occurrence in the breccia and dykes of a varied assemblage of inclusions which may represent portions of lower crust (granulitic inclusions) or upper mantle (eclogitic and rare ultrabasic inclusions) caught up by the magma prior to its intrusion in the upper crust. The granulites are coarse-grained assemblages of garnet (n=1-766), clinopyroxene (3—1-700, 2VY=59°), plagioclase (An,,) plus minor amounts of scapolite and rutile. to Me.) has a high sulphur content (approximately 2-3 per cent S). The scapolite (close The eclogites consist of pyrope-rich garnet and clinopyroxene (3—1-708, 2VY=58°) with minor rutile. Introduction Ruby Hill forms a low hill (about 80 feet high) some 12 miles south of Bingara on the western side of Bingara-Barraba road. Curran (1896) first reported the occurrence of a red pyrope-rich garnet in a “coarsely crystal- lizing basic rock ’’ within the basalt occurring at Ruby Hill. The garnet matrix was described as a probable segregation from the basalt and was composed of “pyroxene, feldspar and kelyphite rings of a composite substance surrounding garnet ’’. Considerable interest in Ruby Hill was aroused by a report that ten diamonds totalling 44 carats were found in the breccia filling of the Ruby Hill igneous pipe (Pittman, 1901) but no further diamonds were ever recovered from the breccia. In 1902 Card published a detailed petrological discussion of the inclusions in the basic breccia and basalt dykes at Ruby Hill and described them as mostly “ eclogites ’’ with some “ augite picrites ’’. The present study of the Ruby Hill pipe and its inclusions arose from the renewed petrological interest in eclogitic rocks as possible materials composing the earth’s upper mantle (Lovering, 1958). Eclogites occurring as inclusions within igneous pipes are particularly important in that they may well represent direct samples of the upper mantle caught up in the magma of the pipe during its passage to the earth’s surface. The Nature of the Intrusion The form of the Ruby Hill igneous pipe is essentially that described by Pittman (1901) and shown in his sketch map. The main part of the roughly circular pipe is composed of a rather decomposed, brownish volcanic breccia of generally basic composition intruded by three large and at least two smaller dykes composed of a very fine grained basaltic rock. The inclusions occur in both the breccia and the basaltic dykes, but those occurring within the breccia tend to be very much more altered with very little garnet remaining. The pipe itself intrudes greywackes and mudstones of the Upper Devonian Baldwin formation and many inclusions of these rocks occur within the breccia. The “eclogite”? and _ ultra-basic inclusions occur in both the breccia and the basalt dykes but those within the breccia are always very much altered. The large (up to 1 cm. across) ruby-red garnet xenocrysts described by Curran (1896) and Card (1902) occur in both the breccia and basalt. An old analysis reported by Curran (1896) is given in Table 1 and a calculation of the structural formula would suggest that it is not a first-class analysis. However, the analysis is of sufficient accuracy to establish that the garnet contains over 50 mol. per cent pyrope and has probably resulted from the break-up of garnet granulite and/or eclogite inclusions in the pipe. 74 yj. F. LOVERING TABLE ] Garnet Xenocrysts in Ruby Hill Breccia Pipe (After Curran, 1896) Structural Formula Analysis (calculated on the basis of 24 (O)) S10, 39°57 Si 6-02 Al,O; 23-68 Al 4-24 ae 26 Fe,O, 0-18 Fee? 0-02 a FeO 10-04 Mg 3°28 MnO 3°76 Fe?+ 1-28 >6-46 MgO 14-45 Mn 0-48 CaO 8-76 Ca 1-42 Total 100-44 3°743 Almandine 19-7 mols, Andradite 0-4 Grossular 21:7 Pyrope 50°7 Spessartine 7°5 THE BRECCIA Superficially, the breccia resembles the so- called ‘‘ yellow ground ”’ of the weathered zone of the South African diamond bearing pipes. However, it is obvious that the Ruby Hill breccias are generally of basic composition and quite different from the curious volatile rich, ultra-basic kimberlite magmas of the South African pipes. The Ruby Hill breccia does however very closely resemble the basic breccia in the eclogite-bearing pipes occurring near Delegate, New South Wales (Lovering, unpublished work). One unusual feature of the Ruby Hill occurrence is the abundance of very pale pink stilbite filling vughs and veins within the breccia. The breccia is full of fragments of various sedimentary and igneous rocks (from the surrounding country rocks) together with many fragments of basaltic rocks. The granulitic and eclogitic inclusions are much less abundant but this may be due to the fact that they are usually very altered and difficult to recognize. The breccia also contains abundant red garnet and green chrome-diopside grains and probably a considerable variety of other mineral grains derived both from the country-rock inclusions and the more deep-seated inclusions. THE BASALT DYKES Basaltic fragments are common in the breccia but the least altered basalts occur as dykes within the breccia. In hand specimen the dyke basalts are generally very fine grained, occasionally rather mottled in appearance and containing many garnet xenocrysts and granulite ~ and eclogite xenoliths. In thin section there are a number of “‘ pheno- crysts ’’ (up to 1 mm. across) of clino-pyroxene (type I) with border zones of a second clino- pyroxene (type II) which shows virtual optical continuity with the central clino-pyroxene and gives a well defined crystal shape to the “phenocrysts ’’. The type I clino-pyroxene is usually irregular in shape, colourless and has a very low dispersion (high 2V). On the other hand the surrounding type II clino-pyroxene has very strong dispersion with a 2V of approxi- mately 33° and is probably salitic in composition. It would seem that the clino-pyroxene forming in the groundmass of the rock is also salitic in composition so that the type II clino-pyroxene represents a salitic clino-pyroxene which crystal- lized from the magma on to a nucleus of a different sort of clino-pyroxene (type I) which probably is xenocrystic material resulting from the break-up of various deep-seated inclusions in the magma. As such these “ phenocrysts ” are both xenocrystic and phenocrystic in origin. ‘“Microphenocrysts’”’ of olivine occur showing all stages in alteration to serpentine. It 1s also possible that at least some of the olivine occurring in the rock is also xenocrystic in origin, resulting from the break-up of ultra-basic xenoliths in the magma. Some brown spinel xenocrysts showing dark borders were also ~ observed and probably originated from ultra- basic xenoliths. The groundmass consists of small (<0-1 mm.) plagioclase laths (often showing fluidal texture), salitic clino-pyroxene grains and is dusted with extremely small opaque grains about 2u across. There is also a considerable amount of brown glass (n >1-54) in the groundmass. Serpentinous and chloritic material also was observed. The analysis of the basalt (Table 2) indicates that the molecular norm contains a_ considerable amount of nepheline (~8%) although none was observed in the mode. It would seem that the magma filling the dykes in the Ruby Hill breccia was an alkaline olivine basalt type. The basalt also contains xenocrysts of a strongly magnetic black mineral with a sub- metallic lustre. A partial analysis (Table 3) indicates that it is a titanomagnetite with some Fe?+ being replaced by Al$+ and Cr?+ and Fe?* by some Mg?+ and Mn?*. AGE OF THE INTRUSION In the absence of any more positive evidence, the Ruby Hill intrusion has usually been considered to belong to the Tertiary alkaline ECLOGITE-BEARING BASIC IGNEOUS PIPE AT RUBY HILL TABLE. 2 Chemical Analyses of Rocks from the Ruby Hill Pipe “Eclogite* Garnet Eclogite (Garnet Granulite (Altered) Basalt Dyke Granulite) Inclusion imclicion R176 Inclusion R165 R169 (Card, 1902) (Altered) SIO; 43-05 44-30 43-46 46-25 TiO, trace 0-94 2-36 2-16 Al,O3 20:74 18-62 14-49 15-80 HesO; 4-55 5°35 7-49 5-53 FeO 4-08 4-04 4-62 6-12 MnO 0-23 0-13 0-14 0-24 MgO 7-06 8-63 7:59 3°81 CaO 15-30 14-52 14-57 7-94 Na,O 1-59 1-33 1-64 4-54 LEGA) 0:21 0:07 0-16 2-40 P;0; 0-02 0-04 0-07 0-87 HO 2-97 1-65 2-13 2-10 EO — 0-50 0-24 Lol 0-47 CO, oa 0-35 0:28 0-16 Cr,0; — 0-05 0:02 0-02 Total 100-30 100-25 100-32 100-41 Sue — 3-08 2-93 2:81 Moleculay Novi Quartz — — 0-02 = Orthoclase 1-24 0-4] 0-95 14-18 Albite 6-84 11-25 13-88 24-69 Anorthite 48-84 44-63 al ear 15-65 Diopside Fs 1-95 0-67 0-00 1-27 En Soe 8-49 +19-57 13°84 +29-85 5-19 +13-51 Wo , LT 25:) 10-41 16-01 7-12 Hypersthene Fs a LO ees yl ee O00 [8s Ag as En = ai oe Bary eee = Olivine Fa era OFS Ona. en 1-75 : Fo poe Ss da aie oe GB0f vice Apatite 0-05 0-09 O-17 2:06 Magnetite 5-60 7-76 8-48 8-02 Ilmenite — Eeag 4-48 4-10 Hematite a --- 1-64 — Chromite —- ~— 0-03 0-03 Nepheline 3°58 — —- 7-99 Water 3°47 1-89 3°44 2°57 Analyst : Ee P White Are |aceaston A. J. Easton A. J. Easton olivine basalt province of New South Wales. Many of the flow basalts belonging to this province overlie Tertiary plant-bearing sediments and so are Tertiary in age (David and Browne, 1950), but recently a _ palaeo- magnetic study of three supposedly Tertiary intrusions (i.e. Prospect, Mt. Gibraltar and Gingenbullen) has indicated that they are of Mesozoic age (Boesen, Irving and Robertson, 1961). More recently, potassium-argon dating has shown that the Prospect intrusion is 168 million years old while Mt. Gibraltar is 178 million years old, in good agreement with the palaeomagnetic data (Evernden and Richards, 1962). The Ruby Hill breccia does not seem to contain any minerals suitable for K-Ar dating but a palaeomagnetic study has been made on the basalt dyke within the breccia and a south pole position of approximately 49°S, 190° E 76 J. F. LOVERING TABLE 3 Partial Analysis of Titano- magnetite Xenocryst im Basalt from Ruby Hill Doe D 4-90 Analyst: A. J. Easton. * Total iron reported as Fe,Os. has been determined (W. A. Robertson, personal communication). This pole position is rather similar to those found previously for Prospect. Mt. Gibraltar and Gingenbullen and would suggest a Mesozoic age for the Ruby Hill intrusion. Preliminary results of a K-Ar age study of the Delegate intrusion (so similar petrologically to the Ruby Hill intrusion) have shown an age of about 170+10 million years (Lovering, unpublished work) which is consistent with the palaeomagnetic data and strongly suggests that all these intrusions, including Ruby Hill, are lower Jurassic to upper Triassic in age and as such are considerably older than the established Tertiary flow basalts which occur over much the same _ area geographically. The Deep-seated Inclusions Both the breccia and basalt dykes at Ruby Hill contain xenoliths of granulitic, eclogitic and. ultra-basic rocks which show considerable similarities with similar inclusions found in other breccia pipes in Eastern Australia (e.g. Delegate). Card (1902) first described the occurrence in the Ruby Hill breccia of fragments of a rock consisting of garnet-plagioclase clino-pyroxene- kyanite which he called an “eclogite”. It is now generally agreed that feldspar is not a stable phase in rocks of the eclogitic facies, so that the rock described by Card is_ better described as a garnet granulite of the granulite facies. In the present study many garnet granulite inclusions were observed but a number of true eclogite inclusions (consisting entirely of garnet and_ jadeitic clino-pyroxene assemblages) were also found. Card (1902) also described an ultra-basic inclusion (con- taining olivine, pyroxene, amphibole and pleonaste) from the breccia but no unaltered ultra-basic inclusions were found during this study. Several extremely carbonated inclusions were found and may represent extremely altered ultra-basic inclusions. GARNET GRANULITE INCLUSIONS The “ eclogite ’’ inclusions described by Card (1902) are better termed garnet granulites and are essentially coarse grained assemblages of garnet-clino-pyroxene-plagioclase. Scapolite is usually an important minor phase and had been identified as kyanite by Card (1902). Modal analyses on three garnet granulite inclusions (Table 4) are remarkably similar, while the analysis reported by Card (1902) agrees well with an analysis of a garnet granulite collected during the present study (Table 2). Card’s analysis indicates nepheline in the molecular norm while the new analysis does not have free nepheline. However, both analyses indicate that the garnet granulites have affinities with undersaturated basic magmas. The garnet grains are virtually all altered to a confused mixture of fibrous chloritic material, brownish-green hornblende and opaque minerals but occasionally some unaltered cores are found. Unaltered garnet grains also occur as inclusions within clino-pyroxene crystals. The refractive index of the garnet is 1-766 and is similar to garnets in garnet granulite and eclogite inclusions from the Delegate pipe (Lovering, unpublished work). The clino-pyroxene is normally unaltered and | coloured very pale shades of bluish and greenish- — grey. Optical properties are very similar to those of the clino-pyroxene in the eclogite inclusion (Table 5) and the analysis reported by Card (1902) also would indicate that it is a jadeitic clino-pyroxene with strong similarities to those characteristic of eclogitic rocks (Table 6). The plagioclase grains are virtually untwinned with well-developed cleavages. There is some secondary iron-stained chloritic and/or zeolitic material in fractures but on the whole the plagioclase grains are quite fresh. The refractive index ®6=1:570+0-002 indicates that the plagioclase is labradorite-bytownite (71 mol. per Cem ema). Rutile, often with opaque inclusions, is a minor accessory mineral and forms elongated brown crystals. A very important minor phase is scapolite, which occurs as well developed euhedral grains about 0-5 mm. long or even larger. Cleavages ECLOGITE-BEARING BASIC IGNEOUS PIPE AT RUBY HILL AG: TABLE 4 Modal Analyses of Inclusions in the Ruby Hill Pipe Garnet Granulites ' Eclogites Phases (volume per cent) MM 1929C* MM 1929E* R 1657 R 169+ Clino-pyroxene Unaltered 27-2 25-8 26:8 34:5 Altered 0-0 0-0 0-0 11-9 Total 27°2 25°8 26-8 46-4 Garnet Unaltered 0-2 0-2 0-0 0-2 Primary Altered 35-9 45-2 38-4 49-4 Phases Total 36-1 45-4 38-4 49-6 Plagioclase 29-9 22:8 24-1 — Scapolite Unaltered 1-0 1-] 2+2 — Altered 5:8 4-9 2-5 — Total 6°8 6-0 4:7 — Rutile — --- 0-65 0-5 Chlorite (interstitial) oe oo 5 0-5 Secondary Plagioclase (interstitial) a — —— 3 Phases Magnetite (interstitial) — — — 0:3 Calcite (interstitial) — — — 0-5 * Slide number in collection of the Mining Museum, N.S.W. Geological Survey. + Specimen number in personal collection, Department of Geophysics, Australian National University. are often well developed and each scapolite crystal normally has a distinct alteration zone around its margin. The alteration zone may be interrupted where the grain is in contact with clino-pyroxene and a few scapolite grains observed within clino-pyroxene grains were virtually unaltered. The alteration zone is most obvious when the scapolite is near an altered garnet grain. The alteration zone is TABLE 5 Optical Properties of Clino-pyroxenes from Garnet Granulite and Eclogite Inclusions Clino- pyroxene Clino- from pyroxene Optical Property Garnet from Granulite Eclogite (R165) (R169) Refractive indices* a 1-693 — B 1-700 1-708 Y 21 = Optic axial angle 2VY (calculated) 60-5° — 2VY (measured) 59+1° 58+1° Dispersion Strong and Strong and inclined inclined (p>) (o>) * Determinations +0-001. made up of tiny plagioclase crystals, showing well developed fine twinning lamellae with high 2Vx and an average refractive index close to 1-570 indicating a composition close to Any. The scapolitization of plagioclase is observed in many geological environments but the texture in this case indicates the reverse process— TABLE 6 Analysis of Clino-pyroxene from Garnet Granulite Inclusion in Ruby Hill Breccia Pipe (After Card, 1902) Structural Formula (calculated on the basis of 6 (O)) SiO, 45-92 Ss)! 1 $4 p20 . Al,O, 12-03 Al 0:34 bt HesO. 2-24 FeO 1-73 Al 0-181. o4 | MgO 13-30 Bes, 0-06 f CaO 22-73 Na,O 1-19 Mg 0-72 V9. 77:71:99: K,O 0-32 ees 0-05 f H,O+ 0:66 | CO, 0-39 Ca 0-88) | Na a 0-98 Total 100-51 K 0-0 : D 3-338 ~ Casi5 Marg Feg.g Analyst: H. P. White. 78 J. F. LOVERING the alteration of scapolite to plagioclase. The refractive indices for the scapolite are np=1 -588, Ne=1-565 (dnp=0-023, nm=1-576) and suggest a composition of 80 mol. % Meionite using curves published by Shaw (1960). However, an analysis of a scapolite grain by the electron probe X-ray microanalyser shows that the halogen content is very low but that the sulphur content is extremely high (approximately 2:3% S). Shaw (1960) has shown that other sulphur-rich scapolites do not fit on his curve relating Nm and meionite content so that the scapolite in the Ruby Hill garnet granulites probably has a meionite content closer to 70 mol. % than to 80% (as determined from Shaw’s curve). The lower meionite content would be consistent with the observation that the composition of the plagioclase in the alteration zone is about 70 mol. % An. The significance of the occurrence of sulphur-rich scapolites in the garnet granulite inclusions will be discussed elsewhere (Lovering and White, 1963). Veins of zeolitic material occur within some of the garnet granulites. THE ECLOGITIC INCLUSIONS A number of inclusions were found consisting essentially of coarse grained garnet-clino- pyroxene assemblages with accessory rutile and a number of secondary phases resulting from the advanced alteration of the garnet grains (Table 4). Analysis of one such _ eclogite inclusion (Table 2) shows an overall similarity with the garnet granulite inclusions although the molecular norm contains a very small amount of quartz probably arising from the high oxidized iron content of the altered rock. It seems likely that in the unaltered state this eclogite would have had affinities with a saturated basic magma. The garnet grains are virtually completely altered to a felted mass of brown chlorite and/or hornblende with opaque grains. A few very small cores of unaltered garnets were observed but sufficient material for the determination of optic properties was not available. The clino-pyroxene is bluish or greenish grey, normally unaltered but with some recrystal- lization along grain boundaries. The optical properties are very similar to those clino- pyroxene in the garnet granulites (Table 5) and in eclogitic inclusions from the Delegate pipe (unpublished data). On the basis of this evidence it can be concluded that these clino- pyroxenes contain a significant proportion of the jadeitic molecule and are apparently true eclogitic facies pyroxenes. Some brown rutile grains occur as a minor phase in the eclogites and secondary veins and patches of chlorite, calcite, plagioclase and magnetite also occur. THE SIGNIFICANCE OF INCLUSIONS The co-existence of granulitic, eclogitic and ultra-basic inclusions in basic breccias and alkaline olivine basalts seems to be characteristic of certain igneous pipe-like intrusions of upper Triassic-lower Jurassic age over large areas of Eastern Australia. It is significant also that the diamond-bearing kimberlite pipes of South Africa (Williams, 1932) and Siberia (Bobrievich and Sobolev, 1957) also contain exactly com- parable suites of inclusions which are generally considered to be of deep-seated origin (Lovering, 1958). In view of the similarity of the Australian inclusions with those from South Africa and Siberia, it is suggested that the Australian inclusions also represent fragments of possibly lower crustal and upper mantle materials caught up in the pipes during their intrusion into the upper parts of the earth’s crust. In the light of evidence presented previously (Lovering, 1958) it is suggested that the granulitic inclusions probably represent material from the lower crust while the eclogitic and ultra-basic fragments represent material from the upper mantle. If this suggestion is correct it is of extreme importance to theories concerned with the nature and evolution of the earth’s crust and upper mantle in that we have in these inclusions actual samples of both regions which can be studied directly in our laboratories. THE DEEP-SEATED Acknowledgements The author is indebted to Dr. A. J. R. White for the measurements of the optical properties of the minerals quoted in this work and to A. J. Easton for the chemical analyses. Mr. D. R. Pinkstone, Mining Museum, Sydney, very kindly made available for study the original thin sections used by Card in his work on the inclusions in the Ruby Hill pipe. The author is indebted to Dr. J. F. G. Wilkinson for his comments on the original manuscript. References BoBRIEVICH, A. P., AND SOBOLEV, V. S., 1957. Eclo- gitisation of the pyroxene crystalline schists of the Archaean complex (in Russian). Zapiski V sesoyuznogo mineralogischeskogo obschestva, Vtovaya seriya, 86, 3-17. BogsEN, R., IRvING, E., AND ROBERTSON, W. A., 1961. The palaeomagnetism of some igneous rock bodies in New South Wales. J. Proc. Roy. Soc. N.S.W., 94, 227-232. ECLOGITHE-BEAKING BASIC IGNEOUS PIPE AT RUBY HILL Carp, G. W., 1902. An eclogite-bearing breccia from the Bingara diamond field. Rec. Geol. Surv. N.S.W., 7, 29-39. CurrRAN, J. M., 1896. On the occurrence of precious stones in New South Wales and the deposits in which they are found. /. Proc. Roy. Soc. N.S.W., 30, 214-285. Davin, T. W. E. (edited W. R. Browne), 1950. The Geology of the Commonwealth of Australia. Vol. 1. Edward Arnold and Co., London. EVERNDEN, J. F., anpd RicHarps, J. R., 1962. Potassium-argon ages in Eastern Australia. /. Geol. Soc. Australia, 9, 1-50. (Received 1 - WiLLiaMs, A. F., 1932. 9 LOVERING, J. F., 1958. discontinuity. 39, 947-955. LOVERING, J. F., AND WHITE, A. J. R., 1963. The significance of sulphur-rich scapolites in granulitic inclusions of deep-seated origin in igneous pipes. (In preparation.) PittMAN, E. F., 1901. The mineral resources of New South Wales. Geol. Surv. N.S.W. 487 pp. SHAW, D. M., 1960. The geochemistry of scapolite. Part 1. Previous work and general mineralogy. J. Petrol., 1, 218-260. The genesis of the diamond, Ernest Benn Ltd., London. 352 pp. The nature of the Mohorovicic Tvans. Amer. Geophys. Union, Vol. I. May, 1963) Journal and Proceedings, Royal Society of New South Wales, Vol. 97, pp. 81-82, 1964 On Traces of Native Iron at Port Macquarie, New South Wales F. M. QUODLING Department of Geology and Geophysics, University of Sydney, Sydney Since the discovery of terrestrial iron on the west coast of Greenland in 1870, less than a dozen other in situ occurrences of the native metal have been reported. In Greenland and on the adjacent Disko Island, the iron is crystal- lized as a body-centred cubic phase, Alpha, [OR 1m3m; Z=2] (Berry and Thompson, 1962). The native metal is also found crystallized in the Gamma _ face-centred cubic phase, [O02 Fm3m; Z=4]. y irons studied up to the present time are nickel iron alloys. The following source localities have been reported : near Poschiavo, Switzerland (Quervain, 1945) ; Karnten district, Austria (Ramdohr, 1950; Meixner, 1956); Corsica (Avias and Caillére, 1959) ; Tasmania (Ramdohr, 1950; Williams, 1960). Small quantities of native iron have been found by the author in several rocks of a complex in the Port Macquarie district, an area lying north-east of Sydney, New South Wales, on the Pacific coast between latitudes 31° and 32°. The occurrence, which is regarded as petro- logically significant, is unique because both a and y phase irons are present and may even be found in one rock. The native metal was first detected by extraneous lines in magnetite X-ray powder patterns. In order to confirm the discovery, any possible risk of iron contamination from outside sources was eliminated by resorting to Stone Age methods. During preparation of material for X-ray analysis specimens were broken and powdered by pounding with and between quartzite cobbles down to a stage where final grinding could be completed in an agate mortar. The X-ray powder photographs illustrating this note are contact prints of films obtained in a Straumanis type camera of 57-54 mm. diameter with cobalt Ka X-radiation (Fe filtered, A=1-7902A). Each photograph repre- sents a separate extraction of opaque material from rock specimen No. 24333, University of Sydney, a quartz garnet glaucophane lawsonite assemblage, considered by: the author to be a metamorphosed impure chert. Photograph A is the powder pattern of an « phase iron; it shows lines indexed as 110, 200, 211 and 220 of a body-centred cubic lattice. The strongest lines of magnetite appear also and are indicated by their indices alongside the film strip. Contact print B shows the patterns of both « and y irons superimposed. Measured d_ spacings, visually estimated intensities, Miller indices and calculated a parameters are listed in Table 1. The cell side for « iron of this film, 2-863A, compares with 2-8665A for pure iron (A.S.T.M. Index 1962) ; 2-863-2-877A (Fe, Mn) (Donnay et al., 1963) and 2-874A for Disko Island terrestrial iron (Berry and Thompson, 7b7d.). TABLE | X-Ray Powder Data for « and y Ivons of Specimen 24333, University of Sydney B. 1B CG « Iron y Iron vy Iron (of Garnet) dmeas- A Lest. Akl ameas: A Test: hkl Gates: A T eet. 2-024 300 110 2-069 100 lil 2-070 100 1-432 35 200 1-794 60 200 1-795 40 1-169 90 211 1-270 50 220 1-268 25 1-012 30 220 1-083 75 311 1-081 30 1-038 15 222 1-034 10 Ay= 2-863 ayg=3-591 Ag= 3° 584 82 F. M. QUODLING The y iron of this photograph with lines indexed as 111, 200, 220, 311 and 222) has a cell side of 3-591A. The y iron pattern is shown isolated in contact print C. In this case faint extraneous lines are due to reflections from the 420, 640 and 642 planes of garnet. Data for this film are given in Table 1 also. The opaque inclusions from 0-02-0-05 mm. diameter garnets of specimen 24333 have produced this pattern of a y iron. Native iron has not, so far as the author is aware, been recorded as an inclusion in garnet. The parameters for the irons of specimen 24333 differ slightly ; that for the inclusions in the garnet host being 3-584A. Both values compare with cell dimensions for nickel irons, the range of which is from 3-614A (Fes , Nis)) (Donnay et al., tbid.); through 3-560A, Josephenite (Berry and Thompson, 7bid.); to 3:-54A, Awaruite (Williams, zbid.). But microchemical tests show that the associate of iron is not nickel but manganese. The field area specified is still under investigation by the author. References AMERICAN SOCIETY FOR TESTING MATERIALS, A.S.T.M. X-Ray Index. AvIAs, J., AND CAILLERE, S., 1959. Paris, 248, 118-120. BERRY, L. G., AND THompson, R. M., 1962. Powder Data for Ore Minerals. America, Mem. 85. Donnay, DoNNay, Cox, KENNARD AND KING, 1963. Crystal Data Determinative Tables, Second Ed. MEIXNER, H., 1956. Festschrift zum 70 geburtstag von Prof. F. Angel, pp. 95-106. QUERVAIN, F. DE, 1945. Bull. Suisse. 25, 305-310. Ramponr, P., 1950. Min. Mag., 29, 374-394. WiLiiams, K. L., 1960. Am. Mineral, 45, 450-453. 1962. CuRa Acad. S¢t X-Ray Geol. Soc. Min. Péir., (Received 17 February, 1964) Explanation of Plate X-ray powder patterns of three samples, each from specimen U.S.G.D. 24333. A. Alpha iron associated with magnetite. B. Alpha and gamma iron mixture. C. Gamma iron extracted from garnets. POURNAL ROYAL SOCIETY N.S.W. QVUCDIEEN GA iia Magnetite Alpha Gamma Iron Iron 311 110 11] 200 422 333+ 511 440 220 -} 311 222 eu ra ee eee a od ae i lee x scone ent aah ae miler | Journal and Proceedings, Royal Society of New South Wales, Vol. 97, pp. 83-89, 1964 LEPIDOPHLOIOS and CYRTOSPIRIFER from the Lambie Group at Mount Lambie, N.S.W. R. M. Mackay Department of Geology and Geophysics, University of Sydney, Sydney Apstract—Lepidophiloios sp. indet., Cyrtospirifer inermis (Hall), C. oleanensis Greiner and C. gneudnaensis Glenister are recorded and figured, together with diagnoses and Australian references. Lepidophloios This to my knowledge is the first record of the occurrence of this genus in Eastern Australia. The single specimen was_ kindly given to me by Dr. J. Connolly, who found it in the upper reaches of Solitary Creek near Rydal. Division. Lycopsida. GENUS. Lepidophloios Sternberg 1826. DIAGNOSIS. “ Lepidophloyos. Caudex arboreus rudimentis petiolorum squamatus, cicatrice triglandulosa subsquamis.’’ Sternberg. Translation (with the assistance of Mr. A. M. Brough) : The stem of a tree with scale-like leaf cushions and primitive petioles. Small leaf scars on the leaf cushion bear three round pits. Discussion. The change of name of Stern- berg’s Lepidophloyos to Lepidophloios apparently occurred pre-1893 and is probably only a correction of the original Latin. Kidston (1893) discusses fully the relation of Lomatophlotos, Haloma, Pachyphloeus and Cyclocladia to Lepi- dophlotos and concludes that they “. . . merely represent different conditions of growth and preservation of one generic type”. Of the relation of Lepidophloios to Lepidodendron Seward (1910, p. 105) says : . . apart from the form of the leaf cushion. . .we are at present unable to recognize any well defined differences between the two forms Lepidodendron and Lepidophloios. The leaf cushions of Lepi- dophloios differ from those of the true Lepr- dodendron in their relatively greater lateral extension, in their imbricate arrangement and in bearing the leaf, or leaf scar at the summit.”’ The specimen of Lepidophlotos described here does not exhibit any characteristics (branching, etc.) by which its correct orientation can be determined. Since the leaf cushions may be directed upward or downward in different species, or vary in orientation within a single specimen of some species (see Kidston, 1893, pp. 544 and 552 for discussion), this structure cannot be used for orienting purposes. The The evidence for an Upper Devonian age for the Lambie Group is reviewed. specimen is arbitrarily oriented with the leat cushions directed upward and the leaf scar at the top of the cushion. Lepidophloios sp. indet. Plate?) Pig? 12 Material. U.S.G.D.* Specimen N° 7016. Locality. Wallerawang 1:63,360 military sheet ref. 001650. Horizon. 2,200 feet above the unconform- able base of the Lambie Group (refer Mackay, 1961). Description. Specimen N° 7016 is an impres- sion of a piece of bark, 2-8 cm. wide and 8-5 cm. long, preserved in fine quartzose sandstone. The surface is completely covered by rhomboidal, horizontally elongate, convex leaf cushion impressions, 11 mm. wide and 7 mm. long. The latter have acute lateral and upper angles but rounded lower angle and bear, at their summits, triangular leaf scars. The fine markings on the leaf scar are not preserved and hence a specific identification cannot be made. Cyrtospirifer The material described, which was collected from two localities near Rydal in the same stratigraphic horizon, is listed in Table I. The brachiopods are preserved as internal and external molds in fine quartzose sandstone. The shell material, where not completely removed, has been replaced by a pink well- crystallized kaolinite. SYSTEMATIC DESCRIPTIONS FAMILY. Spiriferidae King 1846. GENuS. Cyrtospirifer Nalivkin in Fredericks, 1926. Dracnosis. Medium sized _ plicate shells. Intercalation and bifurcation of the plications on the sulcus and fold, but never on the lateral * All specimen numbers refer to the University of Sydney Geology Department, Palaeontology Collection. 84 RK! Mo MACKAY TABLE 1 U.S.G.D. Specimen Nos. Species Locality A Locality B Cyrto- 1355 8, 138559, 13550 A-F, 13551 A—D spivifer 13580 13554 A-B, 13555 B—-C ineymtis 13556 A-C, 13557 A—C 13561 A—-F, 13564 A-B 13568 A-C, 13569 A—C 13570 A, 13571 A-—D 13572 A, 13574 A-B 13575, 13579 13581 C. olean- 13552 A-C, 13562 13555 A ensts 13563, 13565 A-C, 13566 A C. gneud- 13560 naensts Locality A. Wallerawang 1: 63,360 military grid ref. 001650. Locality B. Bathurst 1: 63,360 military map, grid ref. 973630. map, slopes. Dental lamellae well developed, extend- ing along the valve floor for one-third or more of its length, and joined posteriorly by a delthyrial plate or apical callosity. (Compiled from the literature.) Discussion. Since the erection of the sub- genus Cyrtospirifer by Nalivkin in 1926, various attempts have been made to erect further genera or subgenera, especially by Grabau 1931 e¢ seq. At present Cyrtospirifer is accorded generic status and the other proposed sub- divisions, with the exception of Cvyrtiopsis, have been generally rejected. I am not in a position to express a personal opinion on the status of Cyrtiopsis but it appears that the validity of this genus is at present not established and those authors who support its retention do not agree on diagnostic generic characters. The original author, Grabau (1923, 1931-33) states that Cyrtiopsis is similar to the ‘ Upper Devonian Spirifers’’ and differs from them ‘‘ only in the persistence of the pseudo-deltidium which moreover is pierced’”’. Paeckelmann (1931) and Sartenaer (1956) also believe that the presence or absence of a deltidium constitutes the distinction between Cyrtiopsis and Cyrto- spirifey respectively. But, as Vandercammen (1959) points out, this apparatus can readily be lost before preservation and Glenister (1955) agrees “that absence in the fossil state of apparatus for closing the delthyrium does not constitute proof that this apparatus did not exist ’’. Glenister however states that Cyrtiopsis has “...long convergent curved dental lamellae ” whilst Cyrtospirifer has “‘. . . shorter divergent lamellae”. To further support his claim of generic status for Cyrtiopsis he states “. .Crickmay at least has shown that in © North America the genus Cyrtospirifer is restricted to Frasnian equivalents, while © Cyrtiopsis is restricted to Famennian equi- — valents ’’. This last piece of supporting evidence ~ rests solely on the validity of Crickmay’s faunal ~ division. In his paper (1952) Crickmay gives — no generic diagnoses but states (p. 587): “ The — resemblance of such forms as Cyrtiopsis kindlet to Cyrtospirifer is external and megascopic only. The long, thin, curved, sub-parallel dental lamellae of C. kindle: are typical of Cyrtiopsis and are very different from the short, straight, divergent lamellae of Cyrtospirifer. There are also notable differences in apical and umbonal callus, and in manner of ornament and micro- ornament.’ From his descriptions of species it appears that Cyrtiopsis is characterized by dental lamellae of length 45°-55° of the length of the valve, and micro-ornament consisting generally of concentric microfila and radial micro-striae and completely lacking pustules. Cyrtospirifer on the other hand has dental lamellae of length 30% to “35% or more” of the length of the valve and micro-ornament generally consisting of concentric microfila with pustules developed on the plications, though pustules may be absent and faint radial micro- striae may be present. Application of this basis of distinction between the two genera to the 13 sufficiently well pre- served species of Cyrtospirifer described by Vandercammen (1959) yields five species, C. stolbovi, C. tenticulum, C, bisinus, C. syringo- thyriformus and C. conoideus which fit into Crickmay’s genus Cyrtospirifer ; C. canaliformis and possibly C. monticolaformis which fit into his genus Cyrtiopsis ; one species C. orbelianus, which combines dental lamellae of length up to 50% of the valve with pustules in the micro- ornament; and three species C. brodi, C. verneuili and C. grabaui, which have the short, divergent dental lamellae typical of Crickmay’s genus Cyrtospirifer together with micro- ornament — concentric microfila plus radial micros-striae and completely lacking pustules— typical of Crickmay’s genus Cyrtiopsis. Greiner’s (1957) and Glenister’s (1955) descriptions of micro-ornament are not sufficiently detailed to allow comparison of their species. The degree to which Crickmay’s distinguishing features can be applied to Vandercammen’s species does not indicate that they will be generally applicable, and hence it is questionable whether his generic distinctions and resulting faunal division are valid. This literature survey reveals that at LEPIDOPHLOIOS AND CYRTOSPIRIFER FROM LAMBIE GROUP 85 present Cyrtiopsis does not stand as a clearly defined genus separated from Cyrtospirifer. Intensive study of the holotype of Cyrtiopsis and the large group of species of Cyrtospirifer must be carried out to justify the erection of a separate genus and provide a basis for its definition. For this reason Cyrtiopsis is subse- quently ignored. Recent work on Cyrtospirifer has resulted in the erection of a large number of new species, and each author has stressed different characters as the most important for distinguishing species. Grabau (1931-33) virtually ignores internal structures; Crickmay (1952), Vandercammen (1959) and Paeckelmann (1942) describe both externals and internals, but Crickmay and Vandercammen use only external characters, and Paeckelmann uses mainly external characters for distinguishing between species. It should be noted here also that Vandercammen and Paeckelmann do not consider the nature of the plications—bifurcating on the fold and sinus and simple on the flanks—a diagnostic generic character. In fact Vandercammen describes one species Cyrtospirifer utahensis (Meek, 1876) which shows bifurcation of plications over the entire shell. Glenister (1955) stresses the use of as many characters as possible for intraspecific dis- crimination, but again uses only externals for his comparisons between species. In his intensive study of that group of American species formerly lumped together under the name of “ Spirifer disjunctus’’, Greiner (1957) has carefully described both internals and externals of 16 species of Cyrtospirifer and his intraspecific distinctions include several of both groups ot structures. As my material, which was also described by early authors as “ S. disjuncta’’, exhibits well preserved internals and only moderately preserved externals I have found Greiner’s work the most useful and have relied more heavily upon it than upon the work of any other author. Cyrtospirifer inermis (Hall) 1843 Plate I, Figs. 1-5 Synonymy as in Greiner (1957). In addition the following Australian references. 1876. Spirifer disjunctus Sowerby. de Koninck pp. 79-81. 1880. Spirifer disjuncta Sowerby. Etheridge Hair. p. 255, Pl. Fig:..5. 1951. Cyrtospirifer — subdisyunctus. Maxwell. Maxwell, p. 8, Pl. 1, fig. 17 (a-c). Diacnosis. Shell wider than long, sulcus and fold well defined ; dental lamellae vertical and divergent anteriorly; ventral muscle field longitudinally striate and bisected by a spear- shaped median septum; dorsal muscle field not prominent, dorsal median septum slender. DESCRIPTION. Shell biconvex, ventral valve the more strongly curved; width about twice the length, hinge line produced to form small angularears. Valves ornamented with radiating plications, simple on the flanks but intercalated on the fold and sulcus ; faint concentric growth lines sometimes visible. Convexity of pedicle valve interrupted by narrow sulcus originating at beak and bounded by prominent plications; beak slightly over- hangs a prominent, oblique-angled triangular interarea (sensu Cloud, 1942, p. 138), which bears faint longitudinal striations. Interarea orthocline* and flat, rarely slightly concave, except at the posterior extremity, where it is gently anacline. Delthyrium high triangular, delthyrial angle 26° to 52°, 42°-44° being the most common values. A _ narrow, sharply depressed shelf bordering the delthyrium (Fig. 3) indicates the former presence of a deltidium (sensu Cloud, 1942), exact nature of deltidium unknown. Internally strong, vertical divergent dental lamellae extend anteriorly along the valve floor for one-third to one-half its length. The dental lamellae thicken, or are secondarily thickened posteriorly and are joined along their posterior half by a delthyrial plate which rapidly develops posteriorly into an apical callosity ; from the base of the latter a prominent spear-shaped median septum extends anteriorly for one-third the distance to the anterior margin. A few striations paralleling the median septum mark the muscle field. The fold on the dorsal valve is sharply elevated above the flanks; the beak shghtly overhangs a low dorsal interarea, which is bisected by a small triangular notothyrium. Internally only a very thin median septum, extending along the valve floor for about one- third the valve length, is visible. Cyrtospirifer oleanensis Greiner 1957 Plate I, Figs. 6-9 Synonymy as in Greiner 1957. In addition the following Australian reference. 1951. Sinospirifer sinensis Grabau var. australis Maxwell. Maxwell, p. 6, Pl. 1, Fig. 90,505 Plg2. Tig. 3: DiaGnosis. Shell almost semi-circular with ill-defined fold and sulcus; ventral muscle * Nomenclature for the attitude of the interarea is that of Schuchert and Cooper (1932). 86 Ky MM. MACKAY field circular, deeply imbedded, longitudinally striate anteriorly but radially striate posteriorly ; dorsal muscle field large; median septa well developed. DESCRIPTION. Shell biconvex, approximately semi-circular in outline, ventral valve the more strongly curved with maximum curvature in the vicinity of the umbo. Both valves ornamented with broad, flat-topped, radiating plications simple on the flanks but intercalated on fold and sulcus ; faint concentric growth lines sometimes visible. The ventral valve bears a shallow sulcus, originating at the beak and widening pro- gressively anteriorly. The longitudinally striate, subrectangular uniformly concave interarea, which varies from gently apsacline to gently anacline, is bisected by an equilateral triangular delthyrium. On the internal mold a definite gap between the filling of the delthyrial cavity and the impression of the interarea indicates the former presence of a deltidium, whose exact nature is unknown. Internally the dental lamellae which are curved in section, follow a curving path along the valve floor for one-third of its length, bordering a deeply-imbedded circular muscle field. Anteriorly the dental lamellae consist only of low ridges but posteriorly are better developed and are joined by an apical callosity. From the base of the latter a short, rapidly-thinning median septum extends anteriorly for approximately one-quarter the diameter of the muscle field. The latter is radially striate posteriorly, longitudinally striate anteriorly. Dorsal valve has a low fold and a low ortho- cline interarea bisected by a small triangular notothyrium. Internally, short longitudinal ridges locate the muscle field, which is bisected by a thin median ridge extending anteriorly for half the length of the valve floor. REMARKS. Greiner (1957) describes the ventral imterarea of his species as.) .92 cunvedseana narrowing rapidly towards the extremities ”’. The specimens described here have a more sub-rectangular ventral interarea, however the strong correspondence of all other characters justifies the identification of these specimens with Greiner’s species. Cyrtospirifer gneudnaensis Glenister 1955 Plate I, Figs. 10, 11 1955. C. gneudnaensis Glenister, p. 66, Pl. 5, figs. 6-27; Pl. 6, figs. 1-20. DiaGcnosis. Shell unequally biconvex, approximately as wide as long, fold and sulcus weakly developed, ventral interarea low ; dental lamellae low and relatively short; ventral muscle field oval, divided posteriorly for one- third its length by a prominent median septum. (Abstracted from Glenister’s description.) DESCRIPTION. Ventral valve semi-elliptical, strongly convex; sulcus shallow; exterior ornamented with fine radiating plications. Interarea sub-rectangular, flat and apsacline at the lateral extremities but gently concave, apsacline to anacline, medianly. Delthyrium large, delthyrial angle=60°. On the internal mold a definite gap between the filling of the delthyrial cavity and the impression of the interarea indicates the former presence of a deltidium. Exact nature of the latter unknown. Internally curved dental lamellae extend along the valve floor for one-third its length, thickening, or secondarily thickened, posteriorly and joined just beneath the beak by a small apical callosity. From the base of the latter a short median septum of uniform width and height extends anteriorly for one-third of the distance across the muscle field. A broad median groove for the adductor muscle, confined between two very thin, sub-parallel ridges, completes the bisection of the muscle field. Very fine longitudinal striae are the only other features visible in the muscle field. REMARKS. Since only one_ well-preserved ventral valve was found, precise identification is difficult. There are some minor differences between this specimen and Glenister’s specimens of Cyrtospirifer gneudnaensis, namely the sub- rectangular rather than triangular interarea, and the equilateral rather than broad low delthyrium. However, the striking corres- pondence of important internal structures leads me to place this specimen in Glenister’s species. Age of the Lambie Group Since de Koninck’s (1876) identification of the European Upper Devonian species Spirifer disjunctus and Rynchonella pleurodon collected from the Lambie Group at Walkers Point (presumably Mt. Walker), near Rydal, an Upper Devonian age for these rocks has not been seriously questioned. The additional discovery by David and Pittman (1893) of Lepidodendron australe near Mt. Lambie was taken to indicate an extension of the range of that species formerly considered by McCoy to be Carboniferous. In the intervening years Spirifer disjunctus or Cyrtospirifer disjunctus, R. pleurodon and L. australe have come to be regarded as hall- marks of the Upper Devonian, so that now wherever one or more of these species are identified an Upper Devonian age is immediately MaeiWOPHLOTOS AND CY RTOSPIRIPER FROM LAMBIE GROUP 87 10,200° I5,650' 5, 300° 4,000’ 4, ooo’ |} F000 2,200' 2,000 1,000 “1 gustrole” collected by author 9.7. 996624 Cyrtospirifer inermis, C. gneudnaensis, Lepidophloios sp., “Lepidodenron australe” from localities A&B Portion of succession Fron, which “L. australe” was collected by Dovid & Pittman, 18935 | Boso/ Unconformity area! assumed for the enclosing rocks. Excluding the New England province, such correlations as have been made in the “ Upper Devonian ” of New South Wales are based on spot deter- minations of species whose ranges in Australia are as yet unknown. Moreover, the validity of an Upper Devonian age for the rocks at Mt. Lambie, which has come to be considered the type area (Brown, 1931) depends completely on interregional correlation with Europe using two brachiopod species. Exactly what palaeontological information do we have concerning the Lambie Group ? The data so far available are presented in Figure 1. The range of Cyrtospirifer in Australia is not yet known. In the Catskill delta, extending through New York, Pennsylvania and Ohio States, Cyrtospirifer ranges from the base of the Chemung (see Fig. 2) through the remainder of the Upper Devonian and into the basal beds of the Mississippian system (Greiner 1957). In Europe it ranges from the top of the Middle Devonian right through the Upper Devonian and into the lowermost beds of the Carboniferous (Vandercammen, 1959; Paeckelmann, 1942). A similar range in Australia is therefore very probable. In the Catskill delta C. inermis ranges from Middle Chemung to lower Conewango and possibly into the uppermost Conewango; C. oleanensis ranges from Upper Conewango to Middle Cussewago (basal Mississippian) (Greiner, HE Glenister (1955) suggests a late Frasnian age for C. gneudnaensis apparently solely on the basis of Crickmay’s (1952) faunal division of the Upper Devonian section in North America the validity of which has already been questioned. Consequently little weight can be placed on Glenister’s range for Cyrtospirifer gneudnaensis. The range of Lefidophlovos in Australia is quite unknown. In Europe Renier (1910), Kidston (1892), Seward (1910) and Arnold (1947) all state it to be a Carboniferous genus. Finally, the stratigraphic value of Lepzdo- dendron australe requires some discussion. Crook (1960) advocates a change of name to Lepto- phloeum australe but gives no reasons for such a change. Fischer (1904), in his review of the nomenclature of Lepidodendron and its species, deals with the relationship of Lepidodendron australe McCoy, Lepidodendron nothum Unger, which the former resembles, and Leptophloeum rhombicum Dawson to the genus Lepidodendron. He concludes that the holotype for each of these “‘ species ’’ 1s only imperfectly preserved or, more precisely, is in a Bergerian state of preservation, the epidermis having been lost or destroyed before fossilization. In this state 88 R. M. MACKAY CATSKILL DELTA | Cussewaogo Tourno/sion Stage Stage CARBONIF - EROUS SYSTEM Conewongo Stoge Fomennion Conneave Stoge Stage Cannadaway Frasnian Fingerlakian Stage , K e s A) 2 X\ § x \y Q | Slage Bie; 2 Correlation of the Upper Devonian-Lower Carboniferous Zones of the Catskill Delta and Europe. (Compiled from data from Greiner (1957) and Wells (1956).) all that remains is a vague outline of the leaf cushion and a “leaf scar’’. This condition is shown by specimens of both Lefidodendron and Lepidophloios where the “leaf scar’’ represents the transverse section of the vascular bundle and the leaf-trace respectively. Such specimens cannot generally be assigned to a particular genus and certainly cannot be used for the erection of new genera. The position of the “ leaf scar ’’, which was used by Dawson (1862) as a feature distinguishing his specimen from Lepidodendron nothum, varies according to the depth of removal of the epidermis and hence is of no generic or specific value. Consequently specimens of the _ so-called “ Lepidodendron australe’’ may be imperfectly preserved specimens of either Lepidodendron or or Lepidophloios. Seward 1910, p. 104, fig. 146 A and B, shows a specimen of Lepidophlots a portion of which exhibits Bergertan preserva- tion. This portion is identical to the specimens from Mt. Lambie figured by David and Pittman (1893) as Lepidodendron australe and to other specimens collected by the writer from the same area. Reviewing the available evidence, it is clear that a definite time span cannot be assigned to the time of deposition of the Lambie Group. An Upper Devonian age is probable but not confirmed. There is the complication of the occurrence low in the succession of a plant of possible Carboniferous age. It is unlikely that the solution to the problems of ‘“ Upper Devonian ”’ stratigraphy will be found in the Mt. Lambie area. The succession is bounded above and below by unconformities (Mackay, 1961), the plant fossils are sparse, the brachiopods are abundant but virtually limited to a single horizon, and the upper four thousand odd feet are apparently unfossiliferous. Other sections may prove more rewarding, particularly the Catombal Group which contains Cyrtospirifer, ““ L. australe’’, Bothriolepis-type fishplates (Sussmilch, 1906), and, in the upper- most beds, Rhacopteris-type plant remains (Stevens, 1950). It is in more continuously and richly fossiliferous sections that the basis for “Upper Devonian’”’ stratigraphical palae- ontology must be sought. Acknowledgements I should like to acknowledge my indebtedness to the University of Sydney, where I held a University Post-Graduate Studentship whilst the work for this paper was being carried out. I would also like to thank Mr. D. Strusz and Mr. A. J. Wright for helpful advice, and Mr. A. M. Brough for translating the Latin diagnosis of Lepidophlotos. References ARNOLD, C. A., 1947. An Introduction to Palaeo- botany. McGraw-Hill, New York. Brown, Ipa A., 1931. The Stratigraphical and Structural Geology of the Devonian Rocks of the South Coast of N.S.W. Proc. Linn. Soc. N.S.Wa 56, 461. Croup, P. E.,. Jir., 1942; of the Silurian and Devonian. Spec. Paper 38. CRICKMAY, C. H., 1952. Discrimination of the Late Upper Devonian. /. Pal., 26, 585-609. Davip, T. W. E., AND Pittman, E. F., 1893. On the occurrence of Lepidodendron Australe(?) in the Devonian Rocks of New South Wales. fee. Geol. Surv. N.S.W., 3, 194-220. Davin, T. W. E., AND Pittman, E. F., 1893. Note on the Occurrence of Lepidodendron in Upper Devonian Rocks at Mt. Lambie, near Rydal, N.S.W. Proc. Linn. Soc. N.S.W., 8, 121-125. Dawson, J. W., 1862. On the Flora of the Devonian Terebratuloid Brachiopoda Geol. Soc. Amer. Period in North-Eastern America. Q.J.G.S., 18, 296-330. ETHERIDGE, R., JR., 1880. Fossils from the Palaeozoic Rocks of N.S.W. Jj. Roy. Soc. NS.W. ie 255, Plc ies ao: FiscHErR, F., 1904. Zur Nomenclatur von Lepido- dendvon und zur Artkritik dieser Gattung. Abhandl. dey Kén. Preussischen Geologischen Landesanstalt. Neue Folge, 39. VA OLGA ae Aiea HOURNAL ROYAL SOCIETY N.S.W. NaN wath LEPIDOPHLOIOS AND CYRTOSPIRIFER FROM LAMBIF GROUP 89 GLENISTER, B. F., 1955. Devonian and Carboniferous Spiriferids from the North-West Basin, Western Australia. Journ. Roy. Soc. W.A., 29, 46-71. GRABAU, A., 1923-24. Stratigraphy of China. Part I. Peking. GRABAU, A., 1931-33. Devonian Brachiopoda of China. I. Devonian brachiopoda from Yunnan and other districts in South China. Palaeont. sinica B., 3, Fasc. 3, 1-545. GREINER, H., 1957. “ Spirifer disjunctus.”’ Its Evolu- tion and Palaeoecology in the Catskill Delta. Peabody Mus. Nat. Hist., Yale Univ. Buil. I. Kipston, R., 1893. Lepidophioios and on the British Species of the Genus. Tvans. Roy. Soc. Edinburgh, 37, No. 25. KonINcK, L. G. DE, 1876. Foss Pal. N. Galles Sud., p. 100. English translation. Mem. Geol. Suvv. N.S.W., Pai. 6, 1898, 79-81. Mackay, Rosin M., 1961. The Lambie Group at Mt. Lambie. Pt. I. Stratigraphy and Structure. He evoc shoy. Soc: N.S.W., 95, 17-21. MAXWELL, W. G. H., 1951. Upper Devonian and Middle Carboniferous Brachiopods of Queensland. Univ. Queensland Papers, Geology, 3, No. 12. McCoy, F., 1874. Prodromus of the Palaeontology of Victoria. Decade I, 37-39. NaLivkKIn, D. V. In Fredericks, 1926. Table pour definition des genres de la Famille Spiriferidae. Acad. Sa. U:R-S.S., Buill., 393-423. PAECKELMANN, W., 1942. Beitrage zur Kenntnis devonischer Spiriferen. Abhandl. des Reichsainis fiv Bodenforschung, Neue Folge, 197. RENIER, A., 1910. Documents pour l'étude de ia Paleontologie du terrain houiller. H. Vaillant- Carmanne, Liége. SCHUCHERT, C., AND CooPER, G. A., 1932. Brachiopod Genera of the Suborders Orthoidea and Penta- meroidea. Mem. Peabody Mus. Nat. Hist., 4, pt. I. SEWARD, A. €., 1910. Fossil Plants. Vol. 2. Camb. Univ. Press. STERNBERG, K., 1826. Vol. I, fasc. 4, p. 13. STEVENS, N.€., 1950. The Geology of the Canowinira District, N.S.W. Pt. I. The Stratigraphy and Structure of the Cargo-Toogong District. J. Proce. Roy. Soe. N.S.W., 82, 319-337. SuSSMILCH, C. A., 1906. Silurian and Devonian rocks in the Orange district. Journ. Roy. Soc. N.S.W., 40, 130. UNGER, F., 1856. Denschr. der Wiener Acad. d. Wiss., 11, 175, Tab. 10, figs. 4-8. VANDERCAMMEN, A., 1959. L’étude Statisque des Cyrtospirifer du Frasnian de la Belgique. J7:sti?. Roy. Scr. Nat. de Belgique, Mem. 145. WELLs, Jf. W., 1956. The Ammonoids Koeneziies and Belocevas in the Upper Devonian of New York. j- Pal., 30, 749-751. Essai flore monde prim. Explanation of Plate I All figures are reproduced at natural size Fig. 1. Cyrtospirifer inermis. U.S.G.D. N° 13,558. Fig. 2. Same as Fig. 1, posterior view. Hig. 3. C. mermis. U.S.G.D: N° 13,570. Fig. 4. C. imermis. U.S.G.D. N° 13,564. mis. 6. C. mermis. U.S.G.D: N° 13,550. valve. mie. 6. C. oleanensis. U.S.G.D. N° 13,563. Big:--7. Same as Fig. 6, posterior view. mic. 8. C. oleanensis. U.S.G.D. N° 13,565. mie. 9. C. oleanensis. U.S.G.D. N° 13,562. Fig. 10. C. gneudnaensis. U.S.G.D. N° 13,560. iz. ll. Same as Fig. 10, posterior view. Fig. 12. Lepidophioios sp. indet. U.S.G.D. N° 7016. Internal mold. of pedicle valve, ventral view. A. Internal mold of pedicle valve. A and B. Internal molds of pedicle valves. A. External mold of pedicle valve. B. Internal mold of brachial Internal mold of pedicle valve, ventral view. Internal mold of pedicle valve. Internal mold of brachial valve. Internal mold of pedicle valve, ventral view. Yr 6 "i na ae th Rt ai eta a Journal and Proceedings, Royal Society of New South Wales, Vol. 97, pp. 91-97, 1964 Devonian Trilobites from the Wellington-Molong District of New South Wales DL) SERUSZ Department of Geology and Geophysics, University of Sydney, Sydney* ABstTRAcT—A small collection of trilobites from the Lower to Middle Devonian Garra Formation is described, including the new species Otavion munroei and Crotalocephalus packhamz. The fauna shows a strong resemblance to those already known from the Upper Silurian and Lower Devonian of south-east Australia, and it is suggested that these faunas have evolved slowly. Introduction Trilobites have not previously been described from the Garra Beds, a formation of Lower to Middle Devonian limestones and shales out- cropping in a 60-mile belt passing through Cudal, Molong and Wellington, N.S.W. A collection of several thousand specimens made in the course of detailed field-work contains only about 50 specimens of trilobites, most of which are fragmentary. The following forms have been identified, or are herein named : Scutellum (Scutellum), sp. indet. Otarion munroet, sp. Nov. Chetrurus (Crotalocephalus) packhami, sp. nov. Gravicalymene australis (Etheridge and Mitchell, 1917). Calymene, sp. nov. ? Leonaspis, sp. indet. STRATIGRAPHY: Following reconnaissance mapping by Joplin and Culey (1938) and by Basnett and Colditz (1946), and studies of the corals by Hill and Jones (1940), Hill (1942) and Jones (1944), it was thought that the Garra Beds could be divided, both lithologically and palaeontologically, into a lower series of shales, and an upper series of limestones. Detailed mapping by the author has shown that, while this subdivision remains broadly tenable, facies changes are frequent and rapid. Insufficient outcrop, coupled with these lateral and vertical changes, prevent consistent stratigraphic sub- division of the Garra Beds. Shales and calcareous shales occur throughout the sequence, but are commonest towards the base of the formation. Here, the fauna is generally poor, dominated by the corals “‘ Cyséz- phyllum”’ sp. Hill and Jones, Tvyplasma * Present address: Department of Geology, Uni- versity College, Townsville, Qld. columnare Etheridge fil., and (locally) Radio- phyllum arborescens Hill and Jones. Common brachiopods are Aivypa sp. cf. reticularis (Linné)—which extends throughout the forma- tion—and Schellwienella sp. nov. Hill (1942) distinguished this fauna from the ‘“ Murrum- bidgee ’’ fauna near Wellington, and, mainly on the basis of the favositids and Tryplasma, assigned it to the Coblenzian Stage. However, the corals—except perhaps for Radiophyllum arborescens — are found throughout the succession. Moreover, Philip (19600) has shown the difficulty of using favositids without very detailed study. Consequently the age of the lower part of the Garra Formation must for the present remain uncertain. Hill’s (1942) “ Murrumbidgee ’’ fauna, occurring in the more richly developed limestones towards the top of the formation, closely resembles the Sulcor- Loomberah fauna of Tamworth, and the Buchan Caves limestone of Victoria, which is known to be equivalent to the Couvinian in age (see Philip, 1960a). As the trilobites here described are from the lower strata, mostly the shales, they must be no younger than this. They show some affinity with previously described Upper Silurian and basal Devonian species, but are at present of doubtful use in age deter- mination. In the following systematic section, the terminology and classification in Moore (1959— Treatise on Invertebrate Paleontology, Part O) are used without modification. Specimens are housed in the palaeontological collection of the Department of Geology and _ Geophysics, University of Sydney. ACKNOWLEDGEMENTS. This work has been carried out during the tenure of a Sydney University Research Grant Studentship. The author would like to thank Dr. G. H. Packham and Dr. T. B. H. Jenkins for valuable criticism and suggestions. 92 DL StRUSZ Systematic Palaeontology Family THYSANOPELTIDAE Hawle and Corda, 1847 Scutellum (Scutellum) Pusch, 1833 TYPE SPECIES: Scutellum costatum Pusch, 1833. Givetian, Iserlohn, Germany. REMARKS: Several species have been described from Australia under the names Bronteus Goldfuss and Goldius de Koninck (junior synonyms of Scutellum Pusch). Scutellum (Scutellum), sp. indet. Plate 1) Fig d MATERIAL: Two incomplete pygidia, SU 6932 ; from road, at junction of portions 81, 104 and 105, parish of Brymedura, county Ashburnham. DESCRIPTION : The pygidia are semi-elliptical, almost flat, with a small, transverse, triangular axis which is bounded anteriorly by a very narrow straight articulating half-ring. The median lobe is slightly raised, wider posteriorly than anteriorly. Each pleural field bears seven radially arranged flat ribs, separated by narrow, shallow furrows. The median rib is wide and undivided, its sides diverging gradually posteriorly ; its forward end expands slightly to meet the median lobe. The forward ends of the two ribs on each side of the median rib are curved gently forward, to meet the median lobe tangentially. The ribs and axis are finely tuberculate. COMPARISON: Of the species described by Etheridge Jr. and Mitchell (1917), two are from ‘““Molong, Parish Bell,. . . limestone-beds adjacent to Molong’”’. Ordovician and Silurian limestones outcrop in Molong itself, and Devonian limestones of the Garra Beds are not far to the west, still in Bell parish. Of the two species, S. mesembrinus (Etheridge fil. and Mitchell) is tuberculate, but without a distinctly trilobed pygidial axis; moreover, the lateral ribs are strongly rounded. The Garra pygidia resemble those of S. bowningensts (Etheridge fil. and Mitchell, 1917) in outline. Although not visible in the figures, there 1s) 2): vaimt evidence of sparse granulation,. . .”’ on the pygidium of this species. S. cresswelli (Chapman, 1915) is poorly figured, and cannot accurately be compared with the Garra specimens. Goldius greent Chapman, 1915, is not a Scutellum. The mushroom-shaped glabella with three small lateral furrows, and the flat pygidium whose ribs bear fine transverse ridges, suggest Eobronteus Reed, 1928 (see Snajdr, 1960, p. 245). This genus does not, however, possess the ~ distinctly trilobed axis and strongly bifurcating median rib of the Victorian species. Chapman’s two species are the only Devonian ones from Eastern Australia known to me. Family OTARIONIDAE Richter and Richter, 1926 Subfamily OTARIONINAE Richter and Richter, 1926 Otarion Zenker, 1833 TYPE SPECIES: Otarion diffractum Zenker, 1833. REMARKS: Most species have been described under the junior synonym Cyphaspis Burmeister. The genus is known from the Middle Silurian to the basal Devonian of Eastern Australia. Otarion munroei, sp. nov. Plate I, figs. 2a-c; text-fig. 1 HoLotyPe: SU 6934 (cephalon only) ; from gully, por. 45, ph. Catombal, co. Gordon, 30 yds. east of por. 38. ParaTyPEs : SU 6935 to 6937 ; same locality. EtTyMoLoGy: The species is named after Mr. G. Munroe, on whose property (‘‘ Catombal’’) it was found, in appreciation fo1 his hospitality. DIAGNOSIS : Small Ofarion with highly convex cephalon; glabella separated from convex, steeply sloping pre-glabellar field by narrow furrow ; eyes large, dome-shaped ; genal spines short. DESCRIPTION—Cephalon: The cephalon is small, semi-circular, and strongly convex. The — glabella is broadly rounded anteriorly, with — gently curved sides diverging slightly posteriorly. The occipital ring is narrow, but strong; the occipital furrow is straight, deep and narrow (sag.). The Zp lateral glabellar furrows are fine, slanting sharply back to separate the small narrow triangular 2 lobes from the glabella proper. The axial furrows are deep and narrow, sharply separating the glabella from the small fixigenae. The axial furrows are truncated anteriorly by the narrow pre-glabellar furrow, whose shallow abaxial ends extend beyond the axial furrows, to die out at the facial sutures. The pre-glabellar field is convex, wide (sag.), and slopes steeply down to the border furrow. The border is convex, thick, and smooth. The facial sutures diverge rearwards across the border and border furrow, then converge to the bases of the eyes; a small palpebral lobe extends towards the top of each eye. Behind the eyes, the sutures diverge gently to the posterior margin. DEVONIAN TRILOBITES FROM WELLINGTON-MOLONG DISTRICT, N.S.W. bnew 1 Cephalon of Otarion munroet sp. nov., recon- structed from holotype and paratypes: dorsal (a) and side (b) views x10. The librigenae are large, sloping steeply up from the narrow border furrows, and are surmounted by large dome-like, subcircular to crescentic eyes. The lateral and _ posterior borders project rearwards as short, sharp genal spines. Surface sculpture is granulose, typical of the genus. The largest granules are in two short rows on the glabella, just adaxial to the 1p furrows. Thorax, pygidium : Unknown. COMPARISON: O. munroei is quite unlike the species of Etheridge Jr. and Mitchell (1893), having much larger eyes and librigenae, and short genal spines. O. lilydalensis (Chapman, 1915) is closer. In this species, the pre-glabellar field is neither as prominent nor as steeply inclined as in O. munroet, which differs also in that the posterior portions of the facial sutures 93 are not widely divergent. The large eyes distinguish O. munroez from all the foreign species that I have seen figured. Family CHEITRURIDAE Salter, 1864 Subfamily CHETRURINAE Salter, 1864 Chetrurus (Crotalocephalus) Salter, 1853 TYPE SPECIES: 1840. Calymene articulata Munster, Cheirurus (Crotalocephalus) packhanmi, sp. nov. Plate I, fig. 7; text-fig. 2 1917. Crotalocephalus sculptus Etheridge fil. and Mitchell, Pl. XXVI, fig. 11, omly. HoitotyPpE: SU6901. The Sydney Uni- versity Palaeontology Catalogue gives the location as “‘ Bank of Nora Ck., 300 yds. W. of road. The Gap, por. 191.” This is inaccurate, the exact locality being an outcrop on the north bank of the creek, 700 yards north-east of the road crossing; SE corner, por. 191, ph. The Gap (personal communication Dr. G. H. Packham). EtymMoLocy: The species is named after the collector, Dr. G. H. Packham. Diacnosis: Glabella_ parallel-sided, with bulbous frontal lobe; trans-glabellar furrows gently V-shaped, shallow axially. Fixigenae small, faintly pitted ; genal spines very short. DEscRIPTION—Cranidium: The glabella is large, parallel-sided to slightly convergent posteriorly, the greatest width being over the posterior part of the frontal lobe. The occipital ring is thick, the occipital furrow narrow, joined axially by the wide, strongly V-shaped pre- occipital glabellar furrow. The pre-occipital glabellar lobes are small, triangular. The 2p and 3f furrows are very broadly V-shaped, and relatively shallow axially. The frontal lobe is semicircular, bulbous, and slightly overhangs the narrow anterior border. The axial furrows are deep, straight and narrow. The faintly pitted fixigenae are small, each forming nearly a Cephalic Dimensions, Otarion munroei Length Glabella Specimen Height Width : No. Sagittal Overall Length Width SU 6934 3-2 3°9 2-0 5:8 1-7 3 6935 3°7 4-5-4 2-0 6-8 2-1 es 6936 3°2 3°8-++ 1-7 c. 4:6 1-7 1-3 6937 3:2 3°5+ ey) 5-0 1-5 1-4 All measurements are in mm. 94 DL. SPRUSZ Brie. 2 (a) Cephalon of Crotalocephalus packhami sp. nov. ; traced from photograph of holotype, x1; (b) cephalon of C. sculptus Etheridge fil. and Mitchell; 1907 epley Xavi tio tl, 092) — packhamt) ; traced from published photograph ; (c) cephalon of C. sculptus ; traced from pl. XXV, fig. 8, of Etheridge Jr. and Mitchell, 1917. Scales of (b) and (c) not given in original publication. quadrant of a circle. The eyes are small, close to and opposite the 3 lobes; the facial sutures run directly forward and outward from them, to enclose 90°. The fixigenae, which are narrower than the occipital ring, slope rather strongly down to the flat or gently concave border ; there is a pair of short genal spines. Librigenae, thorax and pygidium : Unknown. COMPARISON: The cephalon figured by Etheridge Jr. and Mitchell (1917, Pl. 26, fig. 11) as Crotalocephalus sculptus agrees exactly with the holotype of C. packhami. Both are quite distinct from C. sculptus S.S., which is characterized by deeply V-shaped trans-glabellar furrows. Etheridge Jr. and Mitchell did not give a locality for their specimen, nor were a number and repository listed. In C.. sélver- dalensis Etheridge Jr. and Mitchell, 1917, the glabella tapers posteriorly ; in C. packhami it is parallel-sided. REMARKS: The systematic position of C. stlverdalensis and C. sculptus is a little uncertain. Henningsmoen (p. O437, in Moore, 1959) states that Cheirurus (Crotalocephalus) has fixigenae narrower than the occipital ring, with all the glabellar furrows crossing the axis. C. (Cheirurus) has fixigenae wider than the occipital ring, and only the _ pre-occipital glabellar furrow crosses the axis. In both Crotalocephalus silverdalensis and C. sculptus there are three trans-glabellar furrows. However, the dimensions of the cephala figured by Etheridge Jr. and Mitchell clearly show that the fixigenae are wider than the occipital ring. If Henningsmoen’s diagnoses are accepted, therefore, these facts throw some doubt on the validity of the subgenera. Family CALYMENIDAE Burmeister, 1843 Subfamily CALYMENINAE Burmeister, 1843 Gravicalymene Shirley, 1936 TYPE SPECIES: G. convolva Shirley, 1936, p. 409. Upper Bala, Llandeilo, Wales. Gravicalymene australis (Etheridge fil. and Mitchell, 1917) Plate I, figs. 5a, b 1917. Calymene australis Etheridge fil. and Mitchell, p. 481, Pl. XXIV, figs. 1-7, 9 ; PI. XXVILF fies 1948. Gravicalymene australis (Etheridge and Mitchell); Gill, p. 69; PE Vibe ies: 9-12. LECTOTYPE : Specimen figured Etheridge Jr. and Mitchell, 1917, Pl. XXIV, fig. 1 ; topmost Hume “Series ’’, Yass; Upper Silurian. Sub- sequent designation Gill, 1948, p. 70. Specimen in the Australian Museum collection. MATERIAL (Garra Formation) : SU 6933, 6941 to 6949, 7900 to 7902; Mountain Waterhole Creek, ph. of Curra, west of road. SU 6940; Loombah Creek, por. 35, ph. of Catombal, 90 yds. east of por.15. SU 6938; gully, por. 45, ph. of Catombal, 30 yds. east of por. 38. DESCRIPTION: Of the 15 incomplete specimens available, a large cephalon from Mountain Waterhole Creek is the best preserved (see Pl. I). Although a little distorted, this is typical of the species, with a quadrate frontal lobe, and axial furrows only gently diverging posteriorly. The deep crescentic hollow which exists on the librigena, just forward of the postero-lateral suture, seems to be characteristic of G. australis. REMARKS: Five species of Gravicalymene have now been described from Australasia. Of these, the closest to G. australis is G. angustior (Chapman, 1915). Indeed, Etheridge Jr. and Mitchell (1917) considered that the two species might prove to be synonymous. Shirley (1938), in describing G. angustior? from the Baton River beds of New Zealand, compared his specimen closely with G. australis, and placed the species in synonymy. Gill (1945) did DEVONIAN TRILOBITES FROM WELLINGTON-MOLONG DISTRICT, N.S.W. = 95 likewise in his paper on Victorian Calymenidae, but in 1948, when the type specimens became available, he conclu’ed that the two species were distinct. Examination of published figures reveals the following criteria, additional to those given by Gill (1948). In G. australis the 3p glabellar lobes are larger and more clearly separated from the axis of the glabella than in the other species, and the frontal lobe is more quadrate in outline. Shirley’s specimen is closer to G. angustior than to G. australis, but the glabella is relatively wider posteriorly than in both these species. G. australis is known from the Hume “ Series ” of Yass, and from the Eldon Group, on the Lyell Highway 12 miles from Queenstown, western Tasmania (Gill, 1948). Gill considered that locality to be on the Siluro-Devonian boundary, but Philip (1960a, p. 154) regarded the fauna as Upper Silurian. The present specimens are consequently the first from undoubted Devonian rocks. Calymene Brongniart, 1822 TYPE SPECIES: C. blumenbacht Brongniart, 1822. Middle Silurian. Calymene, sp. nov. ? Plate I, fig. 6 HoOLoTYyPE: SU6930; Mousehole Creek, por. 221, ph. of Boree Cabonne, co. of Ash- burnham ; 780 yds. south-east of road bridge. DEscRIPTION—Cephalon: The cephalon is short, wide, crescentic, and occupies about one-fifth the total length of the carapace. The width is three times the sagittal length, 2-2 times the overall length of the cephalon. The glabella is convex, its widest place being across the pre-occipital lobes. The sides con- verge slightly towards the rounded frontal lobe, which overhangs the very narrow anterior border. The 1 lateral lobes are large, rounded, and flank the narrow (iv.) subdued occipital ring. The 7p furrows are narrow and deep; they slant rearwards, and may unite with the occipital ring. Unfortunately the axis of the glabella has been completely eroded, so this feature is uncertain. The 2 lobes are smaller than the Zp lobes, more quadrate, and slightly papillate. Both the 7/ and 2 furrows expand longitudinally at their adaxial ends, further separating the 2f and 3p lobes. The 3 lobes are mere abaxial swellings of the glabellar sides, not extending on to the upper surface. The 3 furrows are very shallow and short. The frontal lobe is short, slightly expanded, and strongly convex anteriorly. The axial furrows are narrow. The fixigenae are flat-topped, with steeply plunging antero-lateral faces and more gently convex postero-lateral areas. Low eye ridges mark the lines of geniculation. Eyes unknown, but probably small. Forward of the eyes the sutures converge slightly; their post-ocular sections sweep out and back in a wide curve, to cut the margin at the sharp genal angles. Genal spines do not occur. The posterior and lateral borders are flat, wide, and inconspicuous, contrasting with the evenly convex narrow anterior border, which is separated from the overhanging glabella by a narrow, rather deep border furrow. The librigenae are unknown, but were probably narrow, crescentic, and steeply sloping. Surface sculpture is tuberculate. Thorax: The thoracic axis is almost com- pletely eroded, but the two remaining rather distorted posterior rings are strongly arched, with large swellings at their distal ends. The axial furrows are deep and narrow. The pleurae are flat adaxially, steeply inclined to vertical abaxially, their distal ends spatulate. The anterior pleural bands are strong, laterally directed until just inside the fulcrum, when they (with the remainder of the pleura) slant rather strongly rearwards. The pleural furrow and posterior band are subdued, and parallel the anterior band. There are 12 thoracic tergites. The thorax is a little narrower than the cephalon anteriorly, and becomes gradually narrower rearwards. Pygidium: The pygidium is missing, but the outline remains. This is triangular, narrower than the last thoracic tergite, and rather longer than in typical Calymene. COMPARISON: Calymene S.S. is not well represented in Australia, most calymenid species being Gravicalymene. C. bower Gill, 1945, and C. killarensis Gill, 1945, both from the basal Devonian of Victoria, are quite distinct from the Garra species; in particular, they possess a much stronger anterior border. C. dum Etheridge Jr. and Mitchell, 1917, which was stated to be an exceptionally large Calymene, cannot be compared with the Garra species, as the cephalon is unknown. Until further material of this species becomes available, it is best left unnamed. 96 Do i ST RUSZ Family ODONTOPLEURIDAL Burmeister, 1843 Subfamily ODONTOPLEURINAE Burmeister, 1843 Leonaspis Richter and Richter, 1917 (LYPE SPECIES :; Odontopleura Leonhardi Barrande, 1846, p. 38. Lower Ludlovian Kopanina Limestone, near Beroun, Czecho- slovakia. REMARKS: Leonaspis is distinguished from Odontopleura by its shorter, more robust librigenal spines, which are slanted rearwards. In Acidaspis the spines are directed vertically downwards. Leonaspis, sp. indet. Plate I, figs. 3, 4 MATERIAL: SU6931 (external mould of librigena) ; por. 4, ph. of Boree Nyrang, co. of Ashburnham, 80 yds. north-west of bridge over Walker’s Creek. SU 6939 (portion of librigena) ; from old road, southern boundary of por. 64, ph. of Catombal, co. of Gordon. DESCRIPTION: The librigenae are small, crescentic. The lateral borders are thick and relatively wide, bearing a row of small nodes. The librigenal spines are short, rectangular, abruptly truncated distally, and directed slightly rearwards. The lateral border furrows are faint. The librigenae slope steeply upwards to the small, bulbous, crescentic eyes. The upper portions are finely tuberculate. The genal spines are narrow, circular in section, and directed slightly outwards and rather noticeably downwards. COMPARISON: Prantl and _ PYibyl (1949, p. 154) noted that Leonasfis occurs in Australia, but did not name the species. Etheridge Jr. and Mitchell (1896) described four species of Odontopleura from the Silurian of Yass; of these, only O. ratte: resembles Leonaspis sp. This species, however, has the rearmost two or three librigenal spines based on the genal spines, and also has a completely tuberculate cephalon. The tubercles in Leonaspis sp. are confined to the upper portions of the librigenae. Leonaspis (Leonaspis) dormitzert (Hawle and Corda, 1847), from the Silurian of Czecho- slovakia is very similar to Leonaspis sp., but it also is more strongly tuberculate. References BARRANDE, J., 1846. Notice préliminaire sur le systéme Silurién et les Trilobites de Bohéme. Leipzig. (Fide Prantl and Pribyl, 1949.) BasnettT, E. M., anpb Cotpitz, M. J., 1946. General Geology of the Wellington District, N.S.W. J. Proc. Roy. Soc. N.S.W., 79 (1945), 37-47. 1822. Histoire Paris and Strasbourg. naturelle des (Fide BRONGNIART, A, Crustacés fossiles. Shirley, 1936.) CHAPMAN, F., 1915. New or Little-known Victorian Fossils in the National Museum. Part XVIII. Some Yeringian Trilobites. Roy. Soc. Victoria, Proc. (N.S.), 28, 157-171, pls. XIV—XVI. ETHERIDGE, R., JR., AND MITCHELL, J., 1893. The Silurian Trilobites of New South Wales, with References to those of Other Parts of Australia. Part II. The Genera Proetus and Cyphaspis. Linn. Soc. N.S.W., Proc. (Ser. 2), VIII, 169-178, VI-VII. ETHERIDGE, R., JR., AND MITCHELL, J., 1896. The Silurian Trilobites. .. Part IV. The Odonto- pleuridae. Jbid., XXI, 694-721, L-LV. ETHERIDGE, R., JR., AND MITCHELL, J., 1917. The Silurian Trilobites. .. Part VI dhe) Caly- menidae, Cheiruridae, Harpeidae, Bronteidae, etc., with an Appendix. Jbid., XLII, 480-510, XXIV-XXVII. Gut, E. D., 1945. Tulobita ~ of the, | family, Calymenidae from the Palaeozoic Rocks of Victoria. Roy. Soc. Victoria, Proc. (N.S.), LVI, 171-186, VII. GitL, E. D., 1948. Eldon Group Fossils. Queen Victoria Mus. (Launceston), Rec., 2, 57—74, 7-8. Hawte, I., and Corpa, A. J. C., 1847. Prodrom einer Monographie der b6dhmischen Trilobiten. K. bohm. Gesell. Wiss., Abh., 5. Prague. (Fide Prantl and Pribyl, 1949.) Hitt, D., 1942. Middle Palaeozoic Rugose Corals from the Wellington District, N.S.W. J. Proc. Rov. Soc. N.S.W., 76, 182-189, V—VI. Hitt, D., anp Jones, O. A., 1940. The Corals of the Garra Beds, Molong District, New South Wales. Ibid., 74, 175-208, II-VIII. Jones, O. A., 1944. Tabulata and Heliolitida from the Wellington District, N.S.W. JIbid., 77 (1943), 33-39, I. Jorrin, G. A., AND CuLEy, A. G., 1938. The Geo- logical Structure and Stratigraphy of the Molong- Manildra District. Jbid., 71 (1937), 267-281, IT. Moore, R. C. (ed.), 1959. Treatise on Intertebrate Paleontology. Part 0Q—Arthropoda 1 0 1-560. Geol. Soc. Amer. & Univ. Kansas Press. Lawrence, Kansas. Munster, G., 1840. Die Versteinerungen des Ueber- gangskalkes mit Clymenien und Orthoceratiten von Oberfranken. Beitr. z. Petvefacten-Kunde, Ill, 7, 33-121, 5-20. (ide Prantl & Priby® 1949.) Puitip, G. M., 1960a. Victorian Siluro-Devonian Faunas and Correlations. Internat. Geol. Cong., 21st, Copenhagen 1960, Rept., 7, 143-157. Puitie G. M., 1960b. The Middle Palaeozoic Squamulate Favositids of Victoria. Palaeontology, 3, 186-207, 30-34. PRANTL, F., AND PkRiByL, A., 1949. A Study of the Superfamily Odontopleuracea Nov. Superfam. (Tri- lobites). Czechoslovakia Stdtntho Geol. Ustavu, Rozpravy, 12, 1-221, 1-11 (English summ. pp. 117-221). neu rRNAL ROYAL SOCIETY N.S.W. SRO SZ eA Tee DEVONIAN TRILOBITES FROM WELLINGTON-MOLONG DISTRICT, N.S.W. 97 Puscu, G. G., 1833. Geognostische Beschreibung von Polen, so wie den tibrigen Nordkarpathen-Landern. Ercrers) Weil, Stuttgart & Tiibingen. (Fide Snajdr, 1960.) - RICHTER, K., AND KicuTEerR, E., 1917. Uber die Einteilung der Familie Acidaspidae und _ iber einige ihrer devonischen Vertreter. Centvalbl. f. Min., Geol., etc., Jahvg. 1917, 462-472. (Fide Prantl and Pyibyl, 1949.) SALTER, L. W. 1853. Figures and Descriptions Illustrative of British Organic Remains. Geol. Surv. Great Britain, Mem., dec. 7, pls. 1-10. (Fide Moore, 1959.) SHIRLEY, J., 1936. Some British Trilobites of the Family Calymenidae. Geol. Soc. London, Quart. Jour., 92, 384-422, XXIX-XXXI. SHIRLEY, J., 1938. The Fauna of the Baton River Beds (Devonian), New Zealand. TIbid., 94, 459-506, XL-XLIV. Snajpr, M., 1960. A Study of the Family Scutellidae (Trilobitae). Ustredntho ustavu geol., Rozpravy 26, 1-264, 1-36 (English summ. pp. 223-262). ZENKER, J. C., 1833. Beitrage zur Naturgeschichte der Urwelt. Jena. (Fide Erben, 1952: Neues Jahrb. Geol. Paléont., Abh. 94, 150-362.) Explanation of Plate 1 All specimens whitened with ammonium chloride, and illuminated from top left. . Scutellum (Scutellum), sp. indet. Otavion munroei, sp. nov. Holotype, SU 6934 ; Leonaspis, sp. indet. Leonaspis, sp. indet. enclosing shale; (a) lateral view, x1:4; . Calymene, sp. nov. ? visible; x1-0. 7. Chetrurus (Crotalocephalus) packhami, sp. nov. holotype, SU 6901, x 2-3. Do UR ko Localities given in text. Dorsal view of incomplete pygidium, SU 6932, x3-2. (a) lateral, (6) anterior, (c) dorsal views, x 5-2. Dorsal view of incomplete librigena, SU 6939, x 4-0. Lateral view of mould of librigena, SU 6931 ; genal spine indicated by arrow ; . Gravicalymene australis (Etheridge fil. and Mitchell, 1917). (b) dorsal view, Dorsal view of carapace, holotype SU 6930; the impression of the pygidium is faintly x 2-4. Cephalon, SU 6941, distorted by compaction of KD 2: Dorsal view of incomplete, partly decorticated cephalon, —————————————————————— eee AUSTRALASIAN MEDICAL rUBLISHING CO, LTD. SEAMER AND ARUNDEL STS., GLEBE, SYDNEY fis ~~ -~ LL ENCY THE ee ee ee ‘OF THE , CommonwaaLTH OF. AUSTRALIA, : LONOURAB LE VISCOUNT DE L'ISLE, VCE. Cy G.C.M, .G., G.C.V.0., K. St. F. we His EXCELLENCY THE GovERNoR OF. New Sovran Watzs, ss Generar SIR ‘ERIC Ww. AOD WARD: KCM. Guy K.C.V.0., C, Be, CB.E., D.S.0, | "iecsideat as : Che : 3 a ig Gt | ae ae ck McKERN, M.So. BR en, "Vice-Presidents Z Fy Oe ee ia i meas a : WwW. 2 G. POGGENDOREF, B.Se.Aer, ap is B. GO asia MA is Hon. Secretaries eS tae wee re on ALAN A. DAY, B.S0., Ph, “De Hows ‘Treasurer Coe Cs eo a x i oe L. ADAMSON, Bese. ee ae Ee Members: of Council AG Feetae oes tla Nea nay 'UMPHRIES, B.Sc” Shs co egine es A. KEANE, Php. 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Authors who. are members 6 Society receive 50 copies of each. paper. f they are ordered by the cape wae As Journal and Proceedings, Royal Society of New South Wales, Vol. 97, pp. 99-105, 1964 Precise Observations of Minor Planets at Sydney Observatory During 1961 and 1962 W. H. ROBERTSON Sydney Observatory, Sydney The programme of precise observations of selected minor planets which was begun in 1955 is being continued and the results for 1961 and 1962 are given here. The methods of observa- tion and reduction were described in the first paper (Robertson, 1958). All the plates were taken with the 9-inch camera by Taylor, Taylor and Hobson (scale 116” to the millimetre). Four exposures were made on each plate. In Table I are given the means for all four images for the separate groups of stars at the mean of the times. The differences between the results average 0 -8028 sec 6 in right ascension and 0”-32 in declination. This corresponds to probable errors for the mean of the two results from one plate of 08-012 sec 6 and 0”-14. The result from the first two exposures was compared with that from the last two by adding the movement computed from the ephemeris. The means of the differences were 08-011 sec 38 in right ascension and 0”-13 in declination. No correction has been applied for aberration, light time or parallax but the factors give the parallax correction when divided by the distance. The observers at the telescope were W. H. Robertson (R,) K. P. Sims (S) and Harley Wood (W). In accordance with the recommendation of Commission 20 of the International Astronomical Union, Table II gives for each observation the positions of the reference stars and_ the dependences. The columns headed “R.A.” and “ Dec.’”’ give the seconds of time and arc with proper motion correction applied to bring the catalogue position to the epoch of the plate. Star 7901 in observation 491 was assumed to be in error by 10”. The column headed “ Star ”’ gives the number from the Yale Catalogue (Vols. 11, 12 I, 12 II, 13 I, 14, 16, 17, 21) and the Cape Catalogue of Faint Stars. I wish to acknowledge the assistance of Mrs. J. Brannigan and Mrs. Y. Lake in the measurement and reduction of some of the plates. Reference RoBERTSON, W. H., 1958. J. Proc. Roy. Soc. N.S.W.., 92, 18; Sydney Observatory Papers, 33. TABLE I R.A. Dec. Parallax No. (1950-0) (1950-0) Factors h m S (eo) / Ww S LA 6 Hebe 1961 U.T. 419 July 27-78721 Ol 35 42-598 —0Ol1 30 11-78 —0:036 —4-69 R 420 July 27-78721 Ol 35 42-559 —0O1 30 11:88 421 Aug. 14-76628 Ol 58 40-068 —03 06 57-04 +0:-002 —4-48 R 422 Aug. 14-76628 Ol 58 40-032 —03 06 57-00 423 Aug. 21-74740 027505) 42-212 —04 06 00-73 —0:013 —4:35 S 424 Aug. 21-74740 02 05 42-168 —04 06 00-96 425 Sep. 12-70452 02 18 43-326 —-08, 22) 51-12 +0:013 —3:-76 W 426 Sep. 12-70452 02 18 43-309 —08 22 51-30 427 Sep. 20-67634 02 19 28-255 —l10 14 06-66 —0:009 —3:50 R 428 Sep. 20-67634 02 19 28-321 —10 14 06-66 429 Oct. 10-61343 02 12 19-112 —14 38 50-47 —0:020 —2:87 R 430 Oct. 10-61343 Ol, P22 192197 —l4 38 50-30 431 Oct. 19-57907 02 06 03-884 —l16 06 12-22 —0:037 —2-67 S 432 Oct. 19-57907 02 06 03-910 —l16 06 12:04 433 Oct. 25 -57533 02 O1 30-826 —l16 46 21-24 +0:-013 —2-56 W A emrtecnuihe mnaeeaan €& 2 cme 100 488 Oct: Oct. Oct. Nov. Nov. Nov. Nov. Dec. Dec. Apr. Apr. May May May May May May June June June June June June July July July July July July July July Aug. Aug. Aug. Aug. Aug. Aug. Aug. Aug. Sep: Sep. Sep. Sep. Apr. Apr. May May May May May May May May June June W. H. ROBERTSON TABLE I—Continued 25-57533 30-5622] 30: 56221 09-51213 09-51213 13 -49922 13 -49922 05- 45449 05 - 45449 7 Iris 1961 U.T. 11-78793 11-78793 08-74170 08-74170 16-71559 16-71559 22-70626 22-70626 14-61396 14-61396 19-60153 19-60153 26 - 57804 26-57804 03 - 56204 03 - 56204 10-52800 10-52800 19-51612 19-51612 27-47990 27-47990 01- 46364 01-46364 08-43635 08+ 43635 15-42171 15-42171 28-40487 28-40487 04-37400 04-37400 06-37798 06-37798 433 Eros 1961 U.T. 11-60387 11-60387 02 -52902 02-52902 08-51761 08-51761 16-47738 16-47738 11 Parthenope 1962 U.T. 29- 81252 29- 81252 06-79143 06- 79143 R.A. Dec. (1950-0) (1950-0) h m Ss ° 4 “a 02 Ol 30-768 —l16 46 Ol 57 46-364 —17 O07 Ol 57 46°340 —17 O07 Ol 51 10-232 —l17 13 Ol 51 10-274 —l17 13 01 49 04-249 —l17 03 Ol 49 04-234 —l17 03 O01 45 29-163 —14 20 Ol 45 29-150 —14 20 18 40 55-621 —23 12 18 40 55-692 —23 12 18 48 32-426 —22 24 18 48 32-454 —22 24 18 47 05-706 —22 11 18 47 05-670 —22 11 18 44 48-917 —22 02 18 44 48-920 —22 02 18 27 34-860 —21 29 18 27 34-795 —21 29 18 22 28-432 —21 22 18 22 28-410 —2] 22 18 14 58-614 —21 11 18 14 58-632 —21 11 18 O7 24-946 —21 00 18 O07 25-026 —21 00 18 00 12-874 —20 49 18 00 12-850 —20 49 17 52 02-235 —20 35 17 52 02-254 —20 35 17 46 19-986 —20 25 17 46 19-918 —20 25 17 438 38-129 —20 19 17 43 38-112 —20 19 17 41 05-100 —20 12 17 41 05-080 —20 12 17 40 00-988 —20 07 17 40 00-944 —20 07 17 41 56-036 —20 02 17 41 55-986 —20 02 17 44 55-818 —20 02 17 44 55-770 —20 02 17 46 01-864 —20 02 17 46 01-821 —20 02 13 58 28-306 —49 47 13 58 28-264 —49 47 13 22 58-950 —45 31 13 22 58-980 —45 31 13. 17 08-916 —43 28 13 #17 «208-914 —43 28 13 138 15-956 —40 35 13 13 15-944 —40 35 22 05 33-484 —ll 26 22 05 33-532 —ll 26 22°13) Soe) —10 57 22 AS Posen le —10 57 22: 13- 13- 39: 39- 24- 24- Ol- Ol- Parallax Factors . S +0-022 —2- —0-035 —2 —0:037 —2: +0-:020 —2 —0:054 —1: +0:019 —1l- +0-010 —l- +0-38 —1l: —0:020 —1- —0:004 —1 —0:002 —1l- +0-026 —l- —0:007 —1-: +0:053 —2- +0:019 —2:- +0-017 —2- —0:004 —2: +0:013 —2: +0-069 —2:- +0:024 —2:- +0-053 —2:- —0:022 +2 +0-011 +1 +0:049 +1 —0:017 +1 —0:009 —3 —0:024 —3 -40 On ww neongnhe egy gon gnvn wa gee a nn wn No. 489 490 491 492 493 494 495 496 497 498 499 500 501 502 503 504 505 506 507 508 509 510 511 512 513 514 515 516 517 518 519 520 521 522 523 524 525 526 527 528 529 530 531 532 533 534 535 536 537 538 539 540 541 542 543 544 545 546 547 548 549 550 PRECISE OBSERVATIONS OF MINOR PLANETS DURING 1961 AND 1962 June June June June June June July July July July July July July July Aug. Aug. Aug. Aug. Aug. Aug. Aug. Aug. Sep. Sep: Sep. Sep. Oct. Oct. Oct. Oct. Oct. Oct. Oct: Oct. Feb. Feb. Mar. Mar. Mar. Mar. Mar. Mar. Mar. Mar. Apr. Apr. Apr. Apr. Apr. Apr. Apr. Apr. May May May May May May June June June June 12- t2- -77341 Pad 25° 25° 04- 04- 12- 12- 16: 16- 24- 24: 02- 02- 09- 09- 22: 22: 27° an: 03: 03- 24: 24: 05- 05- 1l- -45684 16: 16- 22: 22: 21 11 40 Harmonia 1962 U.T. 28- 28- 06: 06- 12- 12- 20- 20- 26> 26- 02: 02: 12- 12- 18: 18: - 60287 - 60287 -58110 -58110 -51964 -51964 -49161 -49161 -46352 46352 -46401 -46401 78371 78371 77341 75437 75437 74123 74123 71871 71871 69581 69581 68614 68614 67995 67995 62938 62938 59731 59731 57600 57600 55885 55885 47829 47829 46159 46159 45684 42028 42028 41220 41220 76480 76480 74590 74590 73321 73321 70465 70465 69445 69445 67796 67796 66486 66486 63828 63898 TABLE I—continued - 643 2-684 -100 -104 ‘751 - 784 - 246 -318 -345 -298 *939 *924 * 242 -248 -032 -026 -670 -644 -786 2700 ‘089 -069 -456 -502 -535 -492 -380 -368 -900 -936 2022 -927 -320 - 298 -755 - 764 °381 -416 *374 -346 -586 -554 -491 -456 -214 -241 -983 -998 °677 -690 -478 -498 -460 -492 *212 -196 -563 -609 -702 -706 -616 -616 —10 —10 —10 —10 —10 —10 —10 —10 —10 —10 —ll1 —ll —ll1 —l] —12 —12 —13 —13 —l4 —14 —15 —15 —16 —16 —17 —17 —17 —17 —17 —l7 —l17 —17 —17 —17 —ll —ll —Ill —ll1 —ll —ll1 —10 —10 —10 —10 —10 —10 —09 —09 —09 —09 —08 —08 —08 —08 —07 —07 —O07 —O07 —07 —O7 —07 —07 20 36 11 -56 -26 -34 -96 -96 -77 -46 -44 “58 -96 -42 -75 -02 -95 a) Re) = 2iL -40 -44 -46 -42 -57 -68 “96 52- °33 04 -08 -47 -79 94 -10 -98 °45 -36 31 -98 -22 84 -13 “75 -90 -09 -72 -56 -68 -54 -90 -78 -70 55> 56: 17- LT: 10- 1l- 48- 48- 15- 15- 42- 42- Isl -34 82 54 54 68 91 24 78 56 74 92 37 20 32 S +0: aan (hs Parallax Factors ; 008 —3- °023. —3 007 —3 -022 —3 ‘017 —3 020 —3 022 —3 088 —3 000 —3 033 —2 018 —2 037 —2: Oll —2 034 —2- 070 —2 007 —2 013. —2: 003 —3: 009 —3:- 000 —3- 020 —3: 002 —3 039 —3- 076 —32- 058 —3: 020 3° 026 —3- 044 —3- 026 —3- 005 —3: 025 —3: 44 -48 -48 -47 -43 -40 “31 -21 -06 -83 ‘75 101 = 102 W. H. ROBERTSON TABLE I—continued R.A Dec: Parallax No. (1950-0) (1950-0) Factors h S g fi u” Ss ” 551 June 11-44848 14 Ol 02-888 —O7T 33 04-59 +0-:0138 —3-86 552 June 11-44848 14 O1 02-899 —O7 33 04-36 553 June 21-41682 14 00 37-719 —08 Ol O1-94 +0:001 —3-80 554 June 21-41682 14 00 37-696 —08 Ol 02:43 555 June 28-40383 14 O01 59-758 —O8 28 54-29 +0:016 —3-74 556 June 28-40383 14 Ol 59-769 —O0O8 28 54-29 557 July 12-36981 14 08 31-024 —09 41 45:55 +0:016 —2-57 558 July 12-36981 14 08 31-000 —09 41 45-08 559 July 20-36760 14 14 16-608 —10 31 43-16 +0:064 —3-46 560 July 20- 36760 14 14 16-628 —10 31 42-20 TABLE IT No Star Depend. R.A. Dec No. Star Depend. TX. Dec: 419 368 0-373198 19-089 47-50 434 519 0-458548 32-852 34-12 385 0- 276696 54-016 15-60 539 0- 237602 01-026 33-04 318 0-350105 31-690 18-72 541 0-303850 18-009 34:58 420 300 0- 241710 24-626 20:07 435 498 0- 349603 29-981 09-68 324 0- 403268 31-441 18-79 516 0: 412348 13-798 10:88 380 0- 355022 34-533 43°53 547 0- 238048 31-019 10:69 421 458 0- 278020 23-617 51-29 436 521 0- 245123 13-461 53°97 462 0- 308204 05-030 27-94 505 0- 453920 21-600 29-85 491 0-413775 22-522 07-05 543 0-300957 30-224 59-37 422 452 0- 331356 23°977 18-63 437 461 0- 249776 22-212 28-79 473 0-379204 28-359 09-43 479 0- 362570 36-610 04:43 496 0- 289440 39:771 36-64 498 0- 387653 29-981 09-68 423 495 0: 341049 38-263 36-96 438 467 0-345146 03-994 09-83 510 0:444391 17-077 31-42 482 0-317678 44-700 13-44 522 0- 214560 22-276 54-11 500 0-337176 43-632 13-98 424 496 0: 308248 39-771 36-64 439 492 0-372340 38-980 43°31 507 0 - 268823 29-994 15:06 459 0-413824 00-476 34-23 513 0- 422930 02-816 51-11 499 0- 213836 36-236 10-78 425 501 0-379598 59-835 21-62 440 442 0- 365044 13-677 00-34 §12 0-339614 12-262 16-19 464 0-312524 59-365 48-79 527 0- 280789 49-367 05-43 498 0- 322432 29-981 09-68 426 502 0: 301926 23-052 16-28 44] 434 0- 362738 42-101 44-85 511 0: 462516 31-819 46-18 439 0: 294578 01-068 03-69 529 0- 235558 05-766 30-97 473 0- 342684 41-536 26-88 427 524 0: 400380 26-188 51-21 442 433 0- 266008 24-210 02-59 540 0: 273218 34-370 20-33 444 0: 356774 30-505 18-71 515 0: 326402 22-117 44-36 458 0:377218 38 - 223 06-64 428 521 0- 333154 45-476 14-19 443 12975 0-325558 53-196 06:46 541 0- 363132 45-143 57-88 13005 0- 308236 09-379 37-94 511 0: 303713 31-821 46:18 13023 0- 366206 32-594 16-51 429 564 0: 333154 40-150 34:83 444 12966 0- 333650 13-873 60-04 577 0: 245448 34:731 15-70 13002 0- 386490 58: 641 08-62 601 0: 421398 26-099 50:36 13039 0- 279860 03-717 52-95 430 562 0: 251628 22-340 13-27 445 13058 0- 346246 26-525 14-08 599 0- 384582 42-349 18-14 13098 0- 286732 31-365 29-72 508 0-363791 10-291 42-72 13136 0- 367022 28-521 45-59 431 541 0- 368470 18-008 34-57 446 13055 0- 275528 10-636 33-94 562 0: 274503 22-341 13-27 13126 0- 313384 04-271 47-62 566 0-357027 55-021 15:07 7941 0-411088 51-837 08-26 432 533 0- 349310 06-742 18-56 447 7873 0- 296022 03-889 32-30 556 0- 327920 16-259 36-40 7941 0- 303856 51-837 08 - 26 574 0-322770 08-164 30-70 13110 0-400122 29-385 13-10 433 516 0-374054 13-798 10-88 448 7872 0: 376250 02-955 50:85 528 0: 348820 02-036 21-96 13098 0- 279522 31-365 29-72 550 0- 277126 11-941 55:14 13136 0: 344228 28-521 45-59 PRECISE OBSERVATIONS OF MINOR PLANETS DURING 1961 AND 1962 No Star Depend. 449 13023 0- 287025 13114 0- 284058 7882 0-428917 450 7872 0:413442 7941 0- 252964 13055 0-333594 451 7708 0- 448498 7756 0- 300646 12855 0- 250856 452 7709 0-346718 7782 0+ 255236 12814 0-398046 453 7670 0- 205832 7673 0-470918 7708 0-323250 454 7650 0- 265106 7689 0-431697 7709 0-303197 455 7542 0-335196 7630 0- 349942 7636 0-314862 456 7563 0+ 241785 7603 0: 503636 7640 0+ 254579 457 7457 0-331636 7526 0-337197 7542 0-331167 458 7476 0-342070 7478 0- 283596 7570 0-374334 459 7384 0-315787 7404 0- 266942 7472 0-417270 460 7375 0- 298622 7412 0- 305905 7473 0-395472 461 7316 0: 297861 7334 0-385024 7384 0-317114 462 7311 0-314298 7353 0-308714 7358 0-376987 463 7279 0- 405084 7316 0-374288 7315 0- 220628 464 7288 0- 282413 7291 0-389892 7334 0-327695 465 7261 0-358654 7286 0-374712 7315 0- 266634 466 7266 0-352678 7281 0-356682 7311 0- 290640 467 7244 0- 212338 7289 0- 362066 7263 0-425596 468 7245 0-428213 7281 0- 219120 7288 0-352667 469 7244 0- 359726 7249 0: 298707 7288 0-341566 470 7235 0+ 246085 7289 0-319722 7257 0-434193 TABLE I]—continued Dec. 16-50 14-24 48-14 50°85 08-26 33°94 56°17 50-79 30°88 36-23 54-86 39-71 46-07 43-52 56-17 30°33 31-36 36-23 33°85 44-48 21-61 46-57 26-44 19-09 19-56 46°89 33°85 57-88 05-16 15-87 36-00 57-63 30°57 12-13 50°47 42-57 49-53 41-20 36-00 15-06 13-18 34°95 06-58 49-53 59-31 48-74 54°75 41-20 02-75 31-05 59-31 25-55 25-74 15-06 20-78 09-83 06-95 02-20 25-74 48-74 20-78 57-16 49-29 45-24 09-83. 46-77 No. 473 474 475 476 477 478 479 480 481] 482 483 484 485 486 487 488 489 490 Star 7244 7304 7269 7245 7286 7296 7269 7315 7291 7261 7303 7312 7279 7309 7320 7289 7296 7334. 11611 11649 Ney 11638 11655 11708 10943 10994 11069 10957 11019 11036 10873 10896 10945 10867 10902 10927 10768 10849 10865 10752 10889 6356 7806 7827 7838 7813 7819 7836 7858 7862 7878 7843 7873 7876 7878 7889 7893 7867 7891 7892 7901 7933 7938 7915 7918 7941 Depend. - 248796 -319868 -431336 - 366182 - 340772 - 293046 - 297304 - 356499 - 346196 - 301768 - 287701 410531 425582 - 229194 345225 486456 246794 266750 340003 349620 -310377 -393375 - 387606 - 259019 - 366035 - 265090 - 368874 -317470 -446096 - 236434 - 286981 -480242 °232777 - 305884 -412430 - 281686 - 236760 - 242738 - 520502 - 284626 - 280204 -435170 » 249817 -372482 -377701 358749 269713 371538 356316 371538 272146 307558 -432280 - 260162 412586 -321694 - 265720 - 299108 -321726 -379166 -319735 -353710 -326555 -386316 - 281074 -332610 ee 52° 28> 55° 58: 42- 47- 55° 46- 25° 44- 42- 13- 42- 39: 03> “318 47- 49- 49- 35: 23° 20- 55: 50: 56- 23° 27° 39- 44- 40- 21° 48: 57: 57: O1 31 125 086 624 884 695 962 624 194 569 151 130 499 222 378 175 962 152 91 91 09 14 31 28 49 16 02 39 92 00 50 23 02 00 -96 58: 37° 49- 39- 03- 26- 58: 21- 28- 05- 14: 25: 53° 54: 51: 38: 55> ll; 15: 38- 14- 16- 03- 09- 08- 53° 14- 40- 46- 10- 04: 80 33 37 85 89 87 39 305 210 921 216 906 678 092 266 422 768 199 692 422 44] 922 526 559 977 082 083 238 402 295 752 WOAWHRUWAARDROMROADISHSAUSL = : aoa 10 & oo = Saar 103 “12 AwMADw SCHNSH me Ow SO 0 = COO = PADI OW oO bo @ Ot 104 W. H. ROBERTSON TABLE [I—continued : No. Star Depend. R.A. Dec. No. Star Depend. R.A. Dee: 493 7915 0- 214108 46-401 16-85 515 9298 0-441737 41-615 14-33 7946 0- 438808 36-237 05-88 9350 0-309120 36-695 38-82 7953 0-347083 38-807 20-12 8199 0- 249142 44-239 51°32 494 7918 0- 272332 10-295 50-38 516 9323 0-418159 27-051 50-06 7938 0- 463200 40-237 08-70 9324 0- 432536 29-027 40-08 7959 0- 264468 02-647 45-45 9343 0- 149304 44-187 10-83 495 7953 0-406312 38-807 20-12 517 9323 0- 260247 27-051 50-06 7956 0- 319266 47-940 52-53 9326 0- 380952 53° 541 51-77 7974 0- 274422 01-038 50-03 9343 0- 358800 44-187 10-83 496 7941 0+ 322242 04-751 01-91 518 9310 0- 369444 31-376 00-29 7965 0- 315676 42-784 48-76 9350 0- 213785 36-695 38-82 7969 0- 362082 27-647 50-42 8199 0-416771 44-239 51-32 497 7950 0-187178 27-266 47-86 o19 9326 0- 446960 53-541 51-77 7967 0-508641 09-369 42-21 9367 0- 246729 20-920 33°92 7969 0-304181 27-647 50-42 8199 0- 306311 44-239 51-32 498 7956 0: 450917 47-940 52-53 520 9324 0- 322062 29-027 40-08 7961 0- 200856 13-186 55-03 9350 0: 273662 36-695 38-82 7974 0-348226 01-038 50-03 _ 8207 0- 404276 58-202 13-50 499 7956 0+ 290243 47-940 52°53 521 8199 0- 329324 44-239 51-32 7964 0-386971 42-811 33-12 8239 0- 342894 34-084 21-38 7969 0-322786 27-647 50-42 9350 0-327782 36-695 38-82 500 7945 0- 269273 24-192 36-66 522 9343 0- 426503 44-186 10°83 7967 0- 503572 09-369 42-22 8211 0- 208966 17-352 09-96 7980 0: 227155 27-338 26-52 8241 0- 364531 41-321 00-23 501 7947 0-315592 49-784 18-65 523 5235 0- 342406 19-314 23-90 7949 0-311004 14-314 57-77 5246 0-391068 48-842 58-42 7969 0-373404 27-647 50-42 5266 0+ 266526 21-240 20-12 502 7932 0-358776 13-048 40-03 524 5226 0- 352569 09-524 34°88 7950 0-301760 27-267 7:86 5245 0- 326270 33° 389 14-38 7980 0-339463 27-338 26-52 5269 0-321166 19-804 16-49 503 7913 0- 231602 28-600 18-49 525 5253 0- 272691 01-698 41-19 7919 0+ 340952 17-783 19-39 5259 0- 476516 00-474 57°43 7947 0-427446 49-784 18-65 5269 0- 250794 19-804 16-49 504 7910 0- 257184 43-763 52-12 526 5246 0-447891 48-842 58-42 7931 0-392556 10-841 04-63 5265 0- 261167 00-730 18-85 7942 0-350259 06-359 13-7 5273 0- 290942 34-332 48-57 505 8347 0-416275 15-572 03-00 527 5259 0-458519 00-474 57-43 8385 0- 145919 01-108 24-11 5266 0+ 254837 21-240 20-12 7907 0-437806 15-535 13-16 5273 0- 286644 34-332 48-57 906 7884 0-370733 00-898 48-98 428 5250 0-424868 40-431 44-86 7921 0- 174106 34-996 49-98 5265 0- 288580 00-730 18-85 8370 0-455160 23-241 07-77 5283 0- 286551 44-567 24-42 507 8292 0- 289780 06-596 03-87 529 5253 0- 248924 01-698 41-19 8305 0- 350249 24-804 07-13 5258 0- 368826 54-971 34-21 8325 0-359971 13-975 52-82 5273 0-382250 34-332 48-57 508 8299 0- 306654 30-303 21-38 530 5245 0- 236181 33-389 14-38 8301 0: 383882 52-592 17-44 5266 0-504773 21-241 20-12 8317 0- 309464 19-290 07-28 5275 0- 259046 48-425 43-72 509 8272 0- 309874 15-442 36-41 531 5250 0- 234704 40-431 44-86 8289 0-477224 01-204 24-97 5254 0-345210 09-201 30-25 8306 0- 212902 36-117 17-50 5260 0- 420086 27-811 09-52 510 8279 0- 368339 09-373 47-36 532 5245 0-397980 33-389 14-39 8286 0-389856 58-496 22-44 5253 0- 362042 01-698 41-20 8301 0- 241805 52-592 17-44 5275 0- 239978 48-425 43-72 511 8238 0-323944 31-617 26-29 533 5220 0- 322406 38-834 42-45 8254 0- 234491 06-323 06-74 5260 0-377680 13-061 21-79 8279 0-441566 09-373 47-36 5234 0- 299914 44-249 21-73 512 8260 0-214112 44-662 40-81 534 5227 0- 385425 16-497 19-95 8266 0-384111 02-617 21-25 5251 0- 256065 46-563 19-19 8267 0-401777 28-928 20-01 5239 0-358510 03-780 09-18 513 9310 0-272113 31-376 00-29 535 5195 0-410197 12-467 05-59 9350 0- 237398 36-695 38-82 5203 0- 291532 28-996 45-89 8199 0-490489 44-239 51-32 5219 0- 298271 37-672 55+ 24 514 9323 0-318615 27-051 50-06 536 5186 0- 253418 (24-764 24-54. 9326 0-145727 53-540 51-77 5213 0- 344656 34-902 43-06 9343 0-535658 44-187 10-83 5215 0-401926 46-118 39-89 539 540 541 542 543 544 545 546 547 Star 5157 5180 5185 5159 5174 5187 5131 5144 5161 5127 5146 5157 5102 5116 5128 5103 5118 5131 5021 5031 5043 5024 5035 5048 5005 5017 5021 5003 5025 5031 4981 4998 5017 4983 4991 Depend. - 229616 - 323050 -447334 - 188554 498050 - 313396 - 270952 -448468 - 280580 - 239462 -435317 325221 433552 294784 - 271663 -467979 - 275534 - 256487 -312396 249230 438374 -331543 - 348258 -320199 - 280592 351648 367761 460713 - 327900 - 211386 - 303537 - 360274 - 336189 - 323216 - 327206 PRECISE OBSERVATIONS OF MINOR PLANETS DURING 1961 AND 1962 105 TABLE II—continued Regie Dec. No. Star Depend. R.A. Dec 23-978 25-63 549 4981 0-317907 00-219 52-23 45-738 30-86 4998 0: 356568 20-182 09-29 15-359 10-67 5010 0: 325525 38-388 40-56 00-221 47-74 550 4976 0-310179 23-735 51-86 25-790 10-86 4991 0-386011 29-510 54-96 29-188 14-18 5017 0- 303810 24-749 04°47 45-765 21-71 551 4981 0: 322322 00-218 52-23 23-338 19-86 4990 0-377466 26-697 16-14 07-080 03-15 5003 0- 300212 44-584 29-84 26-621 24-71 552 4976 0- 400219 23-735 51-86 31-998 34-25 4991 0: 347420 29-510 54-96 23-978 25-63 5010 0: 252361 38-388 40-55 30-252 01-66 553 4971 0- 289462 51-394 36°15 40-502 07-63 4978 0+ 335220 31-827 42-81 35° 371 38-77 5010 0:375317 38-388 40-55 41-310 33°46 554 4977 0+ 241497 27-844 26-98 53-728 14-44 4982 0-451002 09-436 09-13 45-765 27°71 5009 0- 307500 29-357 07-23 18-953 26-60 555 4983 0-314534 10-088 44-63 52-526 24:61 4995 0-372591 09-771 21-13 03-511 00-94 5010 0- 312875 38-388 40-55 28-345 17-48 556 4976 0- 400890 23-735 51-86 39-596 39-63 4999 0- 300562 24-508 40-20 21-931 47-59 5017 0: 298548 24-749 04-47 29-630 24-41 557 5014 0-459098 06-589 59-36 24-749 04-47 5028 0- 236460 49-620 13-91 18-953 26-60 5041 0: 304442 54°301 55-95 44-585 29-84 558 5015 0- 361678 10-825 43°85 50-995 27-64 5026 0: 236827 29-436 07-50 52-526 24-61 5033 0-401495 38-154 37-09 00-218 52-23 559 5045 0: 218468 10-463 27-11 20-182 09-29 5022 0:454312 15-202 23-96 24-749 04-47 5039 0: 327220 25-935 51-42 10-089 44-63 560 5005 0+ 223500 49-594 14-47 29-510 54-96 5031 0-315382 41-937 19-46 04-889 00-32 5066 0:461118 37-749 33-00 5020 LOIS Os SO OO OO So OO SOO OOO OS SO SO OI OOS) Oo Sea Soe => -349578 (Received 27 September, 1963) | Journal and Proceedings, Royal Society of New South Wales, Vol. 97, pp. 107-115, 1964 Quaternary Sedimentation by Prior Streams on the Riverine Plain, South-west of Griffith, N.S.W. S, Pars Water Conservation and Irrigation Commission of New South Wales, Deniliquin, N.S.W. SuMMARY—The final phase of alluvial deposition by prior streams on the Riverine Plain south- west of Griffith, N.S.W., is described. Streams are classified according to depth and size of stream- bed sediments. The entire sequence is attributed to a gradually waning period of fluviatile deposition, featuring frequent stream diversion, which culminated in a period of relative aridity when aeolian sand deposition occurred. Radio carbon datings of wood samples from the youngest prior streams are recorded. Streambed sections are presented in diagrams demonstrating (i) width and depth relative to measured surface levels and (1°) probable mutual relationships of the streams. Introduction The area investigated comprises the Bene- -rembah Irrigation District and non-irrigated country between the Hay railway line and the Murrumbidgee River (see Fig. 1). The area consists of deep alluvial uncon- solidated sediments which are part of a broad alluvial fan sloping at 2 ft. to the mile in a westerly direction. The stream system responsible for this deposition is now non- functional and consists of prior streams. Micro- topographic variations occur on the alluvial plain in the form of relic streambeds, levees and floodplains. micro relief caused by gilgais. The latter display further This primary configuration has been altered by aeolian processes which account for the major relief in the area. Sand dunes up to 20 ft. in height and low sheet deposits were derived from the prior streams by deflation of streambeds and levees. Also mounds of residual levee soil occur as a result of this process of deflation on the prior levees. Topographic and other surface details of prior streams have previously been described -and mapped as 6 ‘well drained depressions ”’ by Smith et al. (1943), Smith (1945), Johnston | (1953) and Churchward and Flint (1956). Butler (1950) put forward the theory of deposition by prior streams on a regional basis, | while Langford-Smith (1958) has mapped prior | (Murrumbidgee) streams in more detail. Pels (1960) mapped prior streams in the southern | part of the Murrumbidgee Irrigation Areas and discussed the stratigraphy of local alluvial sediments. The aim of this investigation was to map the Stream system in detail and to determine whether individual stream characteristics could be used as a basis for their classification in terms of mutual relationships. This involved mapping of the streams on a base plan with the aid of aerial photographs, boring of transects across the streams to determine their lateral extent and depth in relation to measured surface levels ; the digging of pits in a search for carbon samples for age determinations and to observe stratification of streambed sediments on the pit faces and general observations on the geomorphology of the area. The Pattern of Prior Streams The prior stream system can be readily traced from aerial photographs although location in the field is often difficult. The stream relics form a distributory system of branching streams typical of an aggradational land form (see Fig. 1). Transects bored normal to _ their former direction of flow have revealed a variation in depth between the various streams. It appears that all had an initial period of down- cutting, as coarse stream deposits almost invariably lie in a channel incised into sediments of heavy texture which are delineated, in the vertical plane, by a well-defined break from heavy clay to coarse sand and gravel. The variation in depth of these coarse sediments from one stream to the other, together with the pattern of streams on the plain, suggests that frequent diversion took place. The stream system observable on the surface in this area can be subdivided into five classes, each class representing streams of characteristic depth of coarse streambed sediments. It is likely that further buried streams occur at greater depth. The origin of the five types of 108 S. PELS BENEREMBAH IRRIGATION DISTRIC CEOLOGCY ON pene Mies ry UPPER IAN 08 » QUARTZ/TES, CONDLOMEATES PLIOCENE (?, WN LEUCITE rr —_ PLEISTOCENE SX rasaita aeaToce ALLUVIUM PLEISTOCENE TO 26CENT SAMO DUNES Jou RIDGES TYPE & PRIOR STREAMS » LOCATION REFERENCE TQAN3SECT 1QRIGATION DISTRICT BOUNDARY FROM Hay QUATERNARY SEDIMENTATION SOUTH-WEST OF GRIFFITH, N.S.W. 109 ‘S Q ; a ~ 8 . ts N ie =~ eo : N 43 S ark : % 23 a y fe 1 = | “P' - 20 22 aa 2s rd so t2 ate = y . g . ‘ : > 2 a See eee N Q & ¥ wy WG ft Seem cae aa ae a eh lee ht aca SECTION 110 streams can all be traced as originating from one major prior stream (D-—D1, see Fig. 1). This prior stream and its westerly flowing extension has a channel depth where measured of 45 ft., it contains very coarse gravel and forms the primary (A-type) stream in this area, the others being secondary, tertiary, quaternary and quinternary. This terminology is confusing in a geological field and will be substituted by alphabetical notation. The B-type stream which developed by diversion from the A-type stream has a depth to the bottom of the incision of 32 ft. where measured. Subsequent diversion has created the C-type streams with a depth of 21 ft. while further diversion produced D- and E-type streams. with. ‘depths, of lt atacand sil’ it. respectively. The depths are considered to be a reflection of age. All these streams are identical in their mode of deposition but there is a general decline in size and vigour. The Streambed Sediments The decline of streams has resulted in a decrease of the size of gravels occurring in the streambeds from the A-type to the E-type streams. The deep gravels of Gum Creek (Section D-D1), which is an A-type stream, contain water-worn pebbles up to 2 ins. and the gravel size declines to coarse and fine sand together with some fine gravel in the E-type stream beds. Sand and gravel pits in the B- and C-type streams show that definite horizontal gravel bands occur within the streambed deposits and current bedding in the exposed faces suggests that heavy loads were carried by streams of high velocity. Diversion was brought about by aggradation of the older streams which caused the stream to break through the levee on to lower surface levels. Evidence of this process is abundant in the field and can be seen in Fig. 1. Although the age of origin of the streams are distinctly different, the streambed sediments of all streams have a common relationship to some degree. The diversion of an aggraded stream by the flow breaking through its levees (crevassing) on to lower levels brought about a downcutting action, by lowering the base level of the stream- bed, above the point of diversion. Evidence from deep gravel and sand pits located in the older streams supports this postulation as definite layering of gravel grading into sand Se oo) DRS) can be observed. From general observations — there appears to be a relationship between the depth of younger streams and the levels at which major textural changes occur in the gravel pits of the older streams. The textural changes are thought to represent the base levels of the younger streams. Such layering can be observed in Smith’s borrow pit (location 1) and in the borrow pit near Learmonth’s Well (location 2). Boring across the oldest stream (Gum Creek) also revealed gravel layers at levels which approximate the levels of the younger stream- beds. The newly developed section of the stream below the point of diversion and the incised section above that point became in time an ageraded stream. This process resulted in a complexity of streambed sediments. Downstream from the point of diversion, the older stream contains the original aggraded streambed sediments, while upstream the older streambed sediments were removed to the depth of the younger diverted stream and replaced with younger sediments. Under these conditions, the surface sediments of the streambeds could be of similar age irrespective of whether the channels are of major old streams or minor younger types. This point would also explain the widespread occurrence and general similarity of road- making loam in shallow pits adjacent to most roads over much of the Riverine Plain. Figure 3 shows the idealized relationship as is discussed above. Much time was spent on a search for carbon samples, but only two samples were detected which were considered reliable. One sample was obtained from Smith’s borrow pit in coarse sand and gravel of a C-type stream 15 feet below the surface (location 1). Another good sample of old wood was found in clayey sand of a D-type stream (location 7) previously described as a Mayrung stream by Butler (1958). This sample was obtained from the streambed at a depth of 5 ft. 6 ins. from the plain surface. Both samples were submitted to the Institute of Applied Science, Melbourne, for age deter- mination. Results are discussed under the , heading “ Stratigraphy ”’. The Levee Sediments The clear delineation of the prior streams in aerial observation is due to the presence of levees flanking the stream course. These levees are commonly eroded and have a “scalded ” appearance. The streambed proper has Lil QUATERNARY SEDIMENTATION SOUTH-WEST OF GRIFFITH, N.S.W. § “DIT op Op op . p Wy op op Op . q MAT SAINNG GNV SILNIWIGSS ar ie Lee safe) = ONIATASIAO SSLNSWIGSS WysalsS 40 a dIHSNOIIN1I3S = GSSIMWW3SGl ONIMONSG € ‘Oils oF, oF oP WW SINIWIGASS WW3IAIS AdAL-Oo S3NNG ONVS Fe G3ASISOdDIG3SA ANY ALISNI SINSWIG3S 33A357 a Pee ela eo ee een eee Se oe eee ee pee te Np ee ge ee et Do GUI * = aoe oo ANN pee ea oo ee Se ee ee See hee CR ey oe es eee ee ee ene ets _——— Oo ~~ 7RRX BARR) ESR DOOR LOR EN EMLLN eee eee — - Porritt ante! x NS \ SCOTS: SARKIS ESSN EERSORS ‘7 112 generally a good grass cover which further accentuates its outline. The levees are usually deflated but, where they are well developed, minor gullying also occurs, particularly on the steep side, closest to the stream course. Both these forms of erosion and subsequent deposition are considered to have been responsible for the occurrence of heavier textured layers which occur over the streambed sediments between the levees. The levee sediments consist of a red brown sandy clay containing some gravel and lime. Profile development at these locations has resulted in a clay enriched B-horizon which may _ occur from 6 ins. to 18 ins. below the surface. The scalded areas have been deflated and consist of the exposed B-horizon. Soil mounds of residual A-horizon occur and it appears that these are being gradually worn away during rainstorms and various stages of degradation can be observed. The dispersed materials spread out radially over the surrounding scalded area and are subsequently removed by deflation. Residual gravel, varying in size according to proximity to the streambed, is common on these scalded areas. Two other types of rock occur scattered over the eroded levees. These are so common that at first examination they appear to be part of the alluvial sediments. Quartzites and other rocks with conchoidal fracture are abundant on the scalded surfaces. These are in the form of sharp edged rock “chips” which are undoubtedly artifacts representing waste from aboriginal implement making. Another type of stone common on the scalded levees consists of a burnt clay which has a blackened red appearance. This stone is derived from old aboriginal fires and according to the stage of erosion is either scattered or occurs as preserved mounds of hard burned clay pro- truding from the scalded areas. Charcoal and bones are common in these old fires which appear to have been buried in the levee deposits prior to exposure by deflation. The large number of relic fireplaces on the levees flanking the prior streams and their absence in the streambeds suggest that although the system of prior streams may have been at least seasonally inactive at the time of habitation, surface water occurred possibly in the form of lagoons. The Overlying Sediments Streambed sediments of coarse texture may occur on the surface or may be buried by sediments of finer texture to considerable depth. S. PELS te oe ee i wa While it is generally true that the older and better delineated streambeds are often overlain by non-streambed sediments to a_ greater extent than the younger ones, there are many exceptions. This can be seen in Fig. 2, where a stream of the same age appears on the surface in one part and not in another. This may be due to the removal of sand by wind from certain sections of the stream only. It is possible that removal only took place in those parts where the direction of the stream and that of the prevailing winds coincided. This would account for the scattered occurrence of sand dunes and sand sheets found in close proximity to the streams and suggests that the aeolian sands were largely derived from the final stages of streambed deposition which is also strongly corroborated by the fact that prior stream courses are interrupted by sand dunes overlying the stream surface (location 4, Fig. 1). It can be seen that the stream course is obscured by the dune but emerges again on the downstream side. The absence of obvious diversion patterns suggests that these sand dunes were formed subsequent to the period of prior stream activity. Although the prior streams are generally situated in relatively elevated winding belts, the preserved stream channel is often a depressed line within this elevated belt. These depressions may support a grass cover in certain locations or a tree cover in others (linear box swamps). It is not clear why this difference in vegetation occurs. Many shallow linear depressions resemble indistinct prior streams on aerial photographs. Field investigations showed that these elongated depressions lack the characteristic coarse stream- bed sediments. They appear to be relics of former gullies, and it is usual to find traces of streambed sediments at the base of the former channel. The remainder of the channel is filled with heavier textured sediments to a depth of as much as 10 feet.. The latte sediments may be of aeolian origin or the result of slumping of the steep gully walls. Such slumping would produce the broad shape of shallow linear depressions. These postula- tions are supported by the general absence of levees along this type of depression, which suggests that an aggrading phase was not reached. Overlying heavier textured sediments were examined (section A) in an A-type stream and were found to be micaceous and non-calcareous throughout the depth of 12 ft. and are described as a micaceous sandy clay loam containing fine QUATERNARY SEDIMENTATION SOUTH-WEST OF GRIFFITH, N.S.W. gravel which grades into sand and gravel at greater depth. This gradation to finer sediments could be partly attributed to the waning stream activity, but the bulk of these materials is thought to have been derived from the adjacent levees by deflation, rilling, and minor gullying as described under the previous heading. Re-deposition of deflated materials from the levees was not restricted to the streambeds since clayey sheet deposits of medium texture are also found overlying the surfaces between the prior streams. The flood plain component of the entire Riverine Plain is relatively small in the eastern part of the plain and levee and for levee soils are predominant The area of floodplain, characterized by heavy gilgaied soils, becomes much more extensive further west. This phenomenon was also observed by Butler (1956), although the difference between the eastern and western zones was described in terms of deposition of aeolian sediments derived from a far western source with re- deposition restricted to the eastern zone of the Riverine Plain. Butler (1958) and van Dijk (1958) have described the aeolian sediments in some detail and it appears from a comparison of their analytical data of both aeolian and riverine clayey sediments that no exact differences can be established. In fact, van Dijk (1958) has shown that more coarse sand occurs in the typical wind-blown deposits (Widgelli-Tabbita phase, Bingar and Cocoparra) than in the riverine deposits (Barellan and MHanwood) interbedded with these aeolian sediments. The similarity of comparable riverine and aeolian sediments suggests a local fluviatile origin of the aeolian sediments of the plain and on the surrounding hills. Stratigraphy Deposition associated with the prior stream system discussed in this paper represents the final phase of a long period of fluviatile deposition. It has been established (Pels, 1960) that in the lower sequence below the sediments discussed in this paper, sand and gravel deposition has been more extensive and characteristic of deposition by braided streams. There have been a number of these periods of braided stream deposition which were interrupted by periods of deposition by meandering streams when predominantly clay deposition took place with coarse sediments restricted to definite stream channels. 113 It was suggested that the almost general deposition of sand by braided streams could have been related to the Pleistocene periods of glaciation and that the predominant deposition of clay represented deposition during the interglacial stages. The surface pattern of prior streams has similarities to the latter and it has been shown from evidence presented above that this final period of deposition was a period of continuous and gradually waning stream activity by streams which were fre- quently diverted. From the admittedly inadequate number of only two carbon datings it appears that although the prior stream pattern in this area is well preserved, it does not indicate a relatively youthful age. Radio carbon dating of carbon samples obtained from a C- and D-type stream (D- and E-type profiles) at locations 1 and 7 have revealed an age in excess of 36,000 years. The size of the second sample allowed it to be sub-sampled so that it was processed twice. Each sample was subjected to three 1,000 minute counts, and all results were in good agreement. The determined age represents the limits of the dating equipment, but it now appears that the final phase of stream deposition took place in the Pleistocene, and that, apart from the deposition along the Murrumbidgee River (see Fig. 1) no deposition has occurred during the Recent. The established age of the youngest prior streams of greater than 36,000 years suggests that a re-appraisal of the chronology of “ K- cycles ’’ of local soils may be in order. It has been stated that the depositional phases of the surface prior streams could be identified with the K, cycle (Butler, 1959). The K, cycle has been variously stated as representing a period from 3,000 to 7,000 years ago. These ages were largely based on radio carbon datings of layered soils in coastal areas of N.S.W. (Walker, M.Sc. thesis, University of Sydney) and a postulated correlation with inland layered soils. This is clearly not acceptable, and considering the relatively deep incision and limited lateral deposition of the final phases of the prior streams, large areas of the present ground surface must have originated well back into the Pleistocene. This would explain’ the difficulties experienced in attempts made to correlate “soils chronology ”’ with the existing knowledge of quaternary stratigraphy. Other findings presented in this paper are to some extent at variance with those of Butler (1958) and van Dijk (1958). Butler considers the period of deposition, associated with these prior streams, to have 114 been of three phases, namely, an older phase of stream deposition (Quiamong), a phase of aeolian deposition (Widgelli), and, superimposed on those, a younger phase of stream deposition termed the Mayrung. Stream deposition was said to be associated with a period of widespread aridity and the older stream deposition took place during the period leading into the arid period while younger streams were deposited during the period leading out of this period of aridity. As has already been stated, the data presented in this paper suggest that the surface prior streams (as shown in Fig. 1 and including both “ Mayrung”’ and “ Quiamong’”’ streams) were deposited during a period of continuous but gradually waning stream activity by streams which were frequently diverted. The strati- graphical position of the sand dunes also suggests that the climate changed gradually and culminated in a period of relative aridity when sand dunes were formed overlying the prior stream courses in some locations (see Fig. 1). Practical Applications The data obtained are of practical value in the developmental stage the Riverine _ plains generally are in at this time. It has been shown that roadmaking materials are distributed generally and locations of better drained soils are delineated. Irrigation is likely to be initially confined to the areas of greatest prior stream activity, i.e., to the eastern zone of the Riverine Plain, as soils associated with the more vigorous parts of the prior streams are superior for irrigation purposes. This is mainly due to the preponderance of better developed levees over floodplain soils and the greater redistribution of levee soils by deflation. The influence of the streams on groundwater movement and drainage is of particular interest. In parts of the already developed Irrigation Areas the pattern of sedimentation was similar but the surface evidence, so obvious from aerial observation in the less developed areas, has been obscured here by cultivation. Ground- water movement in the Murrumbidgee Irrigation Areas is very difficult to interpret, and it is in terms of quaternary stratigraphy (of prior streams) that many anomalies in the existing Irrigation Areas may be explained. The laterally extensive deep sand _ beds, which were deposited by braided streams, contain water under pressure. Under natural S:ePELS conditions the phreatic surface closely approxi-— mates the piezometric levels in these aquifers. It has been found that the shallower sands are separate channel type sand deposits character- istic of meandering streams and that frequent diversion has caused the deposition of sand- filled channels lying at different levels. Disturbance of the natural equilibrium of the groundwater system by irrigation may cause the piezometric level and phreatic surface to rise, and when this level coincides with channel deposits at higher levels the pattern of ground- water movement would be influenced by move- ment in the coarse streambed sediments. Water superimposed on the present ground- water system by irrigation could initially tend to create perched watertables which would display groundwater movement patterns governed by the pattern of prior streams. Such a system would be extremely difficult to interpret unless the sedimentary pattern of prior streams is known. A further factor which may be of practical application is the intake of surface water into subsurface prior streams. This occurs at location 5 (Fig. 1) and is also likely to occur at location 6. It can be seen that in the vicinity of location 5 the Mirrool Creek is superimposed on a prior stream and old levees occur on both sides of the Creek. Piezometer readings taken in the prior stream north of there (see Fig. 1) show that this buried stream is fully charged. The prior stream portion south of location 5 is known to be dry, as sandpits are located in it. Similar stream flow losses occur in the vicinity of Willow Dam (location 6) to buried streams running west into the Wah Wah Irrigation District. Acknowledgements The manuscript was read for comment by Messrs. H. N. England and S. E. Flint, Water Conservation and Irrigation Commission, and by.Mr. T. Talsma and Dr. J. Loveday, C.S.I.R.O. The assistance of Mr. S. J. Jones, Assistant Field Officer, Water Conservation and Irrigation Commission, is also gratefully acknowledged. Radio carbon datings were carried out by the Institute of Applied Science, Melbourne. References BuTLer, B. E., 1950. A theory of prior streams as a causal factor in the distribution of soils in the Riverine Plain of south-eastern Australia. Avwst. i ATIC eS, ak ButTLer, B. E., 1956. J. Sci., 18. Parna, an aeolian clay. Aust. ee QUATERNARY SEDIMENTATION SOUTH-WEST OF GRIFFITH, N.S.W. Butter, B. E., 1958. Riverine Plain in relation to soils. No. 10, C.S.I.R.O. Aust. But Ler, B. E., 1959. Periodic phenomena in land- scapes as a basis for soil studies. Soil Publication No. 14, C.S.I.R.O. Aust. CHURCHWARD, H. M., AND FLINT, S. E., 1956. Jenargo extension of the Berriquin Irrigation District, N.S.W. Soils and Land Use Series No. 18, C.S.I.R.O. Aust. Dijk, D. C. vAN, 1958. Principles of soils distribution in the Griffith-Yenda Area, N.S.W. Soil Publica- tion No. 11, C.S.I.R.O. Aust. Jounston, R. J., 1953. Pedology of Deniboota Irrigation District, N.S.W. Soil Publication No. 1, C.S.I.R.O. Aust. Depositional systems of the Soil publication 115 LANGFORD-SMITH, T., 1958. Land forms, land settle- ment and irrigation on the Murrumbidgee, N.S.W. Thesis A.N.U., Canberra. LANGFORD-SMITH, T., 1960. The dead river systems of the Murrumbidgee. Geogr. Rev., 50 (38). Pets, S., 1960. The Geology of the Murrumbidgee Irrigation Areas and Surrounding Districts. Groundwater and Drainage Series Bull., No. 5, Water Conservation and Irrigation Commission, NESW. SMITH, R., 1945. Soils of the Berriquin Irrigation District, N.S.W. Bull. No. 189, C.S.I.R. Aust. SMITH, R., HERRIOT, R. I., AND JOHNSTON, E. J., 1943. Soil and land use survey of the Wakool Irrigation District, N.S.W. Bull. No. 162, C.S.I.R. Aust. ry Journal and Proceedings, Royal Society of New South Wales, Vol. 97, pp. 117-119, 1964 Some Applications of Aerial Photographs to the Solution of Topographic and Cartographic Problems A. D. ALBANI School of Applied Geology, University of New South Wales, Kensington ABSTRACT—A procedure for the exact location on a topographic map of details identified on aerial photographs is presented. The determination is based on the location on the topographic map of the nadiral point of the aerial photographs by a graphico-numerical solution to the Snellius problem of inverse intersection. From the nadiral points on the topographic map, detailed features may be located by a method of direct intersection. Introduction During recent years, aerial photographs have assumed an ever increasing importance in many researches where they are used in conjunction with topographic maps. However, the exact location on the map of details (morphological, geological, archaeological, etc.) identified on the aerial photographs has often proved difficult without the use of the _ stereo-plotting instruments. This paper presents a simple procedure for the exact location of such details on the maps without the aid of mechanical plotters, in the case of vertical aerial photographs. Discussion The following terms of photogrammetry are used in the discussion. The principal point, N, of the photogram. This is the point where the optic axis of the camera meets the photographic plate. It is determined by the intersection of _ the straight lines joining the collimation marks of the photogram. The nadiral point, N’, of the map or ground. This is the point of intersection of the vertical from the centre of the camera’s objective with the ground surface. In the case of vertical aerial photographs the centre of the camera’s objective and the principal and nadiral points are colinear and the nadiral point becomes the projection of the principal point on the ground. It is therefore an important feature of vertical photographs that identifiable features subtend equal angles at both the principal and nadiral points of the photogram and map respectively. Further, if the nadiral points can be precisely determined on the topographic map, then the exact location of details from the photograms to the map can be achieved by a method of direct intersection BB using bearings taken at the principal points of two or more photograms. The precise determination of the nadiral point may be obtained with a construction which yields a graphical solution to the Snellius problem of inverse intersection by using the auxiliary points of Collins. Construction The construction requires for each photogram a minimum of three reference points which are identifiable features accurately located on the map. In Figure 1, A, B and C are the three points identified and located on the photogram (Fig. 1, a) and on the map (Fig. 1, b). At the principal point N of the photogram the reference points A and B subtend the angle « and the points B and C, the angle @. The auxiliary point of Collins is obtained by constructing a line through A at the angle 6 with respect to AB, and a line through B at the angle («-+() with respect to BA as shown in Figure 1, 6. The intersecting point E, of the constructed lines, is the auxiliary point of Collins. Since AB subtends an angle « at both E and N’, the nadiral point N’ falls on the circum- ference of the circle through A, Band E. Hence, BE which subtends the angle 6 at A also subtends the angle 6 at N’, and the points N’, E and C are colinear. The second auxiliary point of Collins, F, which is obtained by a similar construction about the line BC, is colinear with N’ and A. The nadiral point N’ is therefore determined by the intersection of the lines EC and FA. Although only three points of reference are necessary for the construction, it is preferable to use four points as illustrated in Figure 2. Has A DT ALBANT AERIAL PHOTOGRAPHS IN TOPOGRAPHIC AND CARTOGRAPHIC PROBLEMS 119 hiG. = In this figure, only the points E of the above construction have been used. The use of four points improves both the reli- ability of the determined position of the nadiral point and provides a better distribution of ref- erence points. Location and Details on the Map The exact location of details from the photograms to the map is illustrated in Figure 3. An important detail X, occurring on the two photograms (no. 56 and 57) in Figure 3, a, subtends angles of 0 and y at their principal points with the directions of the reference points C;, and Ds, as shown. The angles @ and y from the respective reference points are then constructed at the corresponding nadiral points on the map as shown in Figure 3, 6. The position of the detail X on the map is defined by the direct intersection of the constructed lines. C(57) N57) 9 r¢ N56) e B56) 5 Conclusion All details of interest occurring on two or moie photograms may be located in this manner. Also, since the determination is independent of the scale of the map used, it can be applied even to the case of enlargements of the aerial photographs. Acknowledgement The writer is greatly indebted to Mr. L. V. Hawkins, School of Applied Geology, University of New South Wales, for helpful discussion of the present paper. References ALBANI, F., 1957. Boll. Soc. Ital. Fotogrammetria e Topografia, no. 2, 3, pp. 86-93, Rome. CASSINIS, G., AND SOLAINI, L., 1946. Note di Foto- grammetria, Milan. LEuDER, D. R., 1959. pretation, New York. Low, J. W., 1952. Plane Table Mapping, New York. Aerial Photographic Inter- (Received 6 December, 1962) 2 oe ae > ce ae : Pig PY ‘ ‘ ‘ ii ' ue Ms ry ha , 5 ty ; ; : 25% ; : a) . 9 ‘ Di ie 6 j , ¥ i) a) 7 oT . : a é " : : 4 g srt 2 ; . : ES ; . ( ee i : } ae we , a Ey cs e yi » 4 & , f . P. i aD . ; as ae 2 t x ' wenn = aS. q ‘i v a Z i ah a #e.5 FN oe _ Annual Reports Report of the Council for the year ended 31st March, 1963 At the end of the period under review the composition of the membership was 353 members, 19 associate members and 9 honorary members; 15 new members were elected. Six members and associate members had resigned and the name of one associate member was removed from the list in accordance with Rule XVIII. It is with regret that we announce the loss by death of Dr. Adolph Bolliger (elected 1933), Mr. Anthony Dadour (elected 1940), Prof. Francis P. J. Dwyer (elected 1934), Mr. Frank Leechman (elected 1957), Mr. Burnett Mander-Jones (elected 1960). Nine monthly meetings were held. The abstracts of all addresses have been printed on the notice papers. The proceedings of these meetings appear later in this issue of the ‘“ Journal and Proceedings’’. The members of the Council wish to express their sincere thanks and appreciation to the seven speakers who contributed to the success of these meetings and also to the members who read papers at the November meeting. The Annual Social Function was held on 28th March at the Sydney University Staff Club and was attended by 54 members and their guests. The Council has approved the following awards : The Clarke Medal for 1963 to Dr. Germaine A. Joplin, Geophysics Department, the Australian National University. The Society’s Medal for 1962 to Mr. Harley Wood, Government Astronomer, Sydney Observatory. The Walter Burfitt Prize for 1962 to Dr. M. F. Glaessner, F.A.A., Geology Department, the University of Adelaide. ‘The Edgeworth David Medal for 1962 to Mr. R. F. Isbell, of C.S.I.R.O., Division of Soils, Brisbane. The Liversidge Research Lecture for 1962 entitled “Nucleic Acids: Their Structure and Function ”’ was delivered by Prof. D. O. Jordan, of the Department of Physical and Inorganic Chemistry, the University of Adelaide. The lecture has been published in the “ Journal and Proceedings ’’, v. 96, p. 39. The Pollock Memorial Lecture for 1962, given under the joint auspices of the Royal Society of New South Wales and the University of Sydney, entitled ‘‘ Life on Other Planets’, was delivered by Professor F. Hoyle, F.R.S., Plumian Professor of Astronomy, Cambridge University. The Society has again received from the Government of New South Wales a grant of £750. The Government’s interest in the work of the Society is much appreciated. The Society’s financial statement shows a deficit of £117 Qs. 4d. The New England Branch of the Society progressed Satisfactorily during the year. Four meetings at which invited speakers were present were held. Vigorous progress has been handicapped by the decrease in the numbers of distinguished visitors to the University of New England. Unfortunately, funds available are not yet sufficient to pay the expenses of visitors from great distances from Armidale. The President represented the Society at the Commemoration of the Landing of Captain Cook at Kurnell and also attended the Annual Meeting of the Board of Visitors of the Sydney Observatory. On 27th July, the President and the Hon. Secretary waited on His Excellency the Governor of New South Wales. The Society’s representatives on Science House Management Committee were Mr. Donegan and Mr. Adamson. One part of the “ Journal and Proceedings ’’ has been published during the year, Volume 96, Part I, in which appeared three papers. The Section of Geology held five meetings and abstracts of the proceedings will be published later. Council held eleven ordinary meetings and attendance was as follows: A/Prof. W. B. Smith-White 10; Mr. H. A. J. Donegan 7; Mr. A. F. A. Harper 7; Prof. R. J. W. Le Fevre 5; Mr. W. H. G. Poggendorff 3 ; Mr J. L. Gritith 11; Dr. A. A. Day 8; Mr. °C. Wh. Adamson 7; Dr. Ida A. Browne 9; Father A. G. Fynn 10; Dr. N. A. Gibson 6; Mr. H. G. Golding 8; Mr. J. W. Humphries 9; Dr. A. H. Low 5 (absent on leave 6); Mr. H. H. G. McKern 11; Dr. P. D. F. Murray 0; Mr. G. H. Slade 4; Dr. A. Ungar 7. The Libvavy—Periodicals were received by exchange from 398 societies and institutions. In addition the amount of £132 13s. was expended on the purchase of 12 periodicals. The reorganization of the library is almost complete. This has been achieved by the most strenuous efforts of the Assistant Librarian. Among the institutions which made use of the library through the inter-library loan scheme were : N.S.W. Govt. Depts.—Department of Agriculture, Botanic Gardens, Forestry Commission, Main Roads Board, Department of Mines, M.S.W. & D. Board, Department of Public Health, Soil Conservation Service, Sydney County Council, W.C. & I. Commission, Wood Technology Division. Commonwealth Govt. Depts.—C.S.1.R.O., Head Office, Melbourne; Library, Canberra; Division of Animal Physiology, Prospect; Cunningham Laboratory, Brisbane; Division of Food Preservation, Ryde; Division of Irrigation Research, Griffith ; McMaster Laboratory, Sydney ; National Standards Laboratory, Sydney, Division of Oceanography, Cronulla; Division of Textile Physics, Ryde; Division of Tribophysics, Melbourne; Wool Research Laboratory, Geelong ; Australian Atomic Energy Commission; Bureau of Mineral Resources ; Snowy Mountains Hydro Electric Authority. Universities and Colleges —Sydney Technical College, Newcastle University College, University of Adelaide, 122 Australian National University, Mount Stromlo Observatory, University of Sydney, University of New England, University of New South Wales, University of Queensland, University of Tasmania, University of Western Australia. Compantes—A.C.I., A.W.A. Ltd., A.I. & S. Pty. Ltd., B.H.P. ‘Co. Ltd., C:S:R. Co: Ltd., Ducon Condensors, Electrolytic Zinc Co., I.C.I. Ltd., Johnson & Johnson, J. Lysaght Ltd:, Unilever Ltd., Union Carbide Ltd., Wheat Industries Ltd., W. D. & H. O. Wills Ltd. Research Institutes—Bread Research Institute, M.B.T. Research. Laboratories. Museums and Miscellaneous—The Australian Museum, National Museum of Victoria, South Australian Institute of Technology, Edgeworth David Memorial Library, Cessnock ; Institution of Engineers, Australia ; Institution of Radio Engineers. J; L.oGRIEFITH; A. A. Day, Honorary Secretaries. The Honorary Treasurer’s Report Mr. Chairman, Ladies and Gentlemen, Please accept my apology for absence from the meeting, which is due to geological fieldwork. From inspection of the Income and Expenditure Account. it will) be seen that there is a deficit of £117 9s. 4d. compared with a deficit of £196 last year. However, there is one important feature of this year’s accounts which makes direct comparison misleading. This feature is the cost of printing the “ Journal and ANNUAL REPORTS Proceedings’. Owing to the fact that this year’s accounts include printing of only three parts of the “Journal and Proceedings ’’, as opposed to the usual six parts, a provision of £1,000 has been included in the Expenditure Account to cover printing costs of the remainder of Volume 96. Thus while the previous year’s accounts dealt with actual expenditure on printing this year’s accounts provide for an estimated cost of part of the printing. This situation will be reflected in the finances for the coming year when final adjustments will be made. Compared with last year, there was a marked drop in revenue from reprints and back numbers of the “Journal and Proceedings’’. This was _ counter- balanced by sale of unwanted periodicals from the Society’s library. This income can be regarded as connected with the “ Journal and Proceedings ’”’ as the material disposed of has been acquired by exchange. I regret to state that while there has been a slight increase in income from Membership Subscriptions there has been a slight fall in our share of the income from Science House. The most welcome subsidy from the State Government remained constant at £750. Thus the income from our regular sources has remained almost static, while there have been slight rises in our regular items of expenditure such as salaries, postages, general printing, library purchases and miscellaneous expenditure. In conclusion I would thank our Assistant Secretary, Miss Ogle, for the efficient way in which financial routine has been carried out. C. L. ADAMSON, Honorary Tveasurer. 1962 33 104 1,019 609 15 | £31,869 ANNUALS REPORTS Financial Statement BALANCE SHEET AS AT 28th FEBRUARY, 1963 LIABILITIES Accrued Expenses Subscriptions Paid in Advance Life Members’ Subscriptions — Amount “carried forward Trust and Monograph Capital Funds (detailed below)— Clarke Memorial Walter Burfitt Prize Liversidge Bequest : Monograph Capital Fund | Ollé Bequest : Accumulated Funds Employees’ Long Service Leave Fr und Provision Contingent Liability (in connection with Per- petual Lease). ASSETS Cash at Bank and in Hand . Investments— Commonwealth Bonds and Inscribed Stock— At Face Value—held for: Clarke Memorial Fund : Walter Burfitt Prize Fund.. Liversidge Bequest .. Monograph Capital Fund General Purposes Fixed Deposit—Long Service Leave Fund Debtors for Subscriptions. : ; Less Reserve for Bad Debts Science House—One-third Capital Cost Library—At Valuation sea Furniture and Office Equipment—At Cost, less Depreciation Ss, Pictures—At Cost, Jess Depreciation Lantern—At Cost, Jess Depreciation £ Sepa: £ 1,000 25 96 2,014 0 8 1,195 14 11 683 9 9 4,685 9 4 181 12 7 8,760 22,839 159 £32,881 1,986 1,800 0 O 1,000 0 O 700 0 O 3,000 0 O 1,960 0 0O 8,460 159 99 4 6 99 4 6 14,835 6,800 625 13 1 £32,881 bo GO OSes 18 10 5 10 S) oo oo © or SO & So 18 10 a) L 24 ANNUAL REPORTS TRUST AND MONOGRAPH CAPITAL FUNDS Walter Monograph Clarke Burfitt Liversidge Capital Ollé Memorial Prize Bequest Fund Bequest £ sod Ss Sd sin Nsaaa: £ Syd. | Byes ae apital at 28th February, 1963 an an .. 1,800 0 0 1,000 0 0700 0 O 3,000 0 0O — Revenue— Balance at 28th February, 1962 .. : ie DA 94 170 8 7 36 4 5 1,562.6 1)) 4369 47731 Income for twelve monthe 12, 4 0 40° 3270 28 2 123° 2° a WA ees ee. en 210 10 7 64 5 7 41,685 S°4)20i 12 Less Expenditure By 0 > “6 1415 8 8015 10 — 30 0 O Balance at 28th eee 1963 .. A BEZTAS EO (oo) £195 14 11 £16 10 3 £1,685 9 4 £181 12 7 ACCUMULATED FUNDS SS. ele £ Sana: Balance at 28th February, 1962 .. ; 23,021 14° 3 Add Transfer from Subscriptions Received — 2 1940 £23,031 3 3 Less— Increase in Reserve for Bad Debts .. 46 8 6 Transfer for Long Service Leave Fund Provision : v2 20, 00 Transfer from Subscriptions Received. 3, oN 0 Deficit for Twelve Months she ee Bis FOL 192 0 10 £22,839 2 5 Auditors’ Report The above Balance Sheet has been prepared from the Books of Account, Accounts and Vouchers of the Royal Society of New South Wales, and is a correct statement of the position of the Society’s affairs on 28th February, 1963, as disclosed thereby. We have satisfied ourselves that the Society’s Commonwealth Bonds and Inscribed Stock are properly held and registered. HORLEY & HORLEY, Chartered Accountants, Prudential Building, Registered under the Public Accountants 39 Martin Place, Sydney, Registration Act 1945, as amended. 22nd March, 1963. (Sgd.) C. L. ADAMSON, Honorary Treasurer. 697 197 992 9 1,402 42 £4,082 1962 935 7 750 2,088 106 196 £4,082 ANNUAL REPORTS INCOME AND EXPENDITURE ACCOUNT Ist MARCH, 1962, to 28th FEBRUARY, 1963 Advertising Annual Social . MUGEL |... Branches of the Society Cleaning me Depreciation Electricity : Entertainment Insurance : Library Purchases Miscellaneous Postages and Telegrams Printing— J ournal— Vol. 95, Parts 5-6 Binding .. at Mol:* 96, Part 1 . Reprints be Postages Provision for Vol. 96, Parts 2-6 Less— Sale of Reprints ‘ Subscriptions (to Journal) — Back Numbers Refund Postages Printing—General ; Rent—Science House Management. Repairs oe <% Salaries Telephone Membership Subscriptions Proportion of Life Members’ Subscriptions Government Subsidy 10 15 Science House Management—Share | of Surplus q Interest on General Investments Sale of Periodicals ex the as Donation ' Deficit for iwieleye mouchs SOWawa a ee) 1,906 12 671 16 9 8 1,234 216 984 5 1,438 37 Qu PAWAOAaNOGTOAN. £4,677 wn — (Jt) SNonrOoNSC:; aN) Weenie ean er) ROUDMNOCOaF i) Obituary Adolph Bolliger, Ph.D. (Basle), D.Sc. (Sydney), was born in Schmiedrued (Zurich), Switzerland, on 8th October, 1897. His father was a master baker. He qualified to enter the University of Zurich in the autumn of 1916 but was delayed by military service until the following summer. In 1918 he studied at the University of Geneva, saw more military service, and had a brief encounter with Lenin, then a political refugee in Zurich. In 1919, after a short period at Zurich, he entered the University of Basle and obtained his Doctorate of Philosophy (Magna cum Laude) in 1921. For the following two years he worked in the chemical dye and textile industry in Germany. In 1923 he emigrated to the United States which had long attracted Swiss citizens and where relatives were already established. His first work was in a factory but after a short time he obtained a position as a biochemist, specializing in cardiovascular disease in the Henry Ford Hospital, Detroit. In 1926, with two other colleagues, he was awarded the silver and gold medals of the American Medical Association for the best research work presented. In 1928 Bolliger met the eminent Australian surgeon Gordon Craig, who invited him to take up a post in Sydney in the laboratories of the Royal Prince Alfred Hospital. In 1930 he was appointed Director of the Gordon Craig Research Laboratories in the Department of Surgery of Sydney University. In 1935 he became a naturalized Australian citizen and, in 1936, was awarded the Rennie Memorial Medal by the Australian Chemical Institute. Within the University of Sydney he was, in 1938, given the status of Lecturer, in 1949 of Senior Lecturer, and in 1955 of Reader. In 1957, on the presentation of his published works on chemical] studies of integuments of vertebrates and observation on marsupials, he was awarded the degree of Doctor of Science. In 1933 he was elected to membership of the Royal Society of New South Wales, served for a number of years on its Council, was President in 1945-6, and in 1962 was awarded the Society’s Medal (see Journal, v. 96, p. 171). In 1947 he was President of Section N of A.N.Z.A.A.S. at its Perth meeting. In that year also he was awarded the Henry G. Smith Medal. Adolph Bolliger’s published work covers a wide field and includes studies in analytical and organic chemistry, biochemistry, anatomy, physiology and experimental pathology. More recently he became interested in the micro-analysis of marsupial’s milk. He had perfected a method of removing the tiny marsupial foetus from the maternal teat, extracting a drop of milk and then reapplying the foetus in such a way that further survival was possible. This study provoked considerable overseas interest, and it was suspected that it may well have a significant application to the management of human pre-maturity. Bolliger’s genial, generous personality invited friend- ship and those who found his hearty manner a trifle overwhelming and held aloof were the losers. He had a full and happy personal life. His main recreation was skung. In 1937 he married Dorothy Dark, and after her death, Jocelyn Elliot, wth both of whom he had been associated in research in the University. By his death on 22nd October, 1962, Australia lost a notable adopted son who had contributed sub- stantially to Australian science. He leaves five sons, of whom four are in Australia and one is an architect in Switzerland. Anthony Dadour was elected to membership in 1940. He received the degree of Bachelor of Science from the University of Sydney in 1940 and was engaged in the chemical industry. He died suddenly on 18th August, 1962. Francis Patrick Joseph Dwyer, D.Sc. (Sydney), Professor of Biological Inorganic Chemistry in the John Curtin School of Medical Research of the Australian National University, died suddenly on 22nd June, 1962, at his home in Canberra. He was born in 1911 at Nelson Plains, New South Wales, and was educated at the Marist Brothers’ College, Maitland, and the University of Sydney, whence he graduated in 1932. He was recognized as a world authority in the field of inorganic chemistry, his recent work being concerned with the synthesis of metal-containing drugs and their uses in biology and medicine. His research in recent years led to the discovery of a potentially useful biologically active compound which has shown promise in the prevention and cure of a number of local infections. Dwyer’s versatility, and the breadth of his interests, are shown by more than 150 publications (62 in the Society’s Journal) spread over the following topics : the chemistry of platinum, palladium, rhodium, iridium, ruthenium and osmium, isomerism of the triazines and diazoamino compounds and their metal derivatives, the redox potentials of simple compounds and complexes of the platinum series of metals, the optical activity and kinetics of substitution and racemization of Group 8 metal complexes, the diastereo- isomeric effect and the principle of configurational activity, the stereochemistry of multidentate chelates, stereospecific influences in octahedral complexes, electron transfer reactions, the effects of metal complexes in biological systems, and X-ray analysis and micro-analytical reagents and procedures. For his work on diazoamino compounds their metallic hydroxide lakes and metallic salts he was awarded the degree of Doctor of Science of the University of Sydney, the Rennie Medal of the Royal Australian Chemical Institute (1940), and the H. G. Smith Medal in 1945. In 1953 the University of Melbourne awarded him the David Syme Medal and Prize for distinguished work in natural science. From 1934 until 1945 Frank Dwyer was senior lecturer and head of the Department of Inorganic Chemistry in the Sydney Technical College. In 1946 he was appointed senior lecturer in Inorganic Chemistry OBIPUAK Y in the University of Sydney, was visiting professor at Northwestern University during 1953-54. In 1956 he was appointed to a new chair in inorganic chemistry in Pennsylvania State University but resigned in 1957 without taking up the post to become reader and head of the Biological Inorganic Chemistry Unit in the John Curtin School of Medical Research of the Australian National University. In 1960, on account of his outstanding contribution to inorganic chemistry, he was elected to one of the first personal professorships created in the Australian National University. He was elected a Fellow of the Australian Academy of Science in 1961. Shortly before he died he had given a series of lectures at the invitation of the American Chemical Society. He was elected to membership of the Royal Society of New South Wales in 1934 and served on the Council for a period in the 1940's. Dwyer is remembered by many for his outstanding ability, personal charm, friendliness and modesty. Generations of former students will also remember his sense of humour, unfailing cheerfulness and enthusiasm. Professor Dwyer is survived by his widow, two sons and a daughter. George Francis (Frank) Leechman was born in England in 1898, received his education at Dunstable Grammar School and was apprenticed in the Merchant Navy in 1915. He saw considerable sea service during World War I, obtained his Master Mariner’s Certificate in 1923 and settled ashore in Singapore, with his wife, in 1923. After his wife’s death in 1931 he returned to England with his infant son and settled in Cornwall, where he became interested in gemstones and was the owner of a prosperous business. It was at this time that his interest in opals began. During the second war Captain Leechman worked on diamond polishing for the British Government but after the war his keen interest in opals led him to come to Australia to further his knowledge of these stones; the result was his book, “ The Opal Book ’’, which is recognized as a standard work on the subject of opals. During the last few years Captain Leechman had suffered ill health; and after the tragic death of his only son with wife and child in a motor accident near Glen Innes in 1960 he never really recovered. The last year of his life was devoted to the production of a handbook for amateur gemmologists designed to teach them the art of grinding and polishing gemstones. He was elected to membership of the Royal Society of New South Wales in 1957. He died on 9th February, 1963. Burnett Mander-Jones, B.Sc. (Hons.), M.Sc. (Sydney), Dip.Chem.Eng. (Lond.), A.R.A.C.I., member of the Royal Society of N.S.W. and Deputy Chief Analyst of the Mines Department of N.S.W., passed away on 12th July, 1962, at the age of 58 years. He attended Sydney Church of England Grammar School (‘‘ Shore ’’) and Sydney University. After serving as chemist in the Kandos Cement Works, N.S.W., and the Defence Department Laboratories at Maribyrnong, Victoria, he joined the Chemical Laboratory of the N.S.W. Mines Department in 1929, becoming second-in-charge in 1956. He was a keen civilian soldier and had progressed from Gunner to Major in the Anti-Aircraft Artillery at the outbreak of the 1939-45 war, when he immedi- ately enlisted for active service, was promoted to Lieutenant-Colonel, seeing the whole six years’ war service. At the end of the war he proceeded to England (under Commonwealth Grant) and obtained the Diploma in Chemical Engineering of London University. He was an original member of the old Scientific Officers’ Sub-Section, and later Councillor of the Professional Section of the Public Service Association of New South Wales for many years until his death. He was elected to membership of the Royal Society of New South Wales in 1960 and had one paper published in the Society’s Journal. He came of a well-known, respected and talented family. His father was a doctor; both his brothers were Lieutenant-Colonels, one won the Sword of Honour at Duntroon and served on the N.W. frontier of India before the war, the other, who was on General Blamey’s (C.1.C.) staff, is now Director of Education in South Australia; his sister, Miss P. Mander-Jones, was Mitchell Librarian before her retirement. He rowed in his college eight at the University, played vigorous hockey in the early ‘thirties, and was interested in fencing and pistol shooting. A. kindly, sincere, courteous and generous gentleman, but a stickler for the rights of his fellows ; our sincere sympathy is extended to his wife, his brothers and his sisters. Members of the Society Elected During 1962 BADHAM, Charles David, M.B., B.S., D-.R. (Syd.), M.C.R.A., 16 Ormonde Parade, Hurstville. BAKER, William Ernest, B.Sc. (Hons.), Geologist, 394 Kaolin Street, Broken Hill, N.S.W. BRENNAN, Edward, B.E. (App. Geology), 94 Parbury Road, Swansea, N.S.W. DANCE, Ian Gordon, B.Sc. (Hons.), Analytical Chemist, 22 The Promenade, Cheltenham. DRAKE, Rev. Lawrence Arthur, B.A. (Hons.), B.Sc., Canisius College, 102 Mona Vale Road, Pymble. FINDLER, Nicholas Victor, B.E. (Hons:)) Ph.D.:, Applied Mathematician, c/o C.S.R. Co. Ltd., O’Connell Street, Sydney. FISHER, Stephen, M.D., B.Sc., Director of Clinical Pathology, Kanematsu Memorial Institute, Sydney Hospital. GORDIJEW, Gurij, Institute Hydro Meteorology in Moscow, Faculty of Hydrology, Graduated Engineer Hydrogeology (1936), 41 Abbotsford Road, Homebush. LEWIS, Philip Ronald, J.P., Design Engineer, 13 River View Road, Woolooware. MACKAY, Robin Marie, B.Sc., Department of Geology and Geophysics, The University of Sydney, Sydney. NEWMAN, Thomas Montagu, Hotel Acton, Canberra, AVC. READ, Harold Walter, B.Sc., 1 Karog Street, Black- smiths, 2N, N.S.W. SMITH, Glennie Forbes, B.Sc., Geologist, c/o Mine Department, Mt. Lyell Mining and Railway Co. Ltd., Queenstown, Tasmania. THWAITE-E. G., B.Sc., 8 Allars Street) Wese teycie: YATES, Harold, M.Sc. (Syd.), .102 Eyre) Street; Ballarat, Victoria. Medals, Memorial Lectureships and Prizes Clarke Medal 1963 Germaine Anne Joplin, B.A., D.Sc. (Syd.), Ph.D. (Cantab.) The Society’s Medal 1962 Harley Wood, M.Sc. (Syd.) Walter Burfitt Prize 1962 Martin Fritz Glaessner, Ph.D., Dr.Jur. (Vienna), D.Sc. (Melb.) Edgeworth David Medal 1962 Raymond Frederick Isbell, M.Sc. (Qld.) Recipients of Society Awards, 1963 Germaine Anne Joplin, Senior Fellow in the Depart- ment of Geophysics, Australian National Uni- versity—the Clarke Medal. The Clarke Medal for 1962 is awarded to Dr. Germaine A. Joplin, B.A., Ph.D., D.Sc., for her distinguished contributions to Geology, particularly in the field of igneous and metamorphic petrology. She graduated in Science at the University of Sydney in 1930, and has devoted most of her time since then to geological research. She was a Macleay Fellow in Geology of the Linnean Society of N.S.W. from 1941 to 1944, and has carried out research at the University of Sydney, the University of Cambridge, the Bureau of Mineral Resources at Canberra, and more recently at the Australian National University. Her geological interests have taken her to Great Britain, Europe, Canada and U.S.A. She holds the degrees of Ph.D. (Cantab.) and D.Sc. (Syd.). Dr. Joplin lectured at the University of Sydney from 1936 to 1940, and from 1945 to 1949. Both at Sydney and as Research Fellow at A.N.U., where she has supervised the work of graduate students in petrology, she has always been most generous in her assistance and encouragement to younger geologists. Her published work consists of about 40 papers, mainly dealing with the geology and petrology of special areas of eastern Australia, which form the basis of notable contributions to petrological thought, particularly in regard to magmatic differentiation, granitization and metamorphism. Dr. Joplin’s compilation of all known chemical analyses of Australian rocks is being published by the Bureau of Mineral Resources, and at present she is writing a Textbook of Petrology, based on her wide knowledge of Australian rocks. Harley W. Wood, Government Astronomer, Sydney Observatory—the Society’s Medal. Mr. Wood’s contribution to the Society has been rarely surpassed by any member past or present. He has been a member of Council for the years 1943-47, 1950, 1953, 1956-61; Hon. Secretary 1948, 1951, 1958-60; Hon. Librarian 1943-47, 1957; and was President in 1949. Mr. Wood joined the Society in 1936 and has been an active member since that date. Apart from the positions held on Council he has acted on a large number of committees. Since he became Government Astronomer in 1944, Mr. Wood and his group have contributed extensively to the Society’s “‘ Journal’’. This group has under- taken the immense task of mapping a large part of the Southern skies, a task which is never ending. One of the simplest duties in Mr. Wood’s eyes but one of the most important in the progress of a large city is the determination of time. Mr. Wood is responsible for the accuracy of our time signals. Mr. Wood has for many years been one of the leading publicists for science both in the serious and the popular field. This is evidenced by the long booking list to visit our Observatory. Since the advent of artificial satellites and the commencement of investi- gation into such close outer space phenomena, the value of Mr. Wood’s work in the popular educational field has increased markedly. He has done much to correct the nonsense published in science fiction and the newspapers. The Society recognizes that Mr. Wood is one of our most widely known and respected scientists and wishes him success in his future efforts at the Observatory. Martin Fritz Glaessner, Reader in Geology and Palaeontology in the University of Adelaide— the Walter Burfitt Prize. The Walter Burfitt Prize for 1962 is awarded to Dr. Martin F. Glaessner, D.Sc., F.A.A., for his work published during the last six years on problems of Palaeontology, particularly his contributions to the knowledge of Pre-Cambrian fossils of South Australia ; Tertiary stratigraphic correlation in the Indo-Pacific Region and Australia; and evolutionary trends in some Protozoa and Arthropoda. Dr. Glaessner graduated in Palaeontology at the University of Vienna, and has done research work at the British Museum (Natural History). From 1932 to 1937 he took part in several geological expeditions to the Caucasus as Foreign Specialist (Palaeontologist) for the U.S.S.R. Academy of Sciences. In 1938 he joined the Anglo-Iranian Oil Company and in New Guinea established a laboratory for research in micro-palaeontology, which was later transferred to Melbourne. Here he did graduate work at the University and obtained the degree of Doctor of Science. He joined the staff of the University of Adelaide in 1950. In 1953 he was made a Research Associate of the American Museum of Natural History, and in 1956 was elected a Fellow of the Australian Academy Of science. Dr. Glaessner has an international reputation as a palaeontologist and stratigrapher and his researches have been published in scientific journals in most countries of Europe and Asia, and also in U.S.A. and Australia. Dr. Glaessner was the Clarke Memorial Lecturer of this Society in 1953. Raymond Frederick Isbell, Research Officer, C.S.I.R.O. Division of Soils, Queensland—the Edgeworth David Medal. Raymond F. Isbell graduated from the University of Queensland with distinction in geology in 1950 and in 1953 received his M.Sc. A man’s capacity for research may be measured by his ability to adapt himself to other fields of study when he passes on from his academic training. Isbell showed just such versatility and initiative to cope with many phases of field study, ecological, pedological and practical problems of land utilization aside from geology. At an early stage he turned his attention 130 to geographical studies in valuing land resources and, as an officer of the Queensland Bureau of Investigation, covered a number of areas in central and sub-coastal regions in that State. Huis academic training stood him in good stead due to the correlation of geological structures to the land forms and the soils associated with them. Over a period of ten years Isbell has devoted himself to the study of economic resources in the underdeveloped areas of Queensland, mainly of those with a rainfall less than 30 inches. The culminating and most recent work for which he will long be noted is the survey of nearly 40,000 square miles in Central and Southern Queensland and Northern New South Wales comprising the “ Brigalow Belt ”’ characterised by growth in varying density of Acacia harpophylia. Approximately half this great zone stretching 700 miles from north to south and 50 miles wide, is covered by brigalow scrub. Isbell has recorded and analysed its soils, flora, climatology, grazing and crop potential and defined the problems in development. The notable publication of these data has been used by SOCIETY AWARDS economists and others concerned with land use in Queensland. Since the native vegetation is fast disappearing in the face of agricultural and pastoral advances, his work on the ecology and details of flora associated with this great belt of country will be a classic reference. Mr. Isbell has continued his interest throughout in geological studies. He, with collaborators, was responsible for chapters in the volume on the geology of Queensland published by the Geological Society of Australia in 1960. His record of publications beginning in 1954 contains three technical bulletins on the soil and land resources of parts of Queensland, the long publication mentioned on the ‘‘Brigalow Belt’’, three geological papers, two pedological papers and one ecological contribution. All of these involved field observations extensively over the years and together have given a mass of valuable data of particular use in these days of rapid development of Queensland. Abstract of Proceedings, 1962 4th April, 1962 The ninety-fifth Annual and seven hundred and seventy-third General Monthly Meeting was held in the Hall of Science House, Gloucester Street, Sydney, at 7.45 p.m. athe resident, Professor K. J. W. Le Fevre, F.R.S., F.A.A., was in the chair. One hundred members and visitors were present. Nicholas Victor Findler and Gurij Gordijew were elected members of the Society. The Annual Report of the Council and the Financial Statement were presented and adopted. The following awards of the Society were announced : The Society’s Medal for 1961: Dr. A. Bolliger. The Clarke Memorial Medal for 1962: Professor H. Waring; Disc:, F.A.A. The James Cook Medal for 1961: Sir John Eccles, Kt DPhil POR S., F.A.A. The Edgeworth David Medal for 1961: Dr. R. L. Slatyer. The Archibald D. Ollé Prize: Professor V. A. Bailey, D.Phil., F.A.A. Office-bearers for 1962-63 were elected as follows : President : W. B. Smith-White, M.A. Wace-Presidents: H. A. J. Donegan, M.Sc., A. F. A. Hanmer. Voc. K. J. W. Le Fevre, D.Sc:,-F.R.S., PeACa Vd. G. Poggendorft,, B.Sc: Agr. Eonsesecretaries: J. L. Griffith, B.A., M.Sc., Alan A. Day, .Sc; PhD, Hon. Treasurer: C. L. Adamson, B.Sc. Members of Council: Ida A. Browne, D.Sc., A. G. ivan b:5c.,° N. A. Gibson, Ph.D., J. W. Eiumephries, B.sc., “A. H.’ Low, Ph.D., M.Sc., Epic. MeWwerm, M.Sc.,.P. D. F. Murray, D.Sc., Boa As Gr. FL Slade, B.Sc., A. Ungar, Dipl.Ing. Messrs. Horley & Horley were re-elected as Auditors of the Society for 1962-63. The retiring President, Professor R. J. W. Le Fevre, F.R.S., F.A.A., delivered his Presidential Address entitled “‘ Some Chemical and Scientific Problems of the Late Twentieth Century ’’. Reference was made to some of the problems which are, or soon may be, confronting science and scientists. Studies of molecular architecture in relation to properties should increasingly enable chemistry to meet new challenges (e.g., high-speed flight or space exploration) or continuing ones (e.g., disease), and to understand vital processes (e.g., inheritance or the origination of life on this planet). Such particular matters can be viewed with optimism. Considered more widely, however, the outlook for science is pessimistic. Progress is already being handicapped by certain genetic problems (‘‘ training ”’, recording and accessibility of information, political and social attitudes, etc.), but these pale before the dif- ficulties (international, technological, personal, and ethical) foreseeable from the massive expansion of mankind now occurring. (Each year is adding popula- tion equivalent to 22 Cities of Sydney.) All human effort is overshadowed by the apparent predictability from present evidence of a not distant “ doomsday ” (one group gives the date as 13th November, 2026). The balance of nature has been upset. The challenge has an inexorable quality, yet is more neglected by governments than any other of the major factors in the world crisis. Consequences are obvious : can they be mitigated or avoided ? At the conclusion of the meeting the retiring President welcomed Associate Professor W. B. Smith-White to the Presidential Chair. 2nd May, 1962 The seven hundred and seventy-fourth General Monthly Meeting was held in the Hall of Science House, Gloucester Street, Sydney, at 7.45 p.m. The President, Associate Professor W. B. Smith- White, was in the chair. There were present 22 members and visitors. Eric Graham Thwaite was elected a member of the Society. It was announced that Mr. H. G. Golding had been appointed a member of the Council, Dr. B. A. Bolt having resigned. An address entitled “‘ The Employment of Women in Australia’’ was delivered by Mrs. Thelma Hunter, M.A. (Glasgow), of the Department of Government, University of Sydney. It is generally assumed that the participation of women in economic activity has substantially increased over the past half century. To what extent is this so ? And what are the major changes which have taken place in the distribution and characteristics of the female work force ? The speaker considered some of the legal institutional and conventional factors which affect the employment of women in industry. Finally, she gave an analysis of the principles apphed by Australian industrial tribunals in determining the female basic wage. What effect does this have on the application of equal pay rates? And to what extent does the 1958 New South Wales legislation on equal pay affect the Court’s principles of wage determination ? 6th June, 1962 The seven hundred and_ seventy-fifth General Monthly Meeting was held in the Hall of Science House, Gloucester Street, Sydney, at 7.45 p.m. The President, Associate Professor W. B. Smith- White, was in the chair. Ninety members and visitors were present. Ian Gordon Dance was elected a member of the Society. It was announced that the newly elected officers of the Section of Geology were: Mrs. K. M. Sherrard (Chairman) and Mr. H. G. Golding (Honorary Secretary). An address dealing with the Scientific Investigation of Crime was delivered by Detective Sergeant N. A. Merchant, of the Scientific Investigation Bureau, New South Wales Police Department. 4th July, 1962 The seven hundred and_ seventy-sixth General Monthly Meeting was held in the Hall of Science House, Gloucester Street, Sydney, at 7.45 p.m. 132 The President, Associate Professor W. B. Smith- White, was in the chair. Fifty-five members and visitors were present. Glennie Forbes Smith was elected a member of the Society. An address entitled ‘‘ On Some Problems of Artificial Intelligence ’’ was delivered by Dr. N. V. Findler, of the Colonial Sugar Refining Co. Ltd., Sydney. One of the most powerful stimuli to progress in scientific research is the bringing together of two ostensibly widely differing fields of endeavour. An example for this event is the challenging combination of research efforts from the disciples of psychology and computer science. The lecture will attempt to describe the motives and the methodology of a few works with digital computers in this field. Theoretical and practical applications cover a wide area, ranging from mechanized medical diagnosis to computer-composed music. With the advent of faster, bigger and more powerful machines the successful simulation of certain highly organized mental activities of humans has become a problem of ingenious programming rather than representing some insurmountable technological difficulty or a question unsolvable in principle. Ist August, 1962 The seven hundred and seventy-seventh General Monthly Meeting was held in the Hall of Science House, Gloucester Street, Sydney, at 7.45 p.m. The President, Associate Professor W. B. Smith- White, was in the chair. Forty-five members and visitors were present. Stephen Fisher, Robin Marie Mackay, Thomas Montagu Newman, Harold Walter Read and Harold Yates were elected members of the Society. The Edgeworth David Medal for 1961 was presented to. Dr. RK. ©: Slatyer, C:S.A.R.O.,, Division of Land Research and Regional Survey, Canberra, and following the presentation Dr. Slatyer delivered an address entitled “Some Aspects of Water (Use... 5th September, 1962 The seven hundred and seventy-eighth General Monthly Meeting was held in the Hall of Science House, Gloucester Street, Sydney, at 7.45 p.m. The Senior, Vice-President, “Protessonsax. 2). Ww. LeFevre, F.RiS., P.ALA.,; wasn the cham: (Bichty— five members and visitors were present. Charles David Badham and Lawrence Arthur Drake were elected members of the Society. An address entitled “‘ The Sydney Opera House ”’ was delivered by Mr.G. Molnar, Faculty of Architecture, University of Sydney. 3rd October, 1962 The seven hundred and _ seventy-ninth General Monthly Meeting was held in the Hall of Science House, Gloucester Street, Sydney, at 7.45 p.m. ABSTRACT OF PROCEEDINGS The President, Associate Professor W. B. Smith- White, was in the chair. Fifty-four members and visitors were present. Edward Brennan was elected a member of the Society. An address entitled ‘“‘ The Search for Oil in Australia : A Progress Report’’ was delivered by Mr. J. C. Cameron, School of Mining Engineering and Applied Geology, University of New South Wales. 7th November, 1962 The seven hundred and eightieth General Monthly Meeting was held in the Hall of Science House, Gloucester Street, Sydney, at 7.45 p.m. The President, Associate Professor W. B. Smith- White, was in the chair. There were present forty- three members and visitors. The following were elected members of the Society : William Ernest Baker and Philip Ronald Lewis. The following papers were presented: “‘ Geology of Lord Howe Island ’’, by J. C. Standard ; “‘ The Volatile Oil of the Genus Eucalyptus (Fam. Myrtaceae). 1. Factors Affecting the Problem’”’, by J. L. Willis, H. H. G. McKern and R. O. Hellyer. 5th December, 1962 The seven hundred and eighty-first General Monthly Meeting was held in the Hall of Science House, Gloucester Street, Sydney, at 7.45 p.m. The senior Vice-President, Prof. R. J. W. Le Fevre; F.R.S., F.A.A., was in the chair. There were preseng fifty-nine members and visitors. An address entitled ‘‘ Lawrence Hargrave—An Appreciation ’’, was delivered by Mr. W. Hudson Shaw, Assistant Administration Manager (G.S.), OANTAS, Sydney. A few years ago Mr. Shaw endeavoured to obtain some information in Sydney on the famous Australian inventor, without success. Shortly afterwards the author went overseas and during a prolonged stay found time to carry out valuable research in the U.S.A., England and Germany into Hargrave’s life and work. The results were recorded and given to the major Aeronautical Collec- tions of the world located in London, Washington — and Munich. Lawrence Hargrave was a prominent member of this Society for many years and the results of his experiments were made available to experimenters in other parts of the world largely through papers published in the “ Journal and Proceedings ’’. It is appropriate, therefore, that the first public presentation of the results of this research should be given to the Royal Society of New South Wales. The lecture was illustrated with lantern slides, and original models made available by courtesy of the Trustees of the Museum of Applied Arts and Sciences. See “‘ Journal and Proceedings ’’, Vol. 96, p. 17. Section of Geology CHaIRMAN: Mrs. K. M. Sherrard, M.Sc. ; Hon. SECRETARY: H. G. Golding, M.Sc. Abstract of Proceedings, 1962 Five meetings were held during the year, the average attendance being 17 members and visitors. MARCH 16th (Annual Meeting). The election of office-bearers was postponed to the next meeting due to poor attendance. (1) Notes and Exhibits : Mr. H. G. Golding exhibited specimens of rodingite and rodingite-chromitite associa- tions from the Mt. Lightning district in the Coolac- Goobarragandra serpentine belt. (2) Address: ‘‘ Lantern slides to illustrate a new course— The Nature of Geological Thought’, by Dr. L. E. Koch. Dr. Koch showed coloured slides of localities mainly from the Sydney metropolitan area, from New South Wales and other parts of Australia, illustrating landforms, rock types, structures and fossils to illustrate the new course. MAY 18th: Election of office-bearers for 1962: Mrs. K. M. Sherrard was elected Honorary President and Mr. H. G. Golding was re-elected Honorary Secretary of the Section. (1) Notes and Exhibits : Mr. H. G. Golding exhibited specimens of chromitite with ellipsoidal serpentinite structures, from Keef’s Mine, Honeysuckle Range, N.S.W. Similar types had been recorded from overseas and according to Thayer were limited to Alpine type serpentinites. (2) Address: ‘‘ Aspects of the Geology of Mull and Skye’”’, by Dr. T. G. Vallance. At Mull basic igneous sheets intruding mainly Mesozoic and Tertiary country rocks resulted in local hornfelses containing mullite and sapphire. Specimens from the contact of the Rudh, a Chromain tholeiite sill, near Carsaig, were exhibited. At Skye the Tertiary Beinn an Dubhaich granite, south of Broadford, invades Cambrian dolo- mites and limestones. Here boron and fluorine, from the granite were fixed in the hornfelses and dedolomit- ization occurred in the inner contact zone with redistribution of Mg in the cooler outer zone. Magnetite skarns, grossular-wollastonite and hedenbergite-plagio- clase assemblages and monticellite-bearing rocks occur. Fluorine is fixed in the contact zones mainly as clinohumite, cuspidine and fluorite; boron mainly as szaibelyite, datolite, ludwigite, and a new isometric mineral harkerite. Fluoborite represents fixed fluorine and boron. Specimens illustrating these hornfels types described by Tilley (Mineralogical Magazine, 1951) were exhibited by Dr. Vallance. _ JULY 20th: The meeting paid tribute by a short silence to Professor D. W. Phillips and to Mr. A. J. Shearsby, both of whom had died since the last meeting. Address: ‘“ Radio-active Haloes”’, by Professor Paul Ramdohr. MRadio-active inclusions in rocks and minerals result in surrounding haloes. The radiation may wholly or partly destroy either the inclusion or host, and the increase in volume of the resulting product can cause radiation cracks or “ blasting ”’ ranging from a few microns to two metres diameter in the host. Haloes correspond with the radii reached by the various types of alpha particles (e.g. of U, Ra, RaA) in the various mineral media, approximately 1/2000th of the radii in oxygen. Haloes have been noted in about fifty different mineral species. The former explanation for these phenomena—of local de-ionization in ionic-bonded minerals—is inadequate because haloes also occur in minerals with essentially covalent, metallic and molecular bonding (e.g. ilmenite, columbite, arsenopyrite, graphite and coal). Very strong radiation destroys haloes and facilitates special forms of early replacement, e.g. microcline by pyrite. By heating, so-called metamict minerals may be reconstituted with release of much stored energy. Professor Ramdohr illustrated his address by numerous slides. SEPTEMBER 21st; (1) Notes and . Exhibits: Miss H. Drummond exhibited a series of rocks from the Cape Dan area, near the airstrip of the American Radar Station “‘ Project Due E”’ on the coast of East Greenland. Coastal rocks along most of this area appear to be volcanic but those exhibited from this locality included acid garnet-rich gneissic rocks, pegmatites and more basic types, distinct from the fine-grained more recent flows. Miss Drummond also showed transparencies of the Cape Dan and nearby coastal area of East Greenland. Messrs. H. G. Golding and M. Veeraburus jointly noted the occurrence of a spilite-chert-tuff-greywacke assemblage on the western flanks of the Coolac serpentine belt, New South Wales. Specimens of spilite from near Brungle and of red chert and amygdaloidal lava from Mt. Lightning were exhibited. (2) Address: ‘‘ Aspects of the Geology of Thailand ’’, by Mr. M. Veeraburus. The Kohart Plateau of Thailand is regarded as a stable nucleus surrounded by the Japanese, Philippines, Indonesian and Himalayan arcs and the Malayan-Sarawak-Borneo Mountain Chains. Two major revolutions accompanied by granite intrusion—the permo-Triassic or older granite and the late Cretaceous, early Tertiary or Younger granite—are recognized. The stratigraphic column includes representatives of all the main geologic systems other than Pre-Cambrian and Cretaceous. The Upper Cambrian Phuket Series and Taroo Tao Series containing Eophytons and Saukid trilobites respectively is followed disconformably by the Ordo- vician Tungsong Limestone of the Peninsular-Perlis Region. The widespread undifferentiated Kan- chanaburi Series includes Silurian, Devonian and Carboniferous rocks lying unconformably on the aforementioned. The Rat Buri Limestone is Permian. but in places undifferentiated beds are referred to the ‘““ Permo-Carboniferous ’’. The Triassic-Jurassic Khorat Series was followed by Tertiary sedimentation, repre-. sentatives of which include lignite, oil-shale and some oil-reservoir rocks. Pleistocene deposits are widespread. Mr. Veeraburus illustrated his address with colour transparencies. 134 NOVEMBER 16th: (1) Notes and Exhibits: Professor L. J. Lawrence reported on a solid state reaction between cassiterite and bornite in ore from near Inverell, N.S.W. Hexastannite reaction rims are associated with renierite and suggest grain boundary ex-solution of the latter from the Hexastannite. (2) Address: ‘‘ Granitization Phenomena in the Jesenik Mountains in the Bohemian Massif’, by Dr. Z. Misar. Various zones of metasomatic granitiza- tion have been distinguished in the Keprnik Dome in the Jesenik Mountains, in the northern part of the Bohemian Massif. Granite gneisses of the central part of the dome represent a centre of microcline granitiza- tion: and contain large porphyroblasts of microcline up to 5 cm. in diameter. MRelict streaks of biotite SECTION ‘OF ‘GEOLOGY gneisses and inclusions of calc-silicate rock are common. In the second or augen-gneiss zone porphyroblasts of microcline as augen average 1-3 cm. in diameter. The third or “ pearl-gneiss’’ zone contains smaller microcline porphyroblasts (0-3—0-1 cm. diameter), and is surrounded by the non-granitized or primary zone of biotite-plagioclase gneisses. It seems that ata certain stage of geosynclinal development so-called permanent elevations and depressions were formed. The elevations became the centres of granitization while the depressions became centres of submarine vulcanism and exhibit a complete lack of granitization phenomena. The age of these processes is probably Pre-Cambrian. Dr. Misar accompanied his address with colour slides. AUSTRALASIAN MEDICAL PUBLISHING CO, LTD. SEAMER AND ARUNDEL STS., GLEBE, SYDNEY Ww. iH ss POGGENDORFF, B. So.Agr, = es Pe eee WE EE ah Re _ Members of ‘Council te teen tes <—E MIDDLEHURST, M.Sc, © ares ANG “NEUHAUS, AS.T.C. berks A. REICHEL, m.sc. - Se eee ho. a STANTON, Bi he tl NGATS, . 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Ts are saan ae a aut Journal and Proceedings, Royal Society of New Scuth Wales, Vol. 97, pp. 135-144, 1963 Positional Astronomy The Donovan Astronomical Lecture for 1963* HARLEY Woop Sydney Observatory, Sydney ABSTRACT—The aims and methods ct pusitional astronomy are outlined and the contribution of Sydnev Ovservatory briefly described. hemispkere, are iscussed I appreciate the invitation to give the Donovan Astronomical Lecture for 1963 because it gives me an opportunity to speak about the field of astronomy in which our Observatory at Sydney is working. Early in this century Simon Newcomb (1906) was able to say “ the determination of positions of the fixed stars by meridian observations has formed a_ large fraction of the work of the leading observatories since 1750”. Every positional astronomer rejoices that astronomy has enormously extended its bounds so that his work is now only a small fraction of the total of astronomical effort, but I have heard complaints from some of them that, despite a demand for the results of positional astronomy, it is nevertheless difficult to obtain resources and prestige for positional work. This may well be because the newer developments in astrophysics, radioastronomy and space science with their spectacular methods and results, have such public appeal that it is easier to obtain support for them. Some people, even among scientists, appear to feel that positional astronomy which has been active for so long, must be a worked out field and that appreciable improvements can be effected only with long delay or disproportionate effort. This is not so, for although unexpected spectacular results are not likely, it is clear that the application of developing techniques can yield an increase in accuracy which would be of much value in the reasonably near future. Positional astronomy works fundamentally towards the establishment of a coordinate system, a “‘fixed” non-rotating system, to which all positions in the heavens may be referred. Catalogues of stars are compiled with positions referred as accurately as possible to the system, and by comparing positions at different epochs the motions of the stars across the sky are * Delivered in Science House, on 8th Sydney, October, 1963. A Future developments, particularly in the southern evaluated and catalogued. This is done by a variety of methods appropriate to the objective, whether it may be to compile a catalogue of stars over the whole sky, or over a restricted zone or within a limited area of particular interest. On the other hand the position of isolated objects, such as members of the solar system may be sought or, possibly most exacting of all, the aim might be the determination of the distance of a star. A fundamental part is played by positional astronomy in many general activities of astronomy and astrophysics. Firstly a frame- work is provided for the identification of objects, for an accurately known position is the most unambiguous, and, properly used, the surest way of specifying and finding a particular one of any class. There are about 108 stars to magnitude 17 and 10® galaxies to magnitude 18 with many more accessible to observation by large instruments. However, there are 1-5x108 square minutes of arc in the sky so that, if a position is known with an accuracy of a second or two of arc, there can rarely be ambiguity. In some branches of astronomy insufficient attention is given to the positions which may be quoted to too few figures and even these may be in error. One frequently hears of telescope time being lost in the identi- fication of objects and of the necessity for having finding charts for them. The solution is the development of a _ position-minded attitude, for these problems would be greatly diminished if positions were accurately given and if it were insisted that telescopes should be made to point with precision. This should not be too difficult, and in an expensive piece of apparatus like a large telescope there is no reason why, with present facilities for digital and analogue computation, the pointing should not include allowance for refraction and, if necessary, corrections for flexure. Secondly, positional astronomy provides the framework for deter- GUITHSOMIAD pets ganece 136 mination of positions which are needed in celestial mechanics. This includes observations of artificial satellites. Thirdly, positional tech- niques, through proper motions, provide a sieve for the recognition of objects of various classes. Faint nearby objects are indicated by their large proper motions, and stars which belong to clusters or associations are sorted from field stars by community of motion. This process works even if the proper motion is expected to be negligible as in the case of the Magellanic Clouds (Royal Observatory Bulletins, 1963) for the foreground stars may be sorted out by their appreciable motion. Fourthly, statistical studies of proper motions, combined if possible with radial velocities, yield mean parallaxes for certain classes of stars. Hence the motions, by serving to calibrate the zero points for absolute magnitudes of the stars used as distance indicators provide a basis for distance measurement by luminosity methods. Fifthly, proper motions form part of the data for the study of galactic kinematics. In this category come researches which aim at improved values of the constants of galactic rotation and attempts to measure the expansion of associations of stars. The Coordinate System In order to specify position it is necessary to devise a system of coordinates. If these are to be satisfactory, they must conform to con- venience for the purpose for which they are to be used, and their definition should be operational in the sense that a way of making actual measurement of the coordinates is implied. Since it is direction only that is to be specified in three-dimensional space, the system is two-dimensional. There are in the heavens no fixed points to which reference may be made since the stars in space are free to move in any direction and finally the whole problem is conditioned by the fact that we, and the instru- ments with which we observe, are situated on a rotating Earth. This last point means, on the one hand, that the coordinate system, if it is to be convenient in use, must be related to the Earth’s rotation so that it will be easy to point earth-based instruments in a desired direction and, on the other hand, it means that we are provided with a way of scanning large areas of sky with instruments which have limited and stable degrees of freedom relative to their foundation. To establish a two-dimensional system we need first to be able to identify accurately and with stability at least two points in the sky, or, HARLEY WOOD of course, their equivalent a great circle and a point. One available point is the celestial pole about which the heavens appear at any instant to be revolving. It is therefore accessible to observation. The identification of the pole of the heavens leads to the establishment of the Equator as the great circle from which one coordinate, declination, is measured, and it then remains to choose some point on this as the origin for the measurement of the other, right ascension. The point which has been chosen is the equinox, the intersection of the equator and the ecliptic. It is accessible to observation, although not very readily, because the ecliptic is found from motions in the solar system, observation of which is therefore a necessary part of the programme to define the coordinate system. Some decision has to be made, and as good a compromise as possible is made by the choice of this point from which right ascensions are then measured towards the east. The definitions implied by referring positions to the equator and its point of intersection with the ecliptic are affected by the fact that both the equator and the ecliptic are in motion relative to the background of the stars and in fact must be so relative to any standard of non-rotation which is likely to be suggested. The need for operational definition for both measurement and use of the coordinates requiring relation to identifiable points or planes of the sky is satisfied if the position of any body is referred to the equator and equinox of the time of the observa- tion. Positions measured directly in accord with the definition are called apparent places. These are basic. Because of the need to have a common framework for the comparison of positions observed at different times it is necessary to investigate the motions of the fundamental planes so that the positions may be referred to the coordinates based on the equator and equinox of some selected time. Since the direction from which the light of a star appears to arrive is also varied by the motion of the Earth, the effect of this, aberration, must also be removed. Positions dealt with in this way are called mean places. They are convenient, not only for comparing positions observed at different times for determination of stellar motions, or for investigations in celestial mechanics, but also as a base from which apparent places required for observation at all other times may be computed. It is always as mean places that positions of stars appear in catalogues. They are, however, less _ basic because they depend on the adopted values of POSITIONAL ASTRONOMY the constants which describe the motions of the fundamental planes, which are also. derived from the observations. Instruments The description of the coordinates of astronomy is made more real by an account of the instruments with which they may actually be measured. The classical instrument of positional astronomy is the transit circle, but, since it has been described many times (e.g. Watts, 1960), my account must be brief. Its axis, supported on two fixed piers, is designed to be horizontal and running accurately east and west. The eye-end of the telescope is provided with a micrometer having spider lines which may be set on stars or on artificial objects for testing and calibrating errors of the instru- ment. The line of sight of the instrument determined by the spider lines in some standard position is designed to be perpendicular to the axis. In this ideal condition the instrument would thus trace the plane, including the directions of the pole and the zenith, of the meridian of its location. There is another axis of this instrument, the axis of the Earth, which by its rotation causes the meridian plane to scan the whole of the heavens accessible at the place in the course of a sidereal day. If an accurate clock is used to obtain the time when a star is on the meridian its position in right ascension may be interpolated relative to any right ascensions which, like that of the Sun, can be obtained from first principles if the declination is known. To the axis of the instrument is fitted an accurately divided circle which by reference to the reading for the zenith is used for measuring, for the determination of declina- tion, the altitudes at which the stars cross the meridian. Adjustment and maintenance of the transit circle in the desired state with sufficient accuracy is impossible, and so it is necessary to measure the deviations from the ideal so that the necessary corrections to the direct readings may be computed. The failure of the line of sight of the telescope to be perpendicular to its axis of rotation, the error of collimation, is a geometric condition of the instrument itself, and its magnitude may be found without reference to anything external except some auxiliary apparatus provided for the purpose. The departure of the axis from the horizontal has to be measured with reference to the gravitational vector. This may be found accurately because it is perpendicular to a free liquid surface from which a ray of light is AA 137 reflected according to the law of reflection. The nadir, or the zenith, is so continuously and accurately accessible that it is used as a reference point in all instruments for direct determination of celestial positions but because of the dependence of its position.on time and on the place of the observer it is necessarily only an auxiliary point and not a fundamental one. The positions of the celestial pole, including determination of the direction of the axis of the transit instrument, can be found only from astronomical observations, usually of stars near the celestial pole. These cross the meridian at upper and lower culminations at equal intervals of time and at equal distances above and below the pole, thus identifying its direction and altitude. With appropriate corrections for handicaps provided by nature, such as refrac- tion, or by man, such as non-circulatory of pivots or errors of circle divisions, the time of transit of the star leads to right ascension and the circle reading to the declination. Another instrument which is now making a contribution is the impersonal prismatic astrolabe, which has been described by Danjon (1958, 1960), who is responsible for its develop- ment. Bysimultaneous observation of the images of a star direct from the sky and as reflected in a mercury bath the time is found when the star reaches a fixed altitude which is actually near 60°. The altitude is established by the angle of the prism which makes parallel the rays from the two directions. It will be seen that the use of the bath of mercury fixes the relation with the zenith, and, when the instrument is rotated around its axis, the fixed altitude describes a small circle around the zenith. The rotation of the Earth permits the small circle to scan a zone 60° wide in declination. This instrument was designed for observation of longitude and latitude, including the variation of latitude arising from movement of the pole of the Earth’s rotation relative to the body of the Earth. The places of the stars observed may be improved by adjusting them so that consistent values are given for the terrestrial position of the observer. The effectiveness of this instrument is due to the fact that it relies on the geometric stability of only one com- ponent, the prism, which determines the altitude at which the star is observed, and this component has proved very stable. The photographic zenith tube, which was also designed for geodetic operations, can make contribution to the accuracy of catalogued star places. In this instrument the lens is arranged above a bath of mercury so that the image of 138 the star falls on a photographic plate situated just below the lens. The image plane contains the second nodal point of the lens which ensures that small tilting of the lens and photographic plate about a horizontal axis during the opera- tions has no influence on the position of the star image on the plate. The reflection in the mercury bath refers these observations to the zenith, and the meridian is identified as per- pendicular to the direction of the diurnal motion of the star. This instrument therefore scans a narrow zone of declination around all right ascensions and it is suitable for finding the errors which are functions of right ascension in the positions of stars which are accessible to it. Fundamental Corrections The observations are fundamental if they provide for the derivation of the position of the equator among the stars and the position of its intersection with the ecliptic, the zero point for the measurement of right ascension. The derived positions can then be made independent of previous catalogues. The right ascension system through its connection with the ecliptic, is defined by the motion of the Sun, observation of the declination of which, in principle, gives a correction to its right ascension. The fact that the planets move about the Sun in orbits which, with due allowance for perturbations, are plane and contain the Sun makes them also suitable for this purpose. The Sun and the classical planets differ in telescopic appearance from the stars, and systematic differences in observations of positions of the different classes of objects would be expected. For this reason the use of asteroids, which are stellar in appear- ance, was suggested for observations needed for the definition of the system of fundamental catalogues. These methods rely on Newtonian mechanics, by which the planets are taken to move, to provide a standard of rest for the coordinate system. Selected minor planets have been included in programmes for this purpose. The observa- tional programme and the solution of the equations of condition which provide for the corrections to the orbits of the planets, including the Earth, corrections to the system of the catalogue to which the positions are referred and corrections to some coefficients used in the position reductions make a formidable task. There are 164 unknowns in a scheme of Brouwer (1935). For determination of the constant of pre- cession some standard of non-rotation has to be assumed. Up to the beginning of this century HARLEY WOOD it was taken that the general mean direction of the stars remained unchanged. Then with recognition of the real systematic motions of the stars as members of the Galaxy terms for the evaluation of these had to be added to the solution, or the assumption modified. For example, the assumption could be that there is no rotational motion in a direction per- pendicular to the galactic plane or that the velocity component perpendicular to the galactic plane is on the average independent of galactic longitude (J. Schilt, 1960). The background of the distant galaxies has been suggested as a standard of non-rotation and two programmes are in progress to determine accurately the stellar proper motions with reference to galaxies to obtain values of some fundamental constants, particularly the constant of precession. The 20-inch astrograph at the Lick Observatory was designed primarily for this purpose. Yale and Columbia Observatories are establishing an observatory in Argentina with a 20-inch astrograph to extend this work into the southern hemisphere. A programme with similar aims originates in Pulkovo Observatory. This relies chiefly on photographs with standard astrographic instruments estab- lished for the Carte du Ciel programme for connecting the positions of the stars and galaxies. It will take some time before these programmes give definitive results, but it must be expected that they will yield satisfactory standards of non-rotation. If they do not, the result will be startling and well worth the resources expended on the work. Analysis of Observations Positional astronomy is a field in which even the best accuracy that can be achieved is not as good as we would wish to have. Geodesy and celestial mechanics require an accuracy of 0”-1, and this is scarcely obtainable at present. For the determination of proper motions even higher accuracy is desirable. The motions are found by comparing the positions of the stars at two epochs as widely separated as possible and dividing the displacement in the interval by the time that has elapsed. The movements are very small. It was obvious that the Copernican system implied that the revolution of the Earth would yield parallaxes for the stars, that the stars were similar in character to the Sun, and that they must be in motion relative to one another and to any framework of observa- tion that might be established. These facts were appreciated for example by Galileo, but the motions are so small that it was not until POSITIONAL ASTRONOMY 1918, almost 200 years after Copernicus, that Halley first announced the proper motions for the bright stars Arcturus and Sirius. The motions of these stars would be quickly obvious now, but Halley used positions found at times 1,800 years apart. Out of the first 1,000 stars of one of the great Yale Catalogues (Yale Transactions, Vol. 20) of star positions in a well observed part of the sky 151 have motions in both coordinates less than twice their probable errors and only 75 have an annual motion in either coordinate exceeding 0”-1. Such a need for accuracy calls for instruments of great precision and stability. Suppose that the pivots of a transit instrument are 120 centimetres apart, then an error of 0”-1 in the direction of the line of sight of the instrument corresponds to 0-6y error in either of the pivots. In general, both for fundamental instruments, and for photographic ones measuring relative positions, the stability and the accuracy of measurement sought is of the order of one micron or better. Although the transit instrument was set up to have more stability than its predecessors, it is obviously liable to distortion by the effects of changes in temperature of the surrounding atmosphere and elastic deformation which must occur under its own weight as it is moved into different positions. The compilation of star positions requires the study of the individual catalogues from which the positions are drawn. Observations in any field in which refinement is sought are always subject to error with some of the results lying above the mean and some below. This is so with the position measures compiled at a particular observatory during any period. Although observations of the accuracy required for the determination of proper motions are often taken to begin with those of Bradley in the 1750’s, it is clear that the trend towards increasing accuracy is gradually shortening the period over which it is profitable to gather observations. To show this, Table I (see Wood, 1960) gives the probable error of positions based on five observations as estimated in various periods during the past 100 years from the tables published in the General Catalogue. The value given represents the mean for the two coordinates, right ascension and declination. If the individual measures of position at a single observatory are compared for a particular star, it will generally be found that the results are scattered about a mean value in roughly the fashion one would expect for errors arising in an accidental way because the work is being 139 TABLE I Average Probable Equinox of Error in One Catalogues Coordinate 1850 0-42 1875 0-32 1900 0-24 1925 0-18 1950 0-11 done at the limit of the available accuracy ; but, when results from different sources are compared, it is usual to find that those from one catalogue consistently differ from those of another. The systematic differences in the star places remain fairly constant in one part of the sky but vary for different areas and even for stars of different brightness unless special precautions are taken to avoid what is known as magnitude equation. The source of these systematic errors must in part derive from insufficiently well determined instrumental errors or incorrect allowances for refraction but are in part obscure arising in differences of pro- cedures at different places. A star always crosses the meridian of a given observatory at the same altitude, and any systematic error which depends on this will repeat indefinitely but may well be of a different magnitude at another observatory. The circle reading for a fixed direction in space varies from day to day or even in shorter periods, and this gives rise to errors which may be a function of the position of the star. Having selected a set of catalogues, chosen because they have been observed in a funda- mental manner and with the best accuracy, the compiler of a catalogue examines them for systematic differences and _ allots them importance in accordance with his estimation. He then establishes the mean places for as many stars as he can and finds systematic differences from the mean system for each catalogue. After the positions in the catalogues have been corrected for the systematic differences the positions should follow the law of chance errors and the positions should form a harmonious system which is regarded as fundamental. When this has been compiled, more catalogues can be brought to comparison with it to find what systematic corrections they need to bring their positions to the same basis as the funda- mental catalogue. Then the systematic correc- tions may be applied to the positions of a star gathered from different catalogues _corres- 140 ponding to different epochs of observation and its motion determined. The systematic dif- ferences. between two catalogues as well as being functions of magnitude are generally taken, not necessarily with complete justi- fiability, to be in each coordinate of the form of the sum of two terms separately functions of the right ascension and declination. The systematic differences are not completely stable. The differences between Sydney “ Catalogue of 1068 Stars ”’ observed as a foundation for the system of our Astrographic Catalogue and the La Plata catalogues have been inferred from those of each as compared with the Albany General Catalogue; but there are more stars common to the two catalogues than with the G.C., and the use of these gives appreciable differences in some parts of the sky. Systematic differences commonly have amplitude running to several tenths of a second of arc. Many catalogues from individual observatories have been published in recent years. Of the compilations aimed at representing a funda- mental system one that retains importance is the General Catalogue of 33342 stars for the Epoch 1950 (GC). This was compiled as a result of work over three decades of Lewis Boss and Benjamin Boss. It includes all stars to 7th magnitude and many fainter ones whose positions and motions were derived from many catalogues. One of the necessary activities during its compilation was an expedition to San Luis in Argentina, where many observations were made to strengthen the positions of Southern stars. Despite its admitted imper- fections, the GC remains of great value because of the number of stars it contains providing among other things an intermediary between systems of catalogues which may contain few stars in common. The most recent fundamental catalogue is the Fourth Fundamental Catalogue (FK4), which contains the positions and proper motions of more than 1,500 stars with best fundamental observations over the whole sky from material in more than 80 catalogues. This has been a large undertaking, and star places should be referred to this system for several decades. This had in fact already begun before the catalogue was published. The systematic dif- ferences from the FK3, the previous best fundamental catalogue published in 1939, are in several areas more than a tenth of a second of arc, and the epoch of the places is mostly before 1920 so that the errors in proper motions must make the ephemeris places even for years in the immediate future subject to some remaining .HARLEY WOOD — uncertainty. The improvement of the Funda- mental Catalogue presents a continuing Lage to meridian astronomers. Photographic Astrometry In recent decades the great capacity of photography for obtaining relative positions has been exploited. Photographs of the same region at widely separate epochs enable relative motions of the stars to be obtained more accurately than in any other way. The same technique is used for finding the parallactic displacement of nearby stars relative to more distant ones, and the positions of members of the solar system are commonly found by photo- graphing them against a background of stars whose positions are catalogued. The cataloguing of stars by this means began with the under- taking of the Astrographic Catalogue about 70 years ago, and the extension of star positions to include fainter magnitudes and greater numbers is now almost universally done by photography rather than by differential measure- ments with the transit instrument. Many programmes apart from the Astrographic Catalogue have been undertaken in this direction, most notably by Yale University Observatory, Hamburg Observatory and the Cape Observatory. The aim is to find the positions of the stars and to determine their proper motions by comparison with positions found at previous epochs. The positions obtained. are of permanent value because they provide data for later determination of proper motions. In principle, the processes of photographic work for the determination of star places are not complicated. The photograph from a theoretically perfect lens is a central projection of a portion of the sky on the photographic plate. If rectangular coordinates of stars on the plate are measured, the formulae of this projection can transform them to differences in right ascension and declination from the centre of the plate, provided that the centre of the plate is known and its orientation in the sky has been accurately determined from the stars of known position on the plate. The photo- graphic observer needs a sufficient number of reference stars on the plate, not only to attach it to the sky in this way, but to determine, possibly by combining the results from many plates, the errors in the lens and in its adjustment as well as other effects which cause the images of the stars on the plate to depart from the position given by a true gnomonic projection. His aim must be to reproduce the system of the reference stars although, if his work is done POSITIONAL ASTRONOMY properly, there is a good chance that he will reduce the errors of the individual star places which are supplied to him by the meridian observer. _ There are many errors affecting the positions of the star images on the photographic plate. These must either be eliminated by methods of observation, or by adoption of computational techniques in the comparison of the computed positions of reference stars with those that are accurately measured on the plate. E. H. Linfoot of Cambridge once remarked to me that if it was theoretically possible for an error to be present in a lens it would be certain to be there in some degree. In this kind of work every error that can be imagined must be guarded against. The errors depend on the magnitudes and colours of the stars as well as their positions on the plate. Description of methods of dealing with these is made unnecessary by the excellent and accessible account by Dieckvoss (1962). At the present time an extensive plan for producing a catalogue of stars for the northern hemisphere is being carried on at Hamburg Observatory and plans have been formulated for similar work in the south. Sydney Observatory The work of Sydney Observatory in positional astronomy has for many years been associated with the production of a southern zone of the Astrographic Catalogue. The observatories of the southern hemisphere, being few in number were, by comparison with their resources, allotted large portions of the task and Sydney Observatory undertook the section with plates centred from —52° to —64°. This lies along a rich section of the Milky Way for about eight hours of right ascension. It was planned to publish the work in 52 volumes and work has now so far progressed that the last volume of coordinates is in the hands of the printer, and only the introductory volume describing the work and providing facilities to enable it to be conveniently used is in preparation. The Catalogue lists the rectangular coordinates of the stars on the plates and aims to be complete to the 11th magnitude. The whole of the ‘Sydney work contains the coordinates of over 740,000 star images. Melbourne Observatory was also allotted a large zone covering all of the sky south of Sydney zone. Melbourne Observatory was closed in 1944 with only three volumes of a planned eight of the catalogue published. Asa result of requests from the International 141 Astronomical Union the records were trans- ferred to Sydney Observatory and the remaining work undertaken here. The Union allotted funds for the publication. The manuscript of Volumes 4, 5, 6 and 7 was prepared and sent to Paris, where they were published, under the direction of Dr. J. Baillaud. Following his death it was decided to print the remaining volume in Sydney, and this year this volume also has been published and will soon be distributed. The probable error of a single catalogue place in either the Melbourne or Sydney Catalogue is about --0”-36 and at least two places are available for each star. | This work completed, Sydney is looking forward to using the old plate material for proper motion work, and this includes observation of a list of variable stars compiled by Plaut after the Groningen Conference on Galactic Research as well as the proper motions in some interesting areas such as star clusters. Sydney Observatory has a programme for the observation of minor planets which culminate south of the equator. The minor planets which have been selected for purposes of fundamental astronomy mentioned _ earlier receive special attention. Each year several of these which are south of the equator receive a series of observations. In this case four exposures are made on each plate and the reductions carried out with more reference stars than are used for ordinary minor planets. From one plate the probable errors are +-0”-010 sec 8 in right ascension and --0”-14 in declination largely owing to errors in the reference star places including the proper motions used to bring the positions of the stars to the epoch of observation and to emulsion shifts which must be different in different parts of the plate. Astronomical workers rightly point to parallax measurement as a difficult branch of observation, but in comparing positions of a minor planet obtained from separate exposures on one plate the parallax of the minor planet on account of the geocentric motion of the observer has to be taken into account. If it is not done, the right ascension from the later observation is almost invariably less than would be expected from the first observation, and this is after an interval which is usually only about 10 or 12 minutes. Sydney Observatory has begun plans for new catalogue work. In our astrographic zone the old epoch positions will be obtained by re- measuring, with a long screw Hilger measuring machine, old astrographic plates which will be reduced with stars taken from the Cape Catalogues. The plates for the new epoch 142 positions will be taken using a Taylor, Taylor and Hobson lens which has been acquired in recent years. This gives excellent star images over a field 6° square and the average discordance between two measures on a star image with the Hilger measuring machine is 1:3 microns. Diffraction gratings will be used to deal with magnitude equation. The taking of the plates for this programme has been delayed for some months while awaiting the arrival of a new measuring machine, for it will be easy to keep the photography ahead of the measurement. The new measuring machine is being obtained from Grubb Parsons. The measuring agent in each coordinate is a moiré scale, the movement of which is controlled by optically worked slides at right angles. The machine will measure a plate 20 centimetres square. All the mechanical and optical parts and the plate will be in an enclosed thermostatically controlled space. The pointing is to be indicated electronically by patterns on two oscilloscopes, and it is claimed that setting will be possible to better than half a micron. The coordinates will be indicated by counters to show a digitized reading. Much of the computing work for the first part of this programme has already been done by the Utecom department of the University of N.S.W. The Future of Positional Astronomy Efforts must be continued to improve the fundamental system, not only to make it consistent over the whole sky but also to establish a more perfect standard of rest and to extend the number of accurate positions to include enough stars over the whole sky to serve as reference points for all purposes and to provide proper motions to fairly faint magnitudes for studies in kinematics of the Galaxy. The complete programme may be considered at three observational levels. First the fundamental observations, second the extension in number of the stars referred to the fundamental system to a number adequate for reduction of photographs in the third stage which consists in the deter- mination of positions of the stars on the full programme. The fundamental observer’s future is related to the choice of instruments with which he must work and to their geographic distribution. There is need for development of new instruments in this field. Although at first sight the classical transit circle looks a stable instrument it is really very vulnerable consider- ing that its work requires stability of better than a micron. By its nature it cannot be protected from variations of temperature and, HARLEY WOOD as it must point in a great variety of directions, — the flexures are not easy to determine and not necessarily in the meridian. The somewhat complex micrometer, too, is required to be stable in all positions of the instrument. The list of possible weaknesses could be carried further. Considerations of this kind, as well as the existence of systematic differences between the results from different places which occur despite the vigilance that is known to be necessary in this work, show that improvement is worth seeking. The impersonal astrolabe of Danjon does not appear to be a complete answer to the problem. The great circle traced by the transit circle is a more advantageous shape for scanning the sky as the Earth rotates than the small circle around the zenith provided by the astrolabe. It has in principle no places where the observation of either right ascension or declination falls off markedly in accuracy. There should be some- thing to be learnt from the remarkable freedom of the astrolabe from systematic error depending as it does on a sound kinematic basis and on the stability of just one component, the angle of the prism, which defines its degree of freedom in positive relation to one of the identifiable points of the celestial sphere, the zenith. The design itself of the future instrument must remove from the instrument the errors that have had to be so carefully investigated in the past. Danjon (1960) himself has made suggestions for the construction of a transit instrument which by a geometrical device may overcome some of the disadvantages of the transitional transit circle. In four northern observatories mirror transits have been con- structed and it is obvious that they deal with some of the objections, notably with flexure. They are however in initial stages of their use and may prove to have new disabilities. Do they for example introduce new difficulties with refraction ? The question is of such importance that the problem is well worth an elaborate design study such as is undertaken preliminary to the construction of a great reflector. There are many suggestions, some of which have been under study, which could be taken into account. 1. Circle readings should be digitized to the full accuracy of readout rather than photo- graphed in a form suitable for automatic measurement. 2.\It may well be possible to design an instrument without the usual micrometer. The photographic and photoelectric devices that have been tried might well give assistance here. hp AE —eees - i ee POSITIONAL ASTRONOMY If necessary a return to the old situation in which right ascensions and declinations are measured by different instruments should not necessarily be avoided. This is not a radical suggestion for observers in recent years have often engaged in programmes for measurement of only one coordinate. 3. Digital readings could lead to automatic operation of the instrument. This is not meant merely to save the observer labour but to remove him from the vicinity of the instrument where, it has been proved, his body temperature can give rise to trouble. 4. If the instrument depends on a geometric principle as the prismatic astrolabe does, it might be worthwhile to set it high above the ground where it is now claimed better seeing can _be expected. Danjon says that on good nights the astrolabe results are appreciably better than on poor ones. In any case the experience of atmospheric seeing during the search for better observing conditions during both day and night might make a contribution to the design of more stable and more easily observed azimuth marks. 5. A reading of the description of the transit circle reveals that from the thermal point of view the materials of which it is usually made are far from being the most suitable. If they are structurally so desirable, it should be possible to add auxiliary stabilizing components. Such a plan has worked in Schmidt systems which are sensitive to failure of adjustment. As an example it may be possible to arrange an optical system including a mercury bath to ensure that the axis of the instrument is held horizontal by a servomechanism. Extension of the Fundamental System It is necessary to provide enough reference star positions for the photographic programme. This might be done by extending the fundamental programme to include enough stars, but more usually some of the work is transferred to programmes of transit work done differentially to extend the observations to a satisfactory number of stars. This is easier to do in the northern hemisphere where the number of transit circles is more adequate than in the south. The burden may be largely lifted from the transit observer by the use of a very wide-angle camera for catalogue work as has been suggested by Brouwer (1960). If the transit observer had fewer stars to observe, he could concentrate more attention on his fundamental system. Brouwer suggested that a field 20° square might be 143 photographed with a lens rather shorter in focal length than is usual for positional work. Naturally the accuracy of individual position measurements would be less. Deviation from flatness of the glass would be more senious but it might be possible to measure the deviation at the positions of the programme stars on the plate. Repetition of the measures and much overlapping of the areas photographed should reduce these errors. With such wide angle it may well be necessary to do all the computation in the form of apparent places, including the effects of refraction. The number of stars measured need not be large by the standard normally accepted by the photographic observer since the aim would be only to provide enough reference stars for reduction of instruments of longer focal length. The important aim would be to avoid introduction of any systematic error for the long focus observations would reduce the accidental errors. I do not know whether any progress has been made towards such a project. On the other hand, Eichhorn (1960) has shown that by arranging the photo- graphic programme with suitable overlaps fewer reference stars are needed. Another project suggested by Brouwer is the establishment of a revised General Catalogue. The epoch of the General Catalogue is now so far in the past as to make serious the effect of errors, systematic and accidental, of reduction to the present epoch. The undoubted usefulness of the old GC make inevitable a_ similar compilation. The idea is further developed by Fricke (1962), who proposes that it can be based on the FK4. Zone Observations by Photography The photographic zone observations, by which the great mass of the fainter stars are catalogued, may be improved in accuracy by using longer focal lengths and, with Eichhorn’s suggestion in mind, there is a tendency to suggest the use of smaller fields than have been customary for some years now. There must still be a com- promise here for, if much reliance is placed on the computational process and the field made small, some flexibility is lost. For the zone work a field 4° square might be a suitable compromise. The 17-inch square plates of which we in Sydney took a number in 1955 and 1956 for a programme of Yale University Observatory, are not far from the largest practical size. Brouwer and Vasilevskis agree with this. This size and field combine to give a focal length about 220 inches. For catalogue purposes good images are a requirement but a large aperture is not 144 needed. inches would be ample to ensure reaching the desired magnitudes with reasonable exposures and experience with the astrometric lens at Sydney seems to show that. a designer permitted to reduce the aperture ratio to 1:30 would have no difficulty in supplying very good star images over the whole of the suggested field. Such a programme might reduce the probable error for a catalogue place depending on results from several plates to --0”-05. This instrument would require a companion measuring machine. Electronic bisection offers enough superiority in accuracy and in freedom from personality to make it imperative. Our experience here is definitely in support of the view of experts in metrology, and of at least some astronomers, that the long screw should be replaced as a measuring agent. We acquired such a machine of excellent quality in 1951, since when it has been in use for about ten hours per week. It now shows very obviously the effect of wear although it has been lubricated regularly in accordance with the best recom- mendations we were able to obtain. A machine for extensive catalogue work must withstand a great deal of use, and it must be better to rely on a scale of some kind which would not suffer from the effects of mechanical wear. The Southern Hemisphere An astronomer of the southern hemisphere must refer particularly to the weakness of the, positional astronomy in the Southern Sky. Constantly we see references to projects in the north which are not practical in the south. One example of this is in the revision with encouraging results of the plate constants of the astrographic catalogue for some zones. This would not be satisfactory in the south. FP. P. Scott (1962), in a statement on the preparation of the FK4 in the Report of Com- mission 8 of the International Astronomical Union, says that the work “clearly indicates the necessity for more series of absolute observa- tions in the southern hemisphere’’. W. Gliese (1962) in the discussion pointed out that the errors increase south of —25° and beyond —70° they become considerable. An examina- tion of the GC (Irwin, 1960) shows that the probable errors of positions and proper motions An aperture of 8 imches: or evens, HARLEY WOOD south of —30°, about the limit that can be — reached by a northern observatory, are seriously higher than those in the north. This is despite the valuable expedition to Argentina by the Dudley Observatory in 1909. The reason for this situation is painfully obvious. In the same Commission 8 report 29 instruments which are engaged in meridian astronomy in the northern hemisphere are mentioned and only six in the south. The disparity in resources is a good deal greater than this indicates because several of the northern observatories have resources for this work greater than the southern observatories, and some of the northern instruments are of more recent construction or much modernized. The situation will only be partly improved by the expedition by Pulkovo Observatory to Chile and the projected expedition by Hamburg Observatory to Perth. The true solution is for additional instruments to be permanently established by southern countries. If the encouraging amount of experiment on instru- ments in this field should lead to clear improve- ment in the near future, it will be more important to place the improved instrument in the southern hemisphere than to yield to the temptation to modernize one of the instruments which have been set aside by northern observatories who, following the fashions of the time, have turned from positional work. References BrRouwER, D., 1935. Asiy. J., 44, 57. Brouwer, D., 1960. Astr. J., 65, 228. Danjon, A., 1958. Mon. Not. R. Asity. Soc., 118, 411. Danjon, A., 1960. Star and Stellar Systems Vol. 1, ed. G. P. Kuiper and B. M. Middlehurst, University of Chicago Press, 115. DiEckvoss, W., 1962. Sky and Telescope, 24, 198. EICHHORN, H., 1960. Asty. Nachr., 285, 233. FRICKE, W., 1962. Tvans. I.A.U., XIB, 401. GLIESE, W., 1962. Tyvans. J.A.U., XIB, 175. Irwin, J. B., 1960. Vistas in Astronomy, 3, 150. Newcomes, S., 1906. A Compendium of Spherical Astronomy. The Macmillan Company, London, p. 378. RovaL OBSERVATORY, 1963. Bulletin 66. Scott, F. P., 1962. Tyvans. I.A.U., XIa, 16. SCHIET, ic; 1960. Asty. J., 65, 218. Watts, C. B., 1960. Stars and Stellar Systems Vol. I, ed.1G)P: Kuiper and B. M. Middlehurst, acai of Chicago Press, 80. Woop, H. W., 1960. Asitr. J.,.65, 189. (Received 11 December, 1963) Journal and Proceedings, Royal Society of New South Wales, Vol. 97, pp. 145-155, 1964 Our Permian Heritage in Central Eastern New South Wales* J. A. DULHUNTY Depariment of Geology and Geophysics, University of Sydney, Sydney. Mr. President, Mrs. Ladies and Gentlemen— It is indeed very gratifying to have the opportunity of adding a little to all that which has been done by previous Clarke Memorial Lectures in perpetuating the memory of the Reverend W. B. Clarke and his part in the geological pioneering of Australia. The subject of this lecture was chosen with a view to its being of general geological interest. It is concerned largely with the geomorphology of the Central Eastern Highlands between Lithgow, Mudgee, Wellington, Orange and Bathurst. The lecture makes no significant inroads in new knowledge into previously established Tertiary and Pleistocene physio- graphy. Kather it presents, in a popular way, some new ideas provoked by results of recent research into the palaeogeography of the region from Mid-Permian through Mesozoic to early Tertiary time. It depends on distribution, nature and mode of occurrence of Permian sediments outcropping along margins of the Sydney and Oxley Basins, and forming outliers scattered across wide areas of older Palaeozoic basement rocks. From the study of field evidence, many of the broad topographical features in Central Eastern New South Wales appear as a Permian heritage, passed down from an ancient drainage system of far greater antiquity than the Tertiary elevation of the present Eastern Highlands. Clarke, The Stripped Unconformity and the Miocene Surface Marginal Permian sediments are well known along the western side of the Sydney Basin from Burragorang to Lithgow and Rylstone (Fig. 1). They outcrop from beneath Triassic sandstones, rise west towards the Main Divide, and disappear where they have been stripped by erosion from the unconformable surface on the metamorphic basement. The old stripped surface continues * Clarke Memorial Lecture delivered in Science House, Sydney, on 29th June, 1961. to rise to the west until, at places such as Hampton and Yetholme, it is higher than Permian and Mesozoic rocks from beneath which it emerged away to the east (Fig. 2). At this level, rising above 4,000 feet in some places, the stripped unconformity becomes the general plateau surface partly dissected by headwaters of both eastern and western rivers in the vicinity of the Main Divide. Outliers of Permian, standing as high erosional residuals, bear evidence of the fact that the plateau surface is the stripped unconformity. From vantage points such as Hassan’s Walls, it can be seen that the Miocene peneplain, developed in Triassic rocks on the Blue Mountains, passes west and merges with the stripped unconformity, cut in basement rocks, on the Main Divide. From other vantage points such as Cherry Tree Hill and Blackman’s Crown, it can be seen that these two surfaces, on passing west of the Main Divide, again assume their separate identities (Fig. 3). The Miocene surface falls to the west and becomes the general upper level of country into which headwaters of the Macquarie and Turon Rivers have been deeply entrenched. The stripped unconformity continues to rise to the west, as seen in far-flung Permian remnants such as Mt. Bocoble and Mt. Carcalgong. These stand high to the west of the Main Divide above the general Miocene level. They are capped with basalt flows which preserved them from erosion during Miocene peneplanation. Remote Permian Outliers and Valley Deposits North of Rylstone, Permian and Triassic sediments pass from the Sydney Basin to the Oxley Basin, and assume a north-easterly dip. Marginal outcrops of Permian extend north-west from Rylstone to Cooyal and Ulan, then west over the Main Divide, to the Gulgong-Dunedoo region (Fig. 1). South and south-west of the marginal Permian outcrops between Rylstone and Dunedoo, the country is generally occupied by older Palaeozoic J. A. DULHUNTY 146 I ‘1g \ ; Rete DIQWOUDIDgGYy-e—% X \ G41MOD eo be) DUWJOYIDA e on es z UE MEE M fo) = = S SBAIL e : ‘DOD +) x \ II'H He2qG 0 JUMUASD wWydiounye py ara STUPUTIPA SY UDTUSA F==] syuoumpey mogosay |.".] INADAT N . yoruy 9 SUOIBUTTAMra, ae os Se eas = eee an | eres Ons <) Det LOM kre Unto} trom oO i elie OM Oy ON Or at on Delt eG S008 LNANESVE olHddONWLaN (oo SA aE OT ‘a. SE NZSE CU cenee hea an Tae NOdN S.LNASWIGAS NVINASd GNY bya SA! cS ees Cae Ete ah ile 0a tn a ee DIOZOSHW HAO NOILLAGIALSIG AHL rc Cw ae: ax ; ~ eRe ON oe oleae eee ae. PE cE Ngee es, Sta Reda Nae A : een | oe : SATVM HLNOS MAN ale TEN NaaLSVA IWaALNAO AO [oacaeac DE ae a OT OR SOE Shgen seep Bie sfc nes aLk.0 wieihl® Masi shel. jaf my telpvel “co atacenite) limes. bia) en easel Nee etiiet a le a.euha, Neti-ab lohan Nts ate srg NC ree ic ica Wn ee louieNie: GAGS TaN Geol a] NTO aera © Sts [Seite no sae eo ees hae et aie ee ie ieesbuay 2 a anemic ORES SESESESED OSES See) har each iets Aa oer ae ee Core rate saan eae nee Cece Ge AD Gages: SOON ait a ee caries (auch eeiaiane ah sarin OUR PERMIAN HERITAGE IN CENTRAL EASTERN N.S.W. 147 ,OSL% a21N7 aaSog zo SIIIEMPEIET ‘A vajzsade 29, ,OOLS VEWOOLY ¥ + 7 & & Q a= ¢ Wy SI B Q is uy ,002% NOLIWYH he) og /0au apiaig wIe yr re} ,00LE 3 ,OOSE 9 cia eed of q VNVOYL ‘SI S a V = aS) 4 so ,O0fe a. 9 g, SMY Td LSONHLYE a, G oy ore ata BS 8 3 ae) nn N OE are o © ‘ey aenbsey uo LSUNHLY GT 4 ss O0LE MOY z050 } /f 3/0809 - se) = q we fav} (OO£E es ie aPIag wey = a, Ay ,OOE & fas} uesear iy Sb p o 8, ue & oore . = SOONY 000k 5 5 22H SP7eEvoOgow co) ro) Ss = 5 p 5 o ie Q n dp) Pa q aS 5 a6) > 6 Ay) x = ,009 Mory zyoOSog 2 y 2 ea q a ,0064 pra eueyony qi a0 Q OG 00k “Sa arwanbsey wp (| g a 4 sucge8pn > YO DNOGNIYANG 2 ,O0LL EB = SStq suorep a n n na ~~ ay Te ~ ,O0004 “a azrzenboey bo ob vo NOLDN/TTIM fy & ,OOSE ae %) aa Bu0gspesseD 1p & aS as fy = 38 i I Su eX ie RS a0 a Rr) q fe) aS ° ms AS, fas] Se] ¥ = Th q Qe ° oS Vy 3 ,0S8 eae! = g3 D ‘a amwenbseyr vo oggng 2 si H KS | 6 | Wy qQ x ; > oD S os v : 9 G S g ty = ~ em py ,OSPE : esiog 7y © as. S N 9 re X S K y ~N NS X 9 < b>) 9 q ,OOL Beate © aw A neu TeEyN YO F/770D 9 148 basement rocks. However, in this wide area of older rocks, between Bathurst, Mudgee, Wellington and Orange, several small secluded outliers of Permian sediments have been found. These remote occurrences have provided all important clues to Permian and Mesozoic history of much of Central Eastern New South Wales. In valleys of the Cudgegong River and MacDonald’s Creek, west and south-west of Mudgee, there occur outliers of Permian sedi- ments in which Gangamopteris, Vertabraria and Phyllotheca have been found. They consist of fluo-glacial conglomerates with erratics and ice-scratched pebbles, sandstones, mudstones and well-developed varve shales (Dulhunty and Packham, 1961). A remarkable feature of these sediments is the fact that they lie on flat floors of steep-sided valleys eroded out of Silurian and Devonian basement rocks (Fig. 4). Today the valleys are occupied by the Cudgegong River and its tributary, Macdonald’s Creek. The steep present-day valley sides of basement rock evidently represent steep sides of fiord-like estuaries in which sediments were deposited in Permian time. The present-day valleys must have been developed by re-excavation and removal of Permian sediments during the Tertiary and Pleistocene. Somewhat similar beds occur on the valley floor at the junction of the Macquarie and Cudgegong Rivers, near Burrandong, a little east of Wellington. This deposit has been described in some detail by Burgess (1960). Here again it is evident that the present-day valley has been developed by removal of soft Permian sediments from an old Permian valley which became an estuary when drowned by the rising level of the Permian ocean (Fig. 2). Still more remote from present-day areas of Permian rocks is another isolated occurrence of conglomerate and mudstone, near Euchareena, some twenty-five miles north-west of Orange (Fig. 2). These sediments, originally discovered by G. H. Packham, contain Phyllotheca, and Permian microspores have been recognized by R. Helby. They appear to represent estuarine deposits on an old valley floor situated at a level intermediate between the present-day valley of the Macquarie and the Miocene peneplain surface. The Significance of Permian Valley Deposits The Permian beds occurring on the floors of present-day valleys do not exceed 300 feet in J. A. DULHUNTY thickness. The valleys, which are steep-sided, — vary from 500 to 1,500 feet in depth. They must have been completely filled with Permian and younger sediments until late Tertiary or Pleistocene time, otherwise the upper portions of valley sides would have been exposed to erosion ever since Permian time and would have been eroded back a long way by now. It would also seem as though Triassic and even Jurassic sediments must have overlain the Permian in the valleys. Some of the Permian valley deposits along the Cudgegong River are continuous with beds in the main Permian areas to the north, and others may be readily correlated with them. Valley deposits at Burrandong were almost certainly continuous with marginal Permian beds north of Wellington before being separated by erosion. Marginal beds bordering the main Permian areas to the north are near-shore deposits and relatively thin, varying from about 200 to 400 feet in thickness. Estuarine deposits along the actual shoreline, now occurring as valley deposits, could not have been thicker than the near-shore deposits with which they are continuous. However, valleys containing estuarine sediments are between 500 and 1,500 feet deep and must have been completely filled (Fig. 5). Therefore, the Permian deposits, which were less than 400 feet thick, must have been covered by Triassic sediments. Furthermore, Triassic beds overlying Permian in marginal areas are also very thin and frequently overlapped by thick Jurassic beds on to the basement. Thus it is possible that Triassic and even Jurassic sedi- ments were deposited in the valleys above Permian beds before late Permian topography was completely drowned, and _ widespread deposition of Jurassic sands covered the whole area. This is known to have happened between Gulgong, Elong and Dunedoo, where Permian, Triassic and Jurassic sediments all occur in conformable sequence in one valley of basement topography (Dulhunty, 1939). Where late Permian, Triassic and early Jurassic sediments occur in one and the same basement valley, it is difficult to escape the conclusion that tops of valley sides must have been exposed to erosion throughout the whole of the Triassic, and so reduced by erosion to mere shadows of their original height. This must surely mean that lofty mountain ranges towered perhaps 20,000 feet above valley floors in late Permian time, and that they were reduced to ridges less than 1,500 feet high before being covered by Jurassic sands and protected from further erosion. OUR PERMIAN HERITAGE IN CENTRAL EASTERN N.5S.W. 1000 2 n ly : é os > a) q oO = Sadie BSucgaspn Jo) v is") r aa K = a z Vy n Qs 215 sy S| x : Wg c= SY ae) Oo 2 wn fon is | = o a iol) i= 3 e) co wn GvVOeY DNODTIND — -ZFIDINW . ot fy nS Z = = Oo q ag) fae] S (2) Dp oO © { + © fy 6 2 > XN 9 +7000 Fe. ony 4 1 -7000 ,OOL Jas GaOsSOYD Sue ,OOL q « SNYOUTY LS Se ee S ee RS . . SS SS N SEN Van ,00Os AY 27saden ,OOSE /eEsog epiaig uiey ,O00L daos7/ ,OOFE yOsog a79020T "Ip METAMORPHIC BASEMENT ,OOSk FIDGNW ~02U YD SP) BUEToy ,OLSEL MO/y wosog ,OGEE Y Buogespny PERMIAN ,O0OO a vesesg7e7 FOO Cte ena a. y8eose7759e5 bo 30 Miles ,OF6 . : veonvovD |. * MESOZOIC 2O ,008 : FIALVNUY igs Fic. 5.-Section along C-D in Fig. 1, showing Relations between Permian Shoreline Sediments and Basement Relief ,O0LL JaArY 7797 MESOZO/C ,000L£ MODHLIT N ,O6BL JOYIEM IW \ 2 : « 5 @ ,000L DNVUMVAIT7IeM | Y t aq < Wy i : me N a S i) OLE’ 29WeT IW % ~ Fic. 6.—Section along K-L in Fig. 1, showing Basement Relief near Lithgow 150 Basement Relief and Permian Topography The study of the unconformable surface between basement rocks and Permian sediments has revealed marked variation in basement relief from place to place. This is directly related to variation in topographical environ- ment at the time of deposition of late Permian sediments. The different kinds of basement relief fall into three main groups. The first is a generally planar surface with very minor features and gently undulating topography. This type of surface is typical of the uncon- formity near Rylstone and Kandos, as illustrated in Fig. 3. It undoubtedly represents a senile . or very mature land surface, or coastal plane, across which the shoreline advanced quickly as a result of a relatively small rise in sea level. The second kind of basement relief is an - undulating surface with isolated ‘‘ basement _ highs ” of the nature of small and rather steep- sided hills rising above the general level of surrounding basement. This kind of surface is - well developed near Lithgow (Fig. 6), where Mt. Walker, Mt. Lambie and other hills of basement rock rise above the level of the surrounding unconformable surface still partly covered by Permian sediments. The isolated hills are erosional residuals of hard rock developed by differential erosion. They must have been islands in the Permian sea, before complete submergence and burial beneath sediments. Their relatively steep sides are probably due to shoreline erosion and wave ~ action when they were islands. At several places, overlapping occurs on the flanks of isolated hills of basement rock. Near Wallerawang, at the junction of the Bathurst _ and Mudgee roads, Permian marine beds are ' overlapped by coal measures which in turn are overlapped by Triassic sandstone. This _ represents a problem somewhat similar to the occurrence, already described, of Permian, ' Triassic and Jurassic sediments in one basement valley. It means that the upper surface of the basement high was exposed to erosion during the whole of the time in which coal measures were deposited, and its height must have been reduced very considerably before submergence beneath waters of the Triassic lakes. The third kind of basement topography is that developed where estuarine deposits of Permian and Mesozoic sediments occur in valleys carved out of basement rock. It is typical where deposits of Permian occur along the Cudgegong valley and its tributaries west of Mudgee (Fig. 4), and in the Macquarie J. A. DULHUNTY valley at Burrandong. The unconformable surface actually forms the valley floor, and then passes up steep valley sides and over wide low ridges. It is a composite type of basement relief, formed by changing conditions over long periods of time. In its early stages it repre- sented youthful topography in a mountainous terrain where, in late Permian, glaciers extended down from great mountain heights into valleys which had been drowned by a rising sea level to form estuaries along a rugged coastline. Its later stages of development were set in a much more mature scene. After high snow-covered peaks and ridges had been eroded away, nothing but broad flat ridges separated the estuaries. These, by now, were little more than embayments almost filled with fresh water, along the shores of great Mesozoic lakes extending far beyond the northern horizon. Then, with further rise in base-level, lake waters crept over the sides of the estuaries. By mid-Jurassic time, water commenced to spread across low, flat intervening country, producing a vast senile swampy area where great snow- covered peaks and ridges had once towered above the coastline of a Permian ocean. The Regional Permian Picture The distribution of valley deposits and other Permian outliers, the extension of the stripped unconformity from the Sydney Basin west of the Main Divide, and the trend of overlapping of Permian by Mesozoic, strongly suggest a complicated Permian shoreline in late “‘ Upper Marine”’ time, as illustrated in Fig. 7. In this palaeogeographical map, an attempt has been made to trace the actual shoreline, based on evidence already reviewed. The general trend of the coast was from south-east to north-west, through Lithgow, Mudgee and Dunedoo ; how- ever, it was complicated by great embayments and large islands, in a general setting of snow- capped coastal mountains. Granite areas of the present-day Bathurst Plains almost certainly provided low-lying country in late Permian time. Careful studies of relative levels of Pei1mian deposits on granite and adjoining metamorphic rocks, between Mt. Lambie and Hampton in the Lithgow district, leave little doubt that the Bathurst Plains formed a large bay in the late ‘ Upper Marine ”’ shoreline. It follows that late Permian sediments must have been deposited over low- lying granite country where the Bathurst Plains have since developed largely by removal of soft Permian sediments. An even larger embayment seems to have existed further north, where OUR PERMIAN HERITAGE IN CENTRAL EASTERN N.5S.W. 151 7 a a, I ery, | SS ee ee, * Dunedoo | Riaacwen | remenni | | Putco | age2 | Se ee ES oe = | ae feN | -——\ | A ete) | =a a Tes] | ‘ee eae | USC 2 cna CI | 7 Nam 2 | -—te Dubbo = me N, | | ME | | a aN aay, ee ERS i | SETTLES, Pere OF SY STE XK udgee ey, Wellington ae asus MN) xs ae, oes rn atc ere. | Lass. = eS La Rylstone [eae ey a a e | Siwetice rt Riven ._ a [a a [Sa SHORELINE OF PERMIAN UPPER MARINE OCEAN FS” NS ) IN CENTRAL EASTERN Bathurst e S ® @ Lithgow NEW SOUTH WALES LEGEND oe | Permian Land Surface [_] Permian Ocean <~ Present Day Rwers 70 O 70 20 Scale in miles J. A. DULHUNTY 152 ‘277 OOOf- 24 OOOL- wnzOG UNJOT 7/00 - WNIOG SNOFDIVLIAD aNV AISSVANL SLY 7 LV, STAUNSVAIW TYOD ~e~ISAN FILV7 NVINATAS INIYAWW AIAIN FLV7 NVINAGFTdI WA 153 OUR PERMIAN HERITAGE IN CENTRAL EASTERN N.S.W. sospnyy Iesu spurlysiF, urojsey oy} ut Aydersodoy pue Asojossy yo JuouIdojeAeq ey} Surjessny[t suonoss—'g “D1 Sal ~<— 7807 4720S Oe Of O Of Or 7saff Y74ON/ —> WN7VOG qs aN 2 Q, “~~ 74 OOO + a 38 ss ne <8 us SS So of 84 PS Og, SY py oe = % mm m> Ry ON ZN) NS am OX Ow < mo st Ma 0) a 29 OOOL- INIIOIW UW/NID 5 729 Es / 17 OOO/- FINIOOF WNIDT SoS; 154 ocean waters extended south-west from Dunedoo to Wellington, and then south-east in a long narrow arm, or drowned estuary, probably to the vicinity of the present-day junction of the Macquarie and Turon Rivers (Fig. 7). The Macquarie and Turon River valleys of today would seem to have been formed mainly by removal of Permian sediments from valleys originally excavated by a Permian river system and then drowned by the rising level of ocean waters in late Permian time. The general south-east to north-west trend of Permian coastline through Lithgow, Mudgee and Dunedoo was determined by a similar trend in high mountain ranges. Actual positions of many of the old ranges can be seen today where Permian sediments are overlapped by Mesozoic beds along flanks of basement highs which represent eroded stumps of the original mountains. The Changing Scene from Permian to Recent If all the geological features so far discussed are fitted together like pieces of a jig-saw puzzle, there emerges a changing scene of events from about mid-Permian to Recent. The topo- graphical, structural and stratigraphical conse- quences of major events in this history are illustrated in Fig. 8. The six sections, A to F, are intended to represent progressive stages in development of present topography and geology as seen in section G, across the Main Divide from Capertee Valley on the east to the Talbragar River, between Dubbo and Dunedoo, on the west. The datum horizon indicated on each section corresponds to present sea level, and changes in its relative position from one section to another are intended to indicate the extent of subsidence and uplift at different stages in the history of the area. SECTION A Commencing at about mid-Permian, it appears that high mountains, running generally from south-east to north-west, existed in the same general area as the present Eastern Highlands and Main Divide. They carried permanent snowfields, and glaciers moved down valleys into estuaries of the Permian Ocean lying to the north-east. sidence and ocean waters gradually moved further up valleys and drowned foothills of mountains. SECTION B Towards the close of Permian time, the ocean was replaced by freshwater lakes and swamps, It was a period of general sub- | J. A. DULHUNTY and mountains had been reduced in height and ruggedness. Freshwater sediments and peat beds were deposited upon the marine strata. Subsidence was more pronounced east of the mountains, where greater thicknesses of coal measure sediments were deposited in the Sydney Basin. Only thin and somewhat discontinuous beds of late Permian freshwater sediments were deposited north and west of the mountains. SECTION C General subsidence of the whole area continued throughout the Triassic. It continued to be more pronounced to the east. This resulted in deposition of large thicknesses of sediments in the Sydney Basin, and a general tilt of the old basement surface to the east. Erosion of mountains continued during the first half of the Triassic but later in the period, with continued subsidence, mountains which had now been eroded down to mature upland hills were eventually submerged beneath water and sediments of Triassic lakes. SECTION D On passing into Jurassic time, the main areas of subsidence moved from the Sydney Basin on the eastern side of the area to the Great Artesian Basin on the north-west. This resulted in levelling off of old basement surfaces which had been tilted to the east during the Triassic, and also deposition of appreciable thicknesses of Jurassic sediments to the north-west. The present-day thickening of Triassic sediments to the east and Jurassic sediments to the north- west is a consequence of shift in position of the main area of subsidence. SECTION E An uplift of perhaps 2,000 feet appears to have occurred in late Cretaceous or early Tertiary time. This marked the culmination of a long period of subsidence which had gone on almost continuously from early Permian to late Mesozoic. The uplift produced a narrow range of elevated country trending north and south in a position close to that occupied previously by Permian mountains, and also that of the present Eastern Highlands produced subsequently in late Tertiary time during the Kosciusko epoch. The early Tertiary range must have provided a “‘ main divide’ in central eastern New South Wales, with eastern- and western-flowing rivers similar to the present-day situation. Soft Mesozoic sediments were quickly removed ~ from the elevated country by erosion during early Oligocene time. OUR PERMIAN HERITAGE IN CENTRAL EASTERN N.S.W. SECTION F Then followed a long period of peneplanation which produced a mature undulating surface, rising to perhaps 1,000 feet above sea level,by the time Miocene lateritization commenced. The mature Miocene hills, still providing a “main divide’’ between eastern and western drainage, had been carved largely from basement rock. However, large patches of Mesozoic and Permian sediments remained inlaid in the Miocene surface where they filled old valleys, or one-time estuaries, of lakes and seas. East and west of the early Tertiary hills the old Miocene surface extended in extreme senility across Mesozoic sediments which, as yet, had not been elevated at all. SECTION G During Pliocene time, uplifting of the Kosciusko Epoch commenced and eventually lifted the old Miocene surface by an additional 155 2,000 to 3,000 feet to an elevation of between 3,000 and 4,000 feet above sea level. During and following the Pliocene uplift, the old Miocene surface was further dissected by the entrench- ment of old streams which originated as a consequence of the early Tertiary uplift— following then, as now, some general trends of an ancient drainage system which has become our Permian heritage. References BurGess, P. J., 1960. General Geology of the Burrandong-Mumbil District with Special Emphasis on the Engineering Geology of the Burrendong Dam. B.Sc. Honours Thesis, Depart- ment of Geology and Geophysics, The University of Sydney. DutHunty, J. A., 1939. The Mesozoic Stratigraphy of the Gulgong-Coolah District. J. Pyroc. Roy. Soc. N.S.W., 73, 150. DuLuHunNTY, J. A., AND PackHaM, G. H., 1962. Notes on Permian Sediments in the Mudgee District, N.S.W. J. Proc. Roy. Soc. N.S.W., 95, 161. (Received 19 February, 1964) Journal and Proceedings. Royal Society of New South Wales, Vol. 97, pp. 157-162, 1964 Geology and Sub-surface Waters of the Jurassic Walloon Coal Measures in the Eastern Portion of the Coonamble Basin, New South Wales J. RADE Woodside (Lakes Entrance) Oil Co. N.L., Melbourne, Victoria ABstTRact—The Jurassic Walloon Coal Measures are represented in the eastern portion of the Coonamble Basin by the Purlawaugh and the Pilliga Beds. The Purlawaugh Beds are encountered beneath the Pilliga Beds only in topographic depressions in the surface of the Palaeozoic basement complex. eastern portion of the Coonamble Basin. the west. becomes more shaley in that direction. within the Pilliga Beds. West-north-west—trending basement ridges characterize the The Walloon Coal Measures decrease in thickness towards Decrease in the thickness of the Pilliga Beds is also to the west, for the formation The main aquifers of the Walloon Coal Measures are The thicknesses of the shales which separate the aquifers are variable. Figures for the total solids content of some of the bore water are given. Introduction The present paper deals with the Jurassic stratigraphy and hydrology of some 2,200 square miles in the eastern portion of the Coonamble Basin of New South Wales. The area under consideration is bounded to the west by a line joining Coonamble in the south and Walgett in the north, and it extends eastwards to the flanks of the Warrumbungle Mountains (Fig. 1). Stratigraphy In the eastern portion of the Coonamble Basin, the Jurassic System is represented by the Walloon Coal Measures, outcropping to the east of the area under consideration (Kenny, 1927, 1928 ; Hanlon, 1950; Mulholland, 1950 ; David, 1950). Jurassic sedimentation com- menced in some areas with the deposition of the Purlawaugh Beds, and this Formation is overlain by the Pilliga Beds. The latter contain the main artesian aquifers in the New South Wales portion of the Great Artesian Basin. Water bores have been used _ to demonstrate that the Purlawaugh Beds are characteristically developed in the structural depressions between the ridges of the basement complex (Rade, 1954, p. 81). Commonly the Palaeozoic granites and Palaeozoic rocks of the basement ridges are overlain directly by the Pilliga Beds. The isopachous map shows a decrease in thickness of the Walloon Coal Measures towards the western margin of the Coonamble Basin. The greatest known thickness was recorded from the south-east of the area under considera- tion. There 1,291’ of strata are known from Nebea No. 2 Bore, which is located 12 miles north-east of Coonamble. Yowie Bore, 12 miles north-west of Coonamble, revealed a thickness of 1,095’ for the Walloon Coal Measures; Keelendi No. 3 Bore, situated 48 miles south-east of Walgett, penetrated 1,070’ of these sediments, and Combogolong No. 3 Bore, located 18 miles south of Walgett, contained 595’ of the strata. Near the north-east margin of the basin, the quartz-feldspar-porphyry which forms part of the Palaeozoic basement was first penetrated at 2,647’ in the Gorian Bore, 39 miles east of Walgett. Only 700’ of the Walloon Coal Measures are known from this bore, and the Pilliga Beds directly overlie the basement complex. The base of the formation consists of a 3’ bed of coal, and it is overlain by 347’ of sandstone. Argillaceous intercalations appear towards the top of the formation, and the higher beds consist of sandy shales and shales, which contain beds of sandstone ranging in thickness from 6’ to 17’. The sediments are more argillaceous in the Tholoo Bore, situated some 9 miles west-south- west of the Gorian Bore and 30 miles east of Walgett. The Tholoo Bore has a total depth of 2,732’; in it the Pilliga Beds again directly overlie the Palaeozoic basement. The lower unit of the formation is formed of 207’ of sandstone ; it is overlain by 503’ of intercalated sandy shale and shale. A comparison of the sequences in the Gorian and Tholoo Bores thus reveals that the thickness of the sandy facies of the Pilliga Beds decreases in a westerly direction. This trend is maintained as far west as the Ulumbie Bore, situated 5 miles south-east of Walgett and 26 miles west-south-west of the Tholoo Bore. There the Walloon Coal Measures 158 QUEENSLAND J. RADE LOCALITY MAP SCALE OF MILES 80 0 100 ce ariel eiel Area investigated Sheed ] 151° Fic. l are 975’ thick; they are first encountered at a depth of 1,220’, and throughout their entire thickness consist of a rapid alternation of sandstones and shales. Comparable facies changes are apparent in sections traversing from the south-east to north-west of the area. These sections are available from a study of Nebea No. 2 Bore in the south-east, Wingadee No. 6 Bore, Combo- golong No. 3 Bore, and Euroka Bore in the north-west. The facies are somewhat different from those previously considered, for the Pilliga Beds in Nebea No. 2 Bore and Wingadee No. 6 Bore are almost entirely composed of sandstone. Nebea No. 2 Bore has a total depth of 1,934’. Apart from a 23’ bed of gravel, first encountered in the approximate middle of the Pilliga Beds, at 1,213’, the whole of the Walloon Coal Measures in this bore are composed of sandstone. Wingadee No. 6 Bore penetrates 605’ of the Piliga Beds immediately overlying the basement. No shale intercalations are known in the Pilliga Beds, for the whole of the thickness of the formation is in the sandstone facies. Shaley intercalations in the sandstone appear in the Combogolong No. 3 Bore, which is situated 22 miles north-west of the Wingadee No. 6 Bore. There sandstone beds in the Walloon Coal Measures range in thickness from 17’—125’, whereas the intervening shale beds are from 38’-138' thick. Similar partially argillaceous facies of the Walloon Coal Measures were encountered in the Euroka Bore, situated eight miles north of Combogolong No. 3 Bore and 11 miles south of Walgett. A 141’ sandstone bed overlies the basement complex and is in turn overlain by 131’ of shale and 62’ of sand- stone. Above this are two shale layers, 132’ GEOLOGY AND SUB-SURFACE WATERS OF COONAMBLE BASIN 159 TABLE I Walloon Purla- Bore Total Coal waugh Pilliga Beds Locality Depth Measures Beds Wingadee No. 6 2,126’ 605’ absent 605’ 25m. N. of Coonamble Coangra of — 634’ 246’ 35’ sandstone 16m. S.F. of Walgett 127’ shale 226’ sandstone Come by Chance No. 2 — 655’ absent 655’ 31m. S.E. of Walgett Keelendi No. 2 “% — 900’ absent 900’ 35 m. S.E. of Walgett Drilldool No. 2 — 7175’ 80’ 695’ 49m. S.E. of Walgett Milchomi oe 756’ absent 756’ 44m. S.E. of Walgett Kiewa — 720’ 40’ 195’ sandstone 36m. S.E. of Walgett 125’ shale 360’ sandstone Coonamble No. 3 2,179’ 900’ 48’ 852’ Coonamble Yowie . as 2,350’ 1,095’ — — 12 m. N.W. of Coonamble Weetaliba 2,073” 744’ absent 744’ 20 m. N.E. of Coonample Thurn 2,135’ 725’ 30’ 695’ 24 m. W.N.W. of Coonamble and 325’ thick respectively, separated by an 18’ bed of sandstone and overlain by a 30’ sandstone bed. From these descriptions, it 1s apparent that sandy facies of the Walloon Coal Measures are dominant along the eastern margin of the Coonamble Basin, especially in the south-east of the area under consideration. Shales are rarely encountered in the south-eastern margin of the area, are sparsely developed in the north-east, but are dominant in the west. Additional bores which are known to have entered the basement complex may be profitably examined to further elucidate the Walloon Coal Measures sedimentation in the eastern portion of the Coonamble Basin (Table I). A 920’ sequence of shales, claystones, and sandstones of the Walloon Coal Measures was encountered in the Come by Chance No. 1 Bore, situated 22 miles south-east of Walgett. Argil- laceous intercalations are ubiquitous in this section, and the thickest sandstone bed measures only 93’. The Pilliga Beds directly overlie the basement in Come by Chance No. 2 Bore. The Keelendi No. 3 Bore lies near the eastern margin of the Coonamble Basin, and thus the section of the Pilliga Beds which it penetrates is developed in the typical sandy facies. It reaches a total depth of 2,319’. The Pilliga Beds are based by a 95’ bed of sandstone. Overlying this, in turn, are 20’ of white arenaceous claystone, 13’ of sandstone, and a 42’ bed of shale. This sequence is overlain by sandstones containing three shale inter- calations. The lowermost of these _ inter- calations is 109’ thick and consists of brown shale. It is overlain by 44’ of sandstone. The middle intercalation is 33’ thick ; it consists of brown shale, and is overlain by 51’ of sandstone. The uppermost intercalation is represented by 20’ of blue shale. A 30’ bed of sandstone forms the top of the sequence. Keelendi No. 2 Bore penetrates 900’ of the Walloon Coal Measures ; there the Pilliga Beds directly overlie the Palaeozoic basement complex. The sedimentary sequence is initiated by a 347’ bed of porous grey sandstone. Higher beds in the formation are largely composed of shale. They are interbedded with sandstones ranging in thickness from 5’—35’. The Walloon Coal Measures are 775’ thick in Drilldool No. 2 Bore, where the Pilliga Beds contain, in their upper portion, three inter- calations of shale, which correspond to the shale units in Keelendi No. 3 Bore. These shales are from 7’—50’ thick. The Purlawaugh Beds are not developed in the Milchomi Bore. A sandy facies of the Walloon Coal Measures is revealed in the Kiewa Bore. Coonamble No. 3 Bore enters the basement complex at 2,138’. The Purlawaugh Beds overlie the basement. The basal layers of the Pilliga Beds are composed of thinly interbedded sandstones, shales, and sandy shales. Higher beds are formed of sandstone, and the upper layers of the Pilliga Beds consist of sandstone and _ sub- ordinate thicknesses of shale. The upper beds are composed of a 35’ bed of shale, which is overlain, in turn, by 126’ of sandstone and two thin shale beds separated by an 8’ and a 6’ bed of sandstone near the top of the formation. Quambone No. 2 Bore, situated 20 miles west- north-west of Coonamble, attains a depth of 2,026’. It penetrated a sandy facies of the Walloon Coal Measures, and revealed two intercalations of gravel in the sandstone. 160 The Yowie Bore is 2,350’ deep. Successively overlying the basement complex are 4’ of fine- grained black sandstone, 20’ of fine-grained black sandstone and shale, 25’ of fine-grained brown sandstone, shale, conglomerate, 30’ of conglomerate, 15’ of shale, 222’ of sandstone, and 60’ of conglomerate containing coal beds. Three additional beds of conglomerate appear higher in the Pilliga Beds. The present author (Rade, 1954) has suggested that this sequence is a product of cyclic sedimentation. Yowie Bore is situated on one of the west-north-west- trending Palaeozoic basement ridges which penetrates from the eastern margin into the eastern portion of the Coonamble Basin. Faulted parallel basement ridges are known further to the north, near the eastern margin of the basin (Rade, 1954), and it is possible that the ridge on which Yowie Bore is located partially owes its origin to faulting. The black sandstone bed at the base of the Pilliga Beds in the Yowie Bore is of interest. It is comparable with the carbonaceous seam in contact with granite near the bottom of the Gorian Bore. Both beds point to stagnant conditions at the time of deposition of the basal strata of the Pilliga Beds. However, the 347’ of sandstone overlying the coal in the Gorian Bore attest well aerated conditions, and the absence of any form of cyclic sedimentation. Different conditions prevailed in the vicinity of the basement ridges further to the south of the Gorian Bore. There, saltatory uplift of the basement ridges is assumed to have been responsible for cyclic sedimentation. The faults which border the ridges of Palaeozoic basement complex were initiated in pre-Jurassic times, but were rejuver:ated during the Jurassic. Hollywood No. 1 Bore is 2,065’ deep and is located 26 miles north-east of Coonamble. In it the Pilliga Beds are 727’ thick and consist of sandstones containing a 20’ and a 27’ bed of claystone. The Weetaliba Bore penetrated the basement complex at 2,010’. The Thurn Bore penetrated the Palaeozoic basement complex at 2,118’. Directly overlying the basement complex is 30’ of Purlawaugh Beds. At the base of the Pilliga Beds is an 8’ bed of sandstone. This is successively overlain by a 2’ bed of coal and 189’ of sandstone. The upper portion of the Pilliga Beds consists of interbedded sandstones, sandy grey shales, and white claystones. Geological Structure West-north-west-trending ridges in_ the Palaeozoic basement complex dominate the geological structure of the eastern portion of J. RADE the Coonamble Basin. feldspar-porphyries directly underlie the Pilliga Beds in the north-eastern corner of the map area. Further to the south a granitic basement ridge appears as a structural nose in the Palaeozoic basement contour map published by the author (Rade, 1954, text-fig. 2). The Pilliga Beds overlie granite in Keelendi No. 1 Bore, some 44 miles north-east of Coonamble. To the north- east of this granitic ridge the Purlawaugh Beds appear in Drilldool No. 2 Bore. The next basement nose to the south is found 26 miles north of Coonamble. A structural depression filled with the Purlawaugh Beds exists between these two basement noses. Some 40’ of the Purlawaugh Beds are known from the Kiewa Bore, 48’ are recorded from Coonamble No. 3 Bore, 40’ appear in the Thurn Bore, and they are also present in Quambone No. 4 Bore. The Purlawaugh Beds also overlie the basement complex in the Coangra Bore. The vicinity of this bore is occupied by a deep depression in the surface of the basement complex, with the result that the maximum thickness of 246’ for the Purlawaugh Beds is recorded in this area. The depression is elongate to the south-east and is bordered to the east by a basement ridge. The isopach map of the Jurassic (Fig. 2) presented in this paper is constructed between the base of the Mesozoic and the upper artesian aquifer of the Blythesdale Group. It shows that the Jurassic sediments are thickest on the eastern side of the map area, i.e. along the western marginal depression of the Eastern Australian Cordillera. This depression can be traced northwards as far as the Gulf of Car- pentaria, and southwards beyond the Oxley Basin. Petroleum has been found in this depression in south-eastern Queensland. Hydrology The most important artesian aquifers in the Walloon Coal Measures are located in the Pilliga Beds. The upper aquifer generally occurs in the top 100’ of the formation, and it is frequently encountered a few feet below the overlying formation. Such is the case in the Milchomi Bore, where the upper artesian aquifer of the Pilliga Beds is penetrated at the top of the sandy sequence of that formation, at a depth of 1,162’. In those sections of the Pilliga Beds in which the upper 100’ is impervious and does not contain intercalations of porous sandstone, the highest aquifer is frequently much deeper. The depth of the second main aquifer of the Pilliga Beds is variable, depending on the Granites and quartz- — GEOLOGY AND SUB-SURFACE WATERS OF COONAMBLE BASIN 161 @WALGETT @THOLOO Qui umele fe) & § eal 7 rg EUROKA @KEELEND! Ve, Nea ee @ KEELENDI relele) Nol (oy pe wCARINDA @MILCHOMI MBONE @ THURN ea ar @ NEBEA Noo COONAMBLE COCNANBES @ QUAMBONE No.2 GALARGAMBONE WATER BORE SHOWN S ISOPACH MAP OF THE JURASSIC v THUS @ OF THE COONAMBLE BASIN N.S.W. PALAEOZOIC BASEMENT CLOSE CONTOUR INTERVAL 200 FT TO SURFACE OR OUTCROPPING SCALE OF MILES SHOWN THUS B&Q 4 2 0 z 8 12 ; m WARREN ee ee Fic. 2 162 TABLE II Grains of Bore — Aquifers Total Solids per Gallon Gorian ae sue — 48 Weetaliba A an — 26 Quambone No. 2... a 30 Hollywood No. 1... — 42 Wingadee No. 6 as — 50 Come by Chance No. 1 — 55 Come by Chance No. 2 1,862’ 61 2,195’ 57* 2,437’ 60 Euroka 1,584’ 74 1,938’ 62 2,433’ 55 Combogolong No. 3.. 1,695’ 69 1,910’ 1,985’ 57 2,107—2,122’ 2,343’ 58 Coangra as oe — 74 * When all of the flows are included. thickness of the impervious strata which separates the two aquifers. Impervious inter- calations may be represented by shale. In the Hollywood No. 1 Bore, the first artesian aquifer in the Pilliga Beds was encountered at a depth of 1,265’, and it is separated by impervious shales from the next aquifer, at 1,440’. The artesian aquifers of the Walloon Coal Measures from 2,478’-2,535'’ and at 2,732’ in the Tholoo Bore contain 47 grains of total solids per gallon. Similarly, 48 grains of total solids per gallon were encountered in the water of the Gorian Bore. Both these bores are in the northern portion of the area under study. Only 26 grains of total solids per gallon occur in the Weetaliba Bore, situated near the south- eastern margin of the map area. As is the case for the Weetaliba Bore, the Quambone No. 2 Bore also obtained good water from the main southern intake area, and its total solids content is only 30 grains per gallon. Wingadee No. 6 Bore, which is situated in the middle of the area under consideration, has a total solids content of 50 grains per gallon. The deeper J. RADE flows in the Euroka Bore contain less dissolved — material than those from shallower depths (Table II). Shale is a prominent sediment in the Euroka Bore, and the hole is situated in the part of the Coonamble Basin where “salting ’’ is common in sections of high shale content. A similar picture is obtained for Combogolong No. 3 Bore. The extremely high figure of 74 grains per gallon was obtained for the Coangra Bore. The results of the chemical analysis of the water obtained from the bores can be found in Report of Interstate Conference on Artesian Water (1912), Report on the Second Interstate Conference on Artesian Water (1914), and Report of the Fourth Inter- state Conference on Artesian Water (1924). From the figures given above, it is apparent that when the upper portion of the Pilliga Beds is shaley in nature, then the highest aquifer in the formation is more saline than the lower aquifers. The water with least total solids is encountered in the southern and eastern portions of the Coonamble Basin close to the intake beds. References DavID, Sir T. W. EDGEWoRTH, 1950. of the Commonwealth of Australia.’’ W. R. Browne. Arnold, London. Haniton, F. N., 1950. Preliminary reconnaissance survey of the north-western coalfield. Geol. Rep., Dept. Mines, N.S.W., 1989-1945, 92. Kenny, E. J., 1927. Geological survey of the Coonabarabran-Gunnedah district, with special reference to the occurrence of sub-surface water. Ann. Rep. Dept. Mines, N.S.W., 130. Kenny, E. J., 1928. Geological survey of the Coonabarabran-Gunnedah district, with special reference to the occurrence of sub-surface water. Ann. Rep. Dept. Mines, N.S.W., 117. MULHOLLAND, C. St. J., 1950. Review of the southern intake beds of N.S.W. and their bearing on artesian problems. Geol. Rep. Dept. Mines, N.S.W., 1939 - 1945, 125. Rave, J., 1954. Geology and sub-surface waters of the Coonamble Basin, N.S.W. J. Proc. Roy. Soc. NSA 288s Ti: Report of Interstate Conference on Artesian Water, 1912, Sydney. Report of the Second Interstate Conference on Artesian Water, 1914, Brisbane. Report of the Fourth Interstate Conference on Artesian Water, 1924, Perth. “ The Geology Edited by (Received February 27, 1963; as revised February 24, 1964) Journal and Proceedings, Royal Society of New South Wales, Vol. 97, pp. 163-173, 1964 On the Gibbs’ Phenomenon in n-Dimensional Fourier Transforms JAMES L. GRIFFITH pe ceren: of Pure Mathematics, University of New South Wales, Kensington Apstract—It i is shown that with the simple inversion formula, the Hankel transform exhibits a Gibbs’ phenomenon at a point of discontinuity of the same magnitude as in the cases of the Finite Fourier and one-dimensional Fourier transforms. In the case of the -dimensional Fourier transform we must add reasonably heavy restrictions in order that the simple inversion formula should converge. When we do this we find that this transform will exhibit the Gibbs’ phenomenon. In the simplest cases this magnitude will be equal to that in the two transforms mentioned above. 1 The Gibbs’ phenomenon was originally discovered in connection with the simple summation of Fourier series. It is discussed thoroughly in Sansone (1960, pp. 141-148). In its simpler aspects it may be described as follows: Suppose that f is continuous and of bounded variation in a neighbourhood of x) except that at %) it has a simple jump h=/f(%)+) —/(%)—) at % . Let the Fourier coefficients of f be {a,} and let the Fourier terms be {,}. Now write S,(x)= 3 a,0,(2). Then as m—>oo, the approximation curves S,(x) tend to flea b)-+h(U/n) || y-tsiny dy] as aera and to F(%)—) —h(1/7) {: yt 8 ny dy| aS x>%— We can alter the aspect of the eee if we consider it as a feature of the finite Fourier transform. Thus if i TEC n=l, Zeus 2r als eam) then the particular inversion formula A Jin f(x) =T[a,] am 2 iaPal )=lim > Ain Pn(% ) - nw »oe k=1 possesses the Gibbs’ pHOHORENOn: This shows that the phenomenon i isa feature of the particular inversion formula reas for the transform. Cc 164 JAMES L. GRIFFITH 2 The one-dimensional Fourier transform for functions in L1(— 00,00) may be written as co F(y) =n) OU flalax. (2.1) We then consider R I(x,R) =n) e—*7 F(y)dy. (2.2) —R When f(t) is continuous and of bounded variation in the neighbourhood of x, we know that lim I(x,R)=f(x). R—>oo It is also known that the inversion formula lim I(x,R) exhibits the Gibbs’ phenomenon ; R—->0o see, for example, Papoulis, 1962, p. 30. In order to clarify Section 4, we will include a few remarks on this situation. It is easy to prove that if f(¢) is continuous in an interval (x—8, x-+6) then (2.2) converges uniformly to f(x) in (x—438, x+498). We now suppose that f(#) is continuous and of bounded variation in a neighbourhood of %, except that it possesses a simple jump / at %). We write f)=8) —P) where p(t)=h, %y»—A0, we see that I(x,R)—>(h/) { ‘ =" =h—(h/) | : nay (2.3) and when «<0 I(x,R)—>(h/x) \ : a du =(h/n) | EE, (2.4) Jay GIBBS’ PHENOMENON IN n-DIMENSIONAL FOURIER TRANSFORMS 165 Both integrals on the right side of each of the last two equations take the maximum values when «=—7. A limit of the form in (2.3) and (2.4) shows that the Gibbs’ phenomenon takes place. The maximum value of the error is found by suitable choice of « To be more exact we should say that we have shown that the error is at least as great as error found by maximizing the error in (2.3) and (2.4). 3 We now examine the Hankel transform in the form Fi)=| Oot onstoa 0 and the corresponding integral R I(x,R) -| (xy)? Jo(xy) F(y)dy. 0 (3.3) (3.2) The result we require is: If f(x) belongs to L1(0,00) and is continuous and of bounded variation in the interval [a,b], then J(x,R) converges uniformly for all x in [4,g] with 00 —(1/r) IL ae y+O(R- 1) for «<0. (i ny | ‘Then referring back to the previous section, we note that the Hankel transform ree wae inversion integral in the form of (8.2) possesses the Gibbs’ phenomenon. | When v=m or m-+-4 for integral m, the Hankel transform can be considered to be the (v 49)th dimensional Fourier transform of a radially symmetric function. Thus it will be of interest to examine the k-dimensional Fourier transform to see whether the Gibbs’ phenomenon will be displayed in cases when radial Riga ed is lacking. MiCALT SR TNE 4s Vaaacaen Wa dieea: ey pp ae reat ie nis : : i : ; leit 7 feet eae i ina va 4 sid Ce ie ary Dencee ‘the k- erence Cartesian space os E,,. We define the Fourier transform ites fires Wey ot el] Ma (2 ass COIS tii sae mer Pe) PY bechee FW) =(n)-#* | ; ane Gea eo (4.1) : where we assume that f belongs to L1(E,) and that the symbols ~ and x denote the vectors (u,,.. .,%,) and (%,,.. .,%,) respectively, while x.u is understood to mean the corresponding scalar product. ee ee bois append We will examine the integral | I,=(2r) af exp [He] Fav, (270 ya f T(y) var, exp [1(u.(y—x))]aV,, where B, is the k-dimensional ball Hats adie: R, that A ihe set of points in the wspace with Jul0oo unless R=2 (McLachlan, 1941, p. 158 (13)). Thus for k>2, we cannot expect lim I, to converge if Q(s) possesses a jump discontinuity R->00 on any sphere with centre x. Suppose that k=2, then 27 Q(s) =(1/27:) f(x-+s cos 0, y-++s sin 6)d0. 0 Proceeding formally from equation (4.2), we obtain 0 [5 wneRemas=—|jeR]” +f” JisRre"As If we suppose that Q(0-+) exists, Q(s)->0 as soo and that Q’(s) belongs to L1(0,00) then we may take the limit to obtain lim ” R1J,(sR)Q(s)ds=Q(0-4). R>o J 0 We may go a little further when k=2 by supposing that Q(s) possesses a finite number of jumps but is otherwise absolutely continuous. If Q(s) possesses successive jumps at s=a and s=d, then [ wrsRoa——[p6RMeE] +] pieRMeroas where all the terms on the right will vanish as Roo. 168 ee JAMES L. GRIFFITH We return to the general case and write as is usually done v=3(k—2), then ip | ” R19» Jy 44(sR)Q(s)ds 0 00 -| Ritv2ryt—1) Jy 4,(2Ru*) O(2ut)du 0 (by change of variable) = | 2Re+2 (Ren) 1049 ff BR) [ORM 0 We now proceed formally using integration by parts and McLachlan, p. 158 (21) : Tp=—2°R* to —t ]¥(2Ru3) porous | 0 __Ov R2v—2 [ R2u) -#0-) Jy_3(2Ru?) pogrounye ©0 0 __9v R2v—2n [ R2u)—30—*) Jy_»(2Ru4) [wr Q(2u?)] ) 00 0 $2rRe-e0 (R2u)-20—") Jy _ (2 Ru) [wr Q(2u3)]¢+1du, (4.4) where the indices indicate derivatives with regard to wu. We note that we have assumed that f(x) belonged to L1(E,). Thus with a change of origin | s*—1| Q(s) | ds is finite for all x. By a further change of variables | ur | Q(2u4) | du is finite 0 0 and can be seen to be uniformly bounded for all x. These assumptions will not be sufficient to ensure the validity of all the steps in equation (4.4) so we will assume that Q@)(0+-), for 0< 0oo + lim an | Jo(2Ru*) [um Q(2u4) | + Nd. (4.6a) R—> oo GIBBS’ PHENOMENON IN n-DIMENSIONAL FOURIER TRANSFORMS 169 In order to ensure the vanishing of the integral in (5.6a) it will suffice if we assume that u-t[u™ O(2u4)|(™+1) belongs to L1(1,00) and that [w”Q(2u?)]@™+) belongs to £1(0,1). Then lim Ip=2"T\(m+1)Q(0-+). (4.6) R—->0o Now when v=m-+4, we make corresponding assumptions on [w”+?Q(2u2)|™, All integrated terms in equation (5.4) will vanish. We are then left with i —onsRi| u-* J3(2Ru?) [um+e Q(2u*) | (m+1)dy 0 =en/r(a) | u-* sin 2Rut [u™+?Q(2ut)|+Ddu. (4.7a) 0 The limit R->oo in equation (4.7a) can be evaluated by the use of Fourier’s single integral theorem (Titchmarsh, Th. 12, p. 25). To be able to apply this theorem we must be assured that [u”+?Q(2u#)|(+1) belongs to L1(0,00) and that u3[u™+#Q(2u3)|(+ is of bounded variation near the origin (and continuous). The result will be lim [,=2"+4D (3) lim w2[u™+2Q(2u3)] (+) R—->0oo u—0+ =2"+4D (414) (0-4). (4.7) We recall that the “ area’ of the surface of the k-sphere (i.e. k—1 volume) with radius unity is 2r#*/T\(4k) =27%t1/['(v+1). Thus both the equations (4.60) and (4.7a) may be interpreted to be | F(x, +sp1,.. .,%,+sp,)dA nTiegel — imm SE ete ere Sa a eNO Da 4.8a R-~> s—>0+ A 1 ( where A, is the area of the unit sphere. When / is continuous, the limit in (4.8a) reduces to f(x) as expected. We now assume that x is restricted to lie in a compact region C of the k-dimensional space E,. We wish to add restrictions on Q(s) which will ensure the uniform convergence of the limits in equations (4.65) and (4.7b). It is difficult to decide what are the best conditions to impose, but it is obvious that when v=m, the following will be sufficient : For all x in C (i) Q(s) is continuous ; oO b (ii) there exists a b so that { | u-2[u™ O(2u3)]+) | du and { | [wm Q(2u2)|(™+1) | dw are b 0 uniformly bounded ; (il) [u"Q(2u2)|™ is bounded uniformly, Here (i) is necessary to ensure the existence of Q(0+). The condition (ii) is sufficient for the vanishing of the summation terms in equation (4.55). Condition (ii) is sufficient for the uniform vanishing of the integral in equation (4.50). When v=m-+4, the limit Q(0++) does not appear explicitly so it is to be expected that the conditions imposed will be considerably different. Write P(s)=u™+4[Q(2u2)|™+1), s=1?, so that | u-* sin 2Rusfun +4 Q(outyimendu= | sin RsP(s)ds. 0 0 170 JAMES L. GRIFFITH Then for x in C we will assume that (i) | P(s) | ds converges uniformly at the upper limit. 0 (ii) The variation of sP(s) in [0,0] for every fixed 0 is uniformly bounded. (iii) sP(s) is continuous in [0,c]xC for some c>0. We give an outline of the proof of the uniform convergence of the limit. Write 00 ¢c b oO | sin Rs P(s)ds= | -l. | + | sin Rs P(s)ds. 0 0. Jc Sutp co Then choose 0 so that | | P(s) | dsoo. A similar treatment applies to G(s). c | F(s) sin Rs/s is—F(0+){ sin Rs/s as+| (F(s) —F(0+))sin Rs/s ds 0 0 n nN +f (f(s) —F(0+)) sin Rs/s ds. 0 The choice of y so that | F(s)—F(0+) |o J 0 P(s) sin Rs/s ds=47 lim sP(s) s—>0+ = lim ut[umt+t O(2u8) |] +1) u—>0+ the convergence being uniform. 5 Suppose that P is a point situated a distance x from a plane, and lying in a region A which crosses the plane. Suppose also that fis defined so that appropriate conditions in Section 4 hold. Further, let f=1 on the side of the plane remote from P and =0 on the side of the plane including P, in a sufficiently great region. Then for sufficiently small s we see that Q(s)=0 on the side of the plane including P and on the remote side cos—!x/s Prd Pia Q(s) =(270) #27 | Std, { ae i Sa. YS Op aes 0 0 0 cos—?! x/s =e-wHyrae—ayray {~~ st*40, Again writing y=4(k—2) and making some simplification, we obtain i Oem) —e-—yT etary | aA xP/4u GIBBS’ PHENOMENON IN n-DIMENSIONAL FOURIER TRANSFORMS 171 and with a further change of variables De ean be 4u wut) =(2-*/PO4HT(H) | uated (6.1) .' Suppose that v=m an integer. Then [wm Q(2ut)}m) = 2—m—I7.—1 I : (4u—z)—#2-*dz =2-"7-1 cos—! (x?/2u3), Uu>4x2, =(0), U<4x?, Further [um Q(20t) | +1) = 12 —-—-lyu"(4u—x7)-t > 4x7. The corresponding to equation (4.6a) we obtain 3b? Tp=(1/27) | Jo(2.Ru*)xu-1(4u —x*)—2du ; 3x? b =(1/7) (i ; Jo( Rs)xs-1(s? —x?)—2ds =(/n){ | JPOP RAR ds If we now put Rx=« (a constant), we find that lim Iy=(t/n) [aJalA)h-1(6*—at)-Aap =+(/n) | ~ sin yly dy (5.2) (using Erdelyi, 1954, p. 18 (5) somewhat modified). This result shows that the situation exhibits the Gibbs’ phenomenon. If v=m-+4, m an integer [wm +4 Q(2ae4)} om) —(2——14/T(Z)).(208 —x), u>ix? =0, Uuix? =0 U< px, Thus from (4.7a) suitably modified 163 I = (1/2n) | u— sin 2Ruidu te! Rb =(i/n)|_ p-sin pap Thus lim Ty=(0/n) | p- sin pap TX a. R-> a In other words the expected Gibbs’ phenomenon takes place. 172 | JAMES L. GRIFFITH 6 When f/ is not a constant on the side of the plane remote from P in the sitianern ee eaee in Section 5, we may then write Q(s)= { ib Si*F(s,0,)d0, (6.1) 0 where now 2m (rt F(s (sO) — (270) “ef fee ip Ser ae ee S,—sf(S,0;, e ize, .6 pedo ° 207s: With the same change of variables as before 4u uy O(2u3) =2 “ef (4u—z)-*z2—-2F(2u3, cos—1z?/2u4)dz xe 2us =2 72 | (4u —??)-2 F(2u4, cos ¢/2u*)dt x We will assume that F(s,0) has sufficient bounded derivatives 0¢+°/0s700°=Fa,(s,0). For us to proceed at least formally. Suppose that v=m an integer, then 4b? Quh 28 J (2Ru*)du 2—enam/aums | (4u—f?)"—-1F (2u3, cost /2u4)dt 7 x and after putting f=w/R and u=v/kR? LR? 2uh 12 Jo(2v?)dv amnjogme | (40 —w?)™—4F (2v?/R, cos—! w/2v?)dw. (6.2) ao If we expand the derivative into the sum of its components by Leibniz’s Theorem we can show that all terms involving Fy, with a>0 will be O(R-#) as R-oo. Otherwise proceeding formally, we obtain 2vk hm 2 = “{ Jy(2v otydvams3/aome | (4v—w?)™-2F (0+, cos! w/2v*)dw. (6.3) R— oc If we restrict the case to two dimensions, k=2, i.e. m=0, we obtain 2vt lim ae Jol (2v3 ydvaya0 (4v—w?)-2F(0-+, cos} w/2v?)dw R—-> 0 (oe) 1 = Jo(20tydv/a0 | (1—#)-?F(0-+, cos é)dt za* [20% = 4(a/v)(4v—a?)—3 J,(2v*2) F(0+, cos! a/2v4)dv == | : (a/s) (s?—a2)-2 Jy(s) F(O+, cos! a/s)ds. (6.4) GIBBS’ PHENOMENON IN n-DIMENSIONAL FOURIER TRANSFORMS 173 In the case of four dimensions k==4, v=1 a similar reduction gives at aI, Sols) ane cos! «/s)ds ane Zo a a2 238) Jo(s) Fya(0-+, cos? a/s)ds 6.5) When v=m-+4, we write 2urs umtt O(2u2) =2—2m—1 | (4u—t?)™F(2u*, cos—} ¢/2u*)dt x As mentioned above, when we examine 0 | u-* sin 2Rut[um+?Q(2ut)|+Ndu we will find that the terms in the expansion of [w”+?Q(2u3)]™+) which involve Fa, with a>0 will contribute nothing to the limit. The limit result will be 0 : 2 m+1 (2v4 lim I,=2-"-2/T(2) | nan S) | (40 —w2)™ F(0-4, cos! w/2u3)dw R—>00 In the particular case when k=3, m=0 we find that 00 : 1 1 lim I,=(1/(27)%) { se eS & { F(0-+, cos? pat] R->o a/2v4 =cyien)) |” sin Be F(0, cos-+ dt + F(0 +, cos} o/3)| ds a a/'s which is easily seen will reduce to our previous result if F(s,0) is a constant. In the case k=5, m=1 the limit can be expressed in the form % (2 Zi lim 1=(*) | sin $ la (1—#) F(0+, cos #)dt ae FO. costes) [as R—> a as Papou.tis, A., 1962. The Fourier Integral and its References » A ) ERDELYI, A., AND OTHERS, 1954. Tables of Integral sieiblesraloyes MMelenehn 128th Transforms. Vol. 2. McGraw Hill. SANSONE, G., 1959. Orthogonal Functions. Inter- science. McLacHian, N. W., 1941. Bessel Functions for TITCHMARSH, E. C., 1948. Fourier Integrals. Oxford. Engineers. Oxford. (Received 20 July 1963) x ion Journal and Proceedings, Royal Society of New South Wales, Vol. 97, pp. 175-176, 1964 Lower Cretaceous Sporomorphs from the Northern Part of the Clarence Basin, New South Wales J. RADE Woodside (Lakes Entrance) Oil Co. N.L., Melbourne, Victoria ABSTRACT—Preliminary results of spore analysis of some soft coal seams from the northern part of the Clarence Basin are given. Eighteen species were identified, four including the strati- graphically important Perotrilites striatus Cookson and Dettmann, confined to the Lower Cretaceous. the Clarence Basin is Lower Cretaceous. Introduction In 1961 samples of soft coals were collected from the upper part of the grey shales of the Walloon Series at many localities in the northern part of the Clarence Basin. At that time it was believed that the Walloon Series was of Jurassic age and the Cretaceous began with the deposition of the overlying Kangaroo Sandstone. Pre- liminary work on samples from near Old Bonalbo (64 miles north-east of Old Bonalbo), the upper part of a large quarry near Bexhill and from Nimbin has shown them to contain spores not older than the Lower Cretaceous, implying that the upper part of the Walloon Series in this area is Lower Cretaceous. These results are being QUEENSLAND ee a BONALBO NEW SOUTH WALES eGLEN INNES GRAFTON e LOCALITY MAP | Scale of Miles eee AEE: 0 10 20 30°40 50 et — eee —— eed x Location of samples investigated Fi@. 1 It is concluded that the upper part of the Walloon Series in the northern Pane of Distribution of Sporomorphs Nimbin Bexhill Old Bonalbo Sphagnumsporites australis (Cook- son) Potonié Lycopodiumsporites dites Cookson Faveosporites canalis Balme Cicatricosisporites cooksonit Balme Gleichentidites cf. G. circinidites Cookson .. ‘ as a3 + Osmundacidites comaumenstis Cookson .. Dictyotosporites: complex ‘Cookson and Dettmann .. is Cingulatisporites floridus Balme .. Cingulatisporites pavadoxus Cook- son and Dettmann : Entylissa magna de Jersey : Araucariacites australis Cookson. . Inaperturopollenttes limbatus Balme Zonalapollenites dampiert Balme Zonalapollenites trilobatus Balme. . Zonalapollenites segmentatus Balme Perotrilites striatus Cookson and _ Dettmann Balmetsporites glenelgensis Cookson and Dettmann .. Punctatisporites minimus de Jersey eo ae austroclavati- +++ + ++ ae +++++4++ + + published before completion of work on) the remaining localities because ‘they may. have some bearing on the search for oil in this part oe Australia. | Sphagnumsporites australis (Cookstin) Potonié is one of the commoner types in the Tertiary’ lignites of the Kerguelen Archipelago (Cookson, 1947, p. 136) and occurs in the Comaum bore, South Australia (Cookson, 1953, | p. ' 463). According to Balme (1957, p. 16) Lycopodium- sporites austroclavatidites Cookson is common in the Upper Jurassic and Lower Cretaceous 176 of Western Australia. Cookson (1953, p. 469) described it from the Comaum bore, South Australia, and emphasized its affinities with Lycopodium ciavatum Knox. Balme (1957, p. 17) states that Faveosporites canalis Balme_ is common in the Donnybrook Sandstone at Murphy’s Shaft near Donnybrook in the Perth Basin, but only occasional specimens have been found elsewhere. Balme (1957, p. 19) described Cicatricosisporites cooksoni Balme from the Birdrong Formation, Carnarvon Basin, W.A., ? Neocomian—Lower Aptian. It is common in the Upper Jurassic and Lower Cretaceous of Western Australia and in the Albian of Queens- land. It ranges from Lower Callovian to Upper Albian. Gleichentidites cf. G. circinidites Cookson is similar to those described by Balme (1957, p. 23) from Upper Jurassic to Lower Cretaceous rocks from Western Australia, being characteristically smaller than Cookson’s species. Osmundacidites comaumensis Cookson is one of the commonest sporomorphs in the Comaum clays (Cookson, 1953, p. 471). In eastern Australia Dictyotosporites complex Cookson and Dettmann is restricted to Lower Cretaceous (Neocomian—Aptian) sediments (Cookson and Dettmann, 19580, p. 108) ; in Western Australia it occurs also in the uppermost Jurassic. Cookson and Dettmann (19580, p. 108) state: “ Perotri- lites striatus has a wide geographical distribution in the eastern Australian region but appears to have a restricted geological range. So far all the deposits in which it has been found are Lower Cretaceous and mostly Albian.’” Cookson and Dettmann (1958a, p. 43) described Balmei- sporites glenelgensis Cookson and Dettmann from between 6,485 and 6,487 feet in the Nelson bore, parish of Glenelg, Victoria ; according to Baker and Cookson (1955) these sediments are Upper Cretaceous. Cingulatisporites paradoxus Cookson and Dettmann is a useful index fossil, being restricted to sediments of Albian to Aptian age (Cookson and Dettmann, 1958), p.111). Balme (1957, p. 26) described Cingulati- sporites floridus Balme from the Strathalbyn Sandstone near Gingin, Perth, Western Australia. Entylissa magna de Jersey appears to be similar to that described by de Jersey (1960, p. 9) from the Rosewood coalfield of Queensland. Araucariacites australis Cookson is very common in material from the northern part of the Clarence Basin. Balme (1957, p. 31) records Inaperturopollenites limbatus Balme from the Perth Basin and states that it has not been found in any samples known with J. RADE certainty to be Jurassic. Zonalapollenites — dampiert Balme is important and common in the Mesozoic, e.g. Bajocian, Upper Jurassic and Lower Cretaceous, of Western Australia (Balme, 1957, p. 32). De Jersey (1960, p. 10) describes it from the Rosewood coalfield of Queensland, and it has also been found in the Eocene of the Perth area and in Aptian—Albian deposits in New Guinea. Zonalapollenites trilobatus Balme is confined to the Upper Jurassic and Lower Cretaceous. Zonalapollenites segmentatus Balme was very rare in the material examined. Balme (1957, p. 33) described it as fairly common in the Lower Jurassic Cockleshell Gully Sandstone of the Hill River—Jurien Bay area, Perth Basin, but very rare elsewhere. De Jersey (1960, p. 11) recorded it from the Rosewood coalfield, Queensland, which is thought to be Lower Jurassic. Of the 18 sporomorphs identified, 12 are of stratigraphic importance; eight of them occur in Upper Jurassic and Lower Cretaceous sedi- ments, and four are found only in the Lower Cretaceous. Of the latter the most important are Perotrilites striatus Cookson and Dettmann, which has a very limited time range, and Balmeisporites __glenelgensis Cookson and Dettmann, which was found in Upper Cretaceous sediments from the Nelson Bore in Victoria. This assemblage of sporomorphs makes it clear that the upper sediments (grey shales and coal seams) of the supposedly Jurassic Walloon Series are actually Lower Cretaceous. References BAKER, G., AND Cookson, I. C., 1955. ‘“‘ Age of the Nelson bore sediments’, Aust. J. Sci., 17, 133-4. BaLME, B. E., 1957. ‘‘ Spores and pollen grains from the Mesozoic of Western Australia ’’, C.S.I.R.O. Fuel Research Reference T.C. 25. Cooxson, I. C., 1947. ‘‘ Plant microfossils from the lignites of Kerguelen Archipelago’’, B.A.N.Z. Antarctic Research Expedition, 1929-1931, Reports—Series (A), Vol. II, Part 8, pp. 127-142. Cookson, I. C., 1953. ‘‘ Difference in microspore composition of some samples from a bore at Comaum, South Australia’’, Aust. J. Bot., 1, Nr. 3, pp. 462-473. Cookson, I. C., AND DETTMANN, M. E., 1958a. ““ Cretaceous ‘ megaspores ’ and a closely associated microspore from the Australian region ’”’, Micyro- palaeontology, 4, Nr. 1, pp. 39-49. Cooxson, I. C., AND DETTMANN, M. E., 1958b. ““ Some trilete spores from Upper Mesozoic deposits in the Eastern Australian region’’, Proc. Roy. Soc. Vic., N.S., 70, Part 2, pp. 95-128. Der JERSEY, N. J., 1960. ‘‘ Jurassic spores and pollen grains from the Rosewood coalfield ’’, Geol. Surv. Queensland Publ. Nr. 294. AUSTRALASIAN MEDICAL PUBLISHING CO. LTD. SEAMER AND ARUNDEL STS., GLEBE, SYDNEY ao = say te Wales originated in 1821 as the “PI ree Perey) ivity i SEN eae NOW! n unti | "im 1860, | a) H | | } “P Observatory during 1 x 962-63. K.P, Sims 183 New South Wales, | as a periodical . : PART 6A N OTICE ' To AUTHORS | General. to the Honorary Secretaries, Royal Society of New South Wales, 157 Gloucester Street, Sydney. Two copies of each manuscript are required : copy; together with two additional copies of the abstract typed on separate sheets. | Papers should be prepared according to the. They should be ‘as concise as possible, consistent with. - general style adopted in this Journal. adequate presentation. 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Observations were confined to those with southern declinations in the Ephemerides of Minor Planets published by the Institute of Theoretical Astronomy at Leningrad. On each plate two exposures, separated in declination by approximately 0’-5, were taken with an interval of about 20 minutes between them. The beginnings and endings of the exposures were automatically recorded on a chronograph by a contact on the shutter. Rectangular coordinates of both images of the minor planet and three reference stars were measured in direct and reversed positions of the plate on a long screw measuring machine. The usual three star dependence reduction retaining second order terms in the differences of the equatorial coordinates was used. Proper motions, the star positions to the epoch of the plate. Each exposure was reduced separately in order to provide a check by comparing the difference between the two positions with the motion derived from the ephemeris. The tabulated results are means of the two positions at the average time. No correction has been applied for aberration, light time or parallax but in Table I are given the factors which give the parallax correction when divided by the distance. The serial numbers follow on from those of a previous paper (Robertson, 1964). The observers named in Table II are W. H. Robertson (R), K. P. Sims (S) and H. W. Wood (W). The measurements were made by Mrs. J. Brannigan and Miss Y. Welch, who have also assisted in the computation. Reference ROBERTSON, W. H., 1964. J. Proc. Roy. Soc. N.S.W.., when they were available, were applied to bring 79, 33; Sydney Observatory Papers, 45. TABLE [ R.A. Dec. Parallax No. Planet (Ose (1950-0) (1950-0) Factors h m S 2 é ie S ” 1531 16 1963 Apr. 18-64290 15 10 38-62 —13 27 55-4 +0°:01 —3:0 1532 16 1963 May 14-64848 14 50 43-83 —ll 51 26-5 +0:03 —3-°3 1533 52 1963 Jul. 08:53582 17 31 41-79 —16 39 30-1 +0:06 —2:6 1534 58 1963 Jun. 18:-68086 19 35 52:32 —14 56 46-1 +0:07 —2:9 1535 58 1963 Jul. 23-55228 19 06 50:22 —16 23 14-1 +0:03 —2:-6 1536 64 1963 Jul. 08-56860 18 30 51-39 —24 14 48-6 +0:04 —1°5 1537 64 1963 Jul. 23-52145 18 18 11-06 —24 15 30:9 +0:04 —1:-5 1538 70 1963 Jul. 30-64293 21 30 20-35 —37 24 01-0 +0:08 +0°5 1539 70 1963 Sep. 05:°54574 20 59 03:88 —37 35 54-6 +0°18 +0-4 1540 84 1963 Jul. 31-62764 21 20 37-94 —21 35 54-7 +0:05 —1:9 1541 84 1963 Sep. 05-51426 20 47 39-10 —18 06 04-0 +0:07 —2:-4 1542 86 1963 Jul. 31-59408 20 13 21-38 —24 18 26:9 +0:09 —1-5 1543 116 1963 Aug. 19-69748 23 51 50-98 —06 14 52:5 +0:10 —4-1 1544 116 1963 Sep. 10-62032 23 36 38:28 —08 Ol 12-9 +0:08 —3:8 1545 116 1963 Oct. 10:-49042 23 14 15-54 —09 59 52-7 —0:02 —3:5 1546 129 1963 Oct. 23:+70347 03 31 58-60 +01 47 49-0 +0:19 —5-1 1547 129 1963 Nov. 04:57418 03 23 13-74 +00 56 16-6 —0°08 —5:-0 1548 133 1963 May 14-53447 14 27 52:52 —26 45 53-1 —0:02 —1:1 1549 148 1963 Nov. 12-53172 02 06 09-40 —27 56. 55-7 +0:02 —0-9 1550 148 1963 Nov. 21:50861 O22 OMT e252 74. —27 31 54-0 +0:03 —1:-0 1551 152 1963 Jul. 31-66076 22 06 58-89 —29 56 26-8 +0:06 —0-6 A cMmiTHSO NAR mT} 178 Planet 152 160 160 196 196 218 218 238 238 248 248 250 250 268 277 294. 294 317 317 326 326 350 350 357 357 364 368 369 369 369 388 388 412 412 412 438 438 446 446 451] 451 451 462 462 462 478 478 481 48] -487 487 494 494 518 518 519 519 519 530 530 535 535 540 540 578 1963 Sep. 1963 Jun. 1963 Jul. 1963 Jul. 1963 Jul. 1963 Oct. 1963 Oct. 1963 Jul. 1963 Jul. 1963 Jul. 1963 Jul. 1963 1963 1963 1963 1963 1963 1963 1963 1963 1963 1963 1963 1963 1963 1963 1963 1963 1963 1963 1963 1963 1963 1963 1963 1963 1963 1963 1963 1963 1963 1963 1963 1963 1963 : 1963 Jul. 1963 1963 1963 1963 1963 1963 1963 1963 1963 1963 1963 1963 1963 1963 1963 1963 1963 1963 1963 Sep. May Sep. Sep. Oct. Apr. May Jul. Oct. Oct: Oct: May May Oct; Oct. Jun. Jul. Oct. Oct. Sep. Oct. May Jun. Oct. Aug. Aug. Nov. Nov. Nov. -54270 -67790 -58635 -67049 *65325 *56205 -53213 -59400 - 36080 -62168 *55216 -65679 -59324 °57388 -59269 - 63803 *57832 - 64290 - 64848 -67017 *54394 -61574 *53857 *59931 -54807 -55123 -61303 *65963 -61795 -57927 -59740 -50368 - 60276 -58050 -54625 -63803 -57832 -61578 -46157 - 65963 -61795 *57927 -69748 -64883 -62032 -59400 -56080 -58955 -57396 -62168 -53078 -68401 -53564 - 66497 -58269 -61683 -61440 *54369 -62168 -55216 -56476 -54953 - 58608 -49209 -55770 W. H. ROBERTSON TABLE I—continued h 21 18 18 21 21 00 00 20 20 18 19 23 22 15 23 Ol 00 15 14 20 19 02 Ol Ol 00 R.A. (1950-0) m 33 55 34 30 25 27 23 19 13 36 18 04 46 O7 12 03 48 13 48 19 26 16 52 02 53 28 38 08 02 38 20 03 47 41 23 08 48 iS) HK NIRABDUIDMPRWOODAIDAWOAWRINMIWRTBRIUOCNDHE IDR OORUIDNWEHESCHUIREWOORRIUDOH OO Parallax Factors -12 —0O- ‘16 —0O- -12 —0O- -09 —l- ‘ll —l- °04 —4: ‘Ol —4: -00 —4: ‘02 —4:- -02 —2:- -00 —2: °07 —l- -ll —l- ‘10 —3- ‘09 —4: ‘Ol —4: 04 —4 00 —2 03 —3 30 +4 36 +4 03 —l1 00 —l1 08 —3 06 —2 05 —3 02 —2 06 —4 00 —4 09 —4 ll —O 02 —O0O 05 —3 05 —3 20 —3 00 —4 04 —4 ll —l1 06 —l1 06 —4 00 —4 08 —4 12 —4 04 —38 10 —3 Ol —4 Ol —4 04 —O 13 —0 Ol —2 Ol —l1 05 —1 07 —0O 00 —3 02 —3 07 +0 11 +0 ll +0 Ol —2 02 —2 00 —4 18 —4 02 —3 00 —3 02 —1 MINOR PLANETS OBSERVED AT SYDNEY OBSERVATORY DURING 1963 179 TABLE I—continued R.A. Dec. Parallax No. Planet Ulr. (1950-0) (1950-0) Factors nied ara Ss 2 t as Ss e 578 1963 Jun. 14-46157 14 57 14-60 —22 32 46-9 —0:05 —1-7 596 1963 Oct. 10-59931 Ol 04 36-39 —12 57 44:5 +0:08 —3:-1 596 1963 Oct. 24-54807 00 53 10-85 —13 11 03-2 +0:06 —3:1 600 1963 Aug. 27-62460 22 40 11-65 —13 20 21:8 +0-10 —3:1 600 1963 Sep. 18-54856 22 23 53-92 —16 09 10:1 +0:08 —2-7 602 1963 Jul. 25-65576 22 03 18°77 —19 03 33:8 —0:O01 —2-2 602 1963 Aug. 26:54363 21 33 04:81 —18 05 38-1 —0:02 —2-4 618 1963 Oct. 17-63038 02 09 59-09 —13 54 03-1 +0:09 —3:0 618 1963 Oct. 24-58948 02 04 36-00 —14 17 10-3 +0:04 —2:9 618 1963 Nov. 18:-58046 Ol 47 06-67 —14 05 58-9 +0:25 —3:2 636 1963 May 15-61578 15 38 00-91 —24 03 39°8 +0:10 —1-5 660 1963 Nov. 18-64941 05 10 11-97 +00 Ol 18-7 +0:04 —4-9 660 1963 Dec. 11-52454 04 49 32-26 —00 47 58:1 —O:ll —4:8 660 1963 Dec. 19-55658 04 42 15-15 —00 39 24-8 +0:07 —4:8 683 1963 May 22:-52936 14 26 10-68 —29 38 40-4 +0:04 —0°-6 686 1663 Jun. 19-66513 18 48 12-60 —06 58 27:8 +0:13 —4:0 686 1963 Jul. 22-52001 18 18 52-49 —O2 21 47-2 +0:03 —4:6 715 1963 Oct. 17-59361 O01 03 36-34 —05 20 19°7 +0:12 —4-2 718 1963 May 14-67934 17 09 20-30 —28 30 13:8 +0-10 —0:8 747 1963 Nov. 04-60744 04 02 29-30 —14 27 17°3 —0:07 —2-9 747 1963 Nov. 12-59467 03 57 15:88 —14 46 04-6 —0:03 —2-9 747 1963 Nov. —18-61226 03 52 45-56 —14 41 13-8 +0:09 —2-9 753 1963 Jun. 19-69724 19 29 50-04 —34 47 54:3 +0°17 0-0 153 1963 Jul. 09-62567 19 12 43-96 —38 11 01-9 +0:16 +0:5 712 1963 Jul. 30-69203 22 21 18:60 —52 40 03-2 +1-07 +2:-7 772 1963 Aug. 19-61329 21 59 57-88 —54 43 09-0 +0:13 +3:1 Ti2 1863 Sep. 10-53991 21. 36. 43°12 —54 31 11-2 +0:15 +3:0 779 1963 Apr. 17-55126 13 Ol 47-46 —29 59 42-7 —0:01 —0°6 808 1963 Apr. 18-64290 15 09 02-26 —12 58 30:4 +0:01 —3:1 868 1963 Aug. 15-66845 22 56 03-43 —13 03 48-5 +0:10 —3-1 868 1963 Aug. 27-62460 22 47 29°34 —14 30 34:3 +0:08 —2-9 868 1963 Sep. 09-58379 22 37 02-50 —15 58 31:0 +0:09 —2:7 898 1963 Jul. 02:-58464 18 29 24-83 —08 44 37°4 +0:03 —3:7 898 1963 Jul. 18-51162 18 21 03-97 —06 46 15:4 —0:04 —4:-0 909 1963 Oct. 16-60276 Ol 52 03-15 —12 13 48-7 +0:04 —3-2 909 1963 Oct. 23-58050 O01 47 31-21 —12 55 09:0 +0:04 —3:1 909 1963 Nov. 18-54625 Ol 32 59-92 —13 59 35-7 +0:18 —3:1 940 1963 Aug. 27-57726 21 48 13-71 —23 05 33:0 +0:06 —1:7 940 1963 Sep. 16-54469 21 36 05-99 —23 42 14-9 +0:16 —1:7 976 1963 Jun. 27-63298 18 59 24-09 —16 13 51:1 +0:08 —2:7 1021 1963 Nov. 18-64941 05 26 35-81 +01 19 49-3 0-00 —5-0 1021 1963 Dec. 20-50295 04 57 54-78 +05 06 24-4 —0:12 —5:5 1048 1963 Jul. 11-60722 19 53 53-52 —44 17 07:3 0-00 +1:°6 1048 1963 Jul. 15-62022 19 49 23-26 —44 41 24-5 +0:12 +1:6 1048 1963 Jul. 30-53813 19 33 05-67 —45 27 38-7 —0:01 +1:8 1089 1963 Sep. 18-63356 00 18 49-55 —05 27 33-7 +0:10 —4:-2 1089 1963 Oct. 09-53932 23 58 47-12 —0O7 10 53:8 +0°03 —3:-9 1248 1963 Jul. 16-64494 21 06 52-05 —27 09 14-0 0-00 —1:-0 1278 1963 Jul. 11-65079 20 49 56-31 —28 48 49:8 +0:02 —0:8 1278 1963 Jul. 22-63298 20 44 19-42 —31 26 12:7 +0:07 —0-4 1278 1963 Jul. 30-60879 20 38 40-79 —33 11 45:5 +0:08 —O-1 1407 1963 Jul. 22-59520 20 10 15-72 —14 47 05-1 +0:02 —2:-9 1418 1963 May 22-62208 16 37 09°13 —35 41 06:°6 +0:05 +0:°:3 1418 1963 Jun. 19-56017 16 04 26:53 —35 15 19°-8 +0:19 0-0 1467 1963 Jul. 22-67049 21 30 03:37 —25 21 08:1 +0:09 —1-4 1467 1963 Jul. 29-65325 21 23 25-50 —25 O7 21-7 +0-11 —1-4 1514 1963 Aug. 15:63275 21 57 53-89 —12 10 0O1°3 +0:11 —3:3 1580 1963 May 20:69226 18 12 28:46 —34 59 00°3 +0:05 +0:2 1580 1963 May 23:-66113 17 44 22-16 —50 35 51-9 +0:05 +2:°5 1606 1963 Jun. 19:61573 M37 ° 22278 —09 26 53-0 +0:13 —3:7 180 W. H. ROBERTSON TABLE IT No. Comparison Stars Dependences 1531 Yale 11 5299, 5334, 5335 0-40001 0-33110 0- 26889 1532 Yale 11 5211, 5215, 5226 0-37569 0-37106 0- 25325 1533 Yale 12 I 6293, 6300, 6328 0- 34678 0-40181 0- 25141 1534 Yale 12 I 7359, 7374, 7390 0-29112 0-47266 0+ 23623 1535 Yale 12 I 7093, 7108, 7116 0- 25172 0:37211 0-37617 1536 Yale 14 12847, 12865, 12905 0- 28169 0-36162 0- 35669 1537 Yale 14 12669, 12708, 12723 0-18319 0-54816 0- 26865 1538 Cape 18 11082, 11094, 11108 0-33768 0: 43049 0- 23183 1539 Cape 18 10847, 10866, 10893 0-32755 0- 36256 0-30990 1540 Yale 13 I 9145, 9170, 14 14747 0-33754 0-36852 0- 29394 1541 Yale 12 II 8916, 8937, 8944 0: 15257 0-45781 0-38963 1542 Yale 14 14062, 14070, 14092 0: 42335 0- 28355 0- 29310 1543 Yale 16 8420, 8427, 8428 —0-03102 0: 78348 0- 24754 1544 Yale 16 8350, 8364, 8368 0- 12684 0-54986 0: 32330 1545 Yale 11 8149, 8150, 8165 0-19146 0:62712 0-18142 1546 Yale 20 1018, 1026, 1037 0-33953 0-41206 0+ 24842 1547 Yale 21 729, 741, 744 0-38201 0-45631 0: 16168 1548 Yale J4£ 10440, 10462, 10488 0-32552 0- 30386 0-37062 1549 Yale 13 II 800, 814, 819 0-41880 0- 23698 0- 34422 1550 Yale 13 II 748, 770, 800 0: 27678 0-46370 0- 25953 1551 Cape 17 12024, 12059, Yale 13 II 14407 0- 24808 0-37151 0-38041 1552 Capes T7 Aiiai. igo: lis6 0-38416 0- 34447 0-27137 1553 Yale 13 II 12379, 12391, 12404 0-46542 0- 22236 0-31222 1554 Yale 13 II 12072, 12090, 12112 0- 13223 0-57883 0- 28894 1555 Yale 14 14804, 14808, 14838 0+ 22437 0-45262 0-32302 1556 Yale 14 14770, 14774, 14798 0-53176 0- 29128 0-17696 1557 Yale 17,99) 027 112 046337 0: 14133 0-39530 1558 Yale 16 71, 87,717 83 0- 36334 0-38075 0- 25591 1559 Yale ly ZOlS 021036 0- 08896 0: 43856 0-47248 1560 Yale 17 6957, 6975, 6986 0- 23634 0- 30032 0: 46234 1561 Yale, 12 1 7363, 7366; 7392 0-17517 0-31156 0-51327 1562 Waleql2 Wi 21,1236, 1253 0- 36495 0- 38680 0- 24826 1563 Yale 13 I 9707, 9723, 14 15547 0- 28538 0-35183 0-36279 1564 Yale 14 15377, 15390, 15406 0-40346 0- 25033 0- 34622 1565 Yale 11 5288, 5299, 5317 0- 19462 0-42212 0- 38326 1566 Yale 17 7993, 8010, 8020 0- 36769 0- 18014 0-45217 1567 Yale 17 234, 248, 21 214 0- 39607 0- 36057 0- 24336 1568 Malem ili. sia 0-32015 0-11286 0- 56699 1569 Yale 12 I 5611, 5612, 5623 0-48277 0- 25136 0- 26586 1570 Yale 11 5197, 5208, 5216 0- 28002 0- 35862 0-36135 1571 LP1l D 4024, 4034, 4044 0: 27474 0: 48957 0: 23569 1571 Cape 20 5844, 5910 LPI C 3896 0- 20236 0-33792 0-45973 1573 Yale 14 1047, 1068, 1072 0-39267 0- 29122 0-31611 1574 Yale 14 878, 880, 900 0-54888 0- 15328 0- 29784 1575 Yale 77 206) 216; 72 10 270 0-33481 0- 26938 0-39581 1576 Wale a2) 1252325236 0-31156 0-38858 0- 29986 1577 Yale 11 5407, 5432, 16 5413 0-42428 0-33705 0- 23867 1578 Yale 12 II 6812, 12 I 5995, 6009 0-40889 0-30200 0-28911 1579 Yale 21 660, 675, 678 0- 27157 0-31265 0-41579 1580 Yale 21 648, 656 17 743 0- 33360 0- 40802 0- 25838 1581 Yale 21 540, 546, 550 0-18776 0-31886 0-49338 1582 Cape 17 9166, 9201, 9210 0-47675 0-33005 0- 19321 1583 Cape 17 8963, 8982, 9007 0- 24689 0- 26840 0-48471 1584 Yale 11 399, 413, 428 0-51769 0-31540 0- 16691 1585 Yale 11 378, 389, 394 0-38024 0-32901 0- 29075 1586 Yale 11 294, 302, 307 0- 23089 0-44425 0- 32486 1587 Yaler 21, 214, 223) 225 0- 16884 0-51965 0-31151 1588 Valeri 7 69 Lol eo 2 0-33430 0-33522 0-33049 1589 Yale 14 11023, 11031, 11040 0-33178 0- 23625 0-43197 1590 Yale 14 10787, 10801, 10816 0-14315 0-32694 0-52991 1591 Yale 21 660, 675, 678 0- 19637 0-57864 0- 22500 1592 Yale 21 6438, 656, 17 743 0- 17867 0- 30936 0-51197 1593 Yale 17 651, 667 21 560 0- 29965 0-32209 0-37826 1594 Yale 16 8381, 8388, 8395 0-32858 0-49586 0-17555 1595 Yale 16 8350, 8362, 8376 0-10911 0- 29205 0-59884 1596 Yale 16 8322, 8328, 8338 0-34781 Q- 27825 0-37394 1597 Yale 2/7 5114, 5134, 5139 0- 26064 0- 26499 0-47438 PRAMAS EOAAAAASEVSSASO OM SAAAV SAAAAAY SEM M SMO MAY SS SSS MA Sse sgvragregraerssnn MINOR PLANETS OBSERVED AT SYDNEY OBSERVATORY DURING 1963 TABLE II]—continued Yale Cape Cape Yale Yale Yale Yale Yale Yale Cape Cape Cape Yale Yale Yale Yale Yale Yale Yale Yale Yale Yale Yale Yale Yale Yale Yale Yale Yale Yale Yale Yale Yale Yale Yale Yale Yale Yale Yale Yale Yale Cape Cape Cape Cape Cape Yale Yale Yale Yale Yale Yale Yale Yale Yale Yale Yale Yale Yale Yale Yale Cape Cord. Cord. Yale Yale Yale Comparison Stars 5077, 5094, 5099 10718, 10759, 10765 10632, 10642, 10660 II 8450, 8481, 13 I 8457 13437, 13481, 13485 14731, 14772, 13 II 14065 II 13671, 13676, 13718 6136, 12 I 6495, 6518 6049, 6056, 6066 10680, 107138, 10715 10668, 10676, 10697 10494, 10527, 10529 I 7398, 7426, 7433 II 8311, 8347, 8358 276, 280, 289 196, 206, 228 5530, 5545, 5546 5441, 5443, 5461 10879, 10891, 10913 10726, 10748 13 I 6222 216, 228, 236 173, 183, 188 7983, 8010 12 I 8446 I 8358, 8372, 8384 II 9401, 9413, 9415 II 9226, 9256, 9257 495, 12 I 571, 576 I 535, 549, 564 I 443, 445, 473 11061, 11084, 11102 1225, 1240, 1247 1095, 1123, 1125 1067, 1069, 1075 II 9130, 9139, 9156 6371, 6379, 6404 6131, 6136, 6155 213, 17 242, 260 II 10850, 10874, 10881 I 1069, 1081, 1088 I 1045, 1056, 1082 I 1024, 1031, 1045 10110, 17 10648, 10686 9970, 9982, 10008 8716, 8717, 8727 8572, 8614, 8632 8420, 8430, 8470 II 8329, 8337, 8358 5299, 5320, 5335 8063, 8066, 8075 I 8458, 8472, 8485 I 8422, 8427, 8439 6204, 6210, 6220 6157, 6172, 6190 424, 428, 436 400, 408, 423 I 380, 401, 11 344 14922, 14952, 14977 14855, 14862, 14878 I 7020, 7045, 7057 1743, 1754, 1773 1500, 1550 22 1923 14477, 14496, 14529 14327, 14360, 14394 60, 74 16 69 8442, 8449, 8461 II 13903, 13922, 13945 . 18889 Cape Z. 18502, 18511 ororemoooooooooooorcoorocroooqooocoqocooeocoqoooqoooqooorvcocoocooooooqorowocoeoqcococmccooocmcCcooeocmcOCcocoo oo Sm - 14008 - 22906 * 35928 18228 29574 » 28346 28946 31318 27552 -25718 46641 24223 43423 -27218 -44519 -40001 -28878 °25211 29751 -33502 -47965 -34197 23610 * 24741 -62780 -51742 16337 - 36063 -30068 -23797 - 32680 -45704 -46816 *42531 -35620 * 26639 -41468 -31846 - 13660 - 22182 -07787 -30063 - 29427 -41056 -53728 -36910 - 35268 -55296 -38965 21698 -30132 - 16034 *38647 * 29577 -37993 - 23682 -39726 - 27764 -31955 - 29448 *30255 -17748 -11320 - 25019 -40621 - 15473 -37140 Dependences - 38665 - 28416 -51486 *35789 32346 27564 29339 30804 52141 -33882 - 26656 - 22136 -36254 *37517 - 20413 - 36843 -53781 26964 -49760 27857 31638 - 19630 -46616 - 28146 » 22863 -19998 *31347 - 38606 -30575 - 37292 °43127 *33339 -23977 * 24377 -30670 -40839 - 26299 -19220 -31370 -52708 -59618 °48261 - 25939 - 23991 - 30986 -33767 - 26522 - 20671 *32155 * 24637 - 23033 -53368 » 25380 - 36926 - 28617 *47115 -13071 *45316 -31557 °47337 -31301 -59130 °44595 -31670 - 26474 °44300 - 39249 Qo eS Seo eS Se SSS SS SSS So SS SSI SI SS SIS OS SS SoS SS & oS Sona Oo SS oS SS SS SSS SS SSS SS SS = °47326 -48679 *12585 °45983 - 38080 44090 41716 -37878 - 20306 -40400 - 26702 *53641 - 20323 -35265 * 35067 *23155 -17340 °47825 - 20489 - 38640 - 20397 -46173 - 29774 -47113 - 14358 - 28260 -52316 - 25331 *39357 -38910 - 24193 - 20956 - 29208 * 33092 -33710 * 32522 -32233 -48933 -54969 -25110 -32595 - 21676 *44634 - 34953 - 15287 - 29323 - 38209 » 24033 - 28880 -53664 -46835 -30598 *39973 *33497 *33390 - 29203 -47203 » 26920 - 36488 *23215 -38444 * 23122 -44086 -43310 -32905 *40227 - 23612 Wind dN did dO donde ddd sO MBO EO dH ds sO DOWD dO dU DUN EEN done eNews 181 182 Yale Cape Cape Yale Cape Cape Yale Yale Yale Cape Cape Yale 13 D7. 17 L2 18 18 14 14 11 Hird Ft. 16 W. H. ROBERTSON TABLE [I—continued Comparison Stars II 13728, 13741, 13765 11332, 11337, 11369 11265, 11301, 11315 I 7570, 7584, 7609 8223, 8235, 8257 i979, SOM 17 8501 14799, 14818, 14830 14745, 14770, 14774 TEMES Ties facie 9777, 9829, 18 9363 17253, 17280, 17391 5956, 5968, 5974 =~ SS - 15823 ‘40773 -28175 » 27535 -40395 -39186 *31873 -39302 - 34498 -44339 -18512 » 29850 Dependences SQ cqooooocos cS -58039 - 36344 -37144 - 30342 - 06982 - 28734 - 16557 *32255 -31827 - 26027 -43616 - 18298 (Received 11 May, 1964) - 26138 22884 -34681 -42123 - 52623 -32080 -51570 » 28444 - 33676 - 29633 -37872 *51852 SOT i See Journal. and Proceedings, Royal Society of New South Wales, Vol. 97, pp. 183-184, 1964 Occultations Observed at Sydney Observatory during 1962-63 K. P. Sims The following observations of occultations were made at Sydney Observatory with the 114-inch telescope. A tapping key was used to record the times on a chronograph. The reduction elements were computed by the method given in the occultation Supplement to the Nautical Almanac for 1938 and the reduction completed by the method given there. For 1962 a correction of +0-00944 hour (=34 seconds) was applied to the observed time to convert it to Ephemeris Time with which The Astronomical Ephemeris for 1962 was entered to obtain the position and parallax of the Moon. For 1963 a correction of +0-00972 hour (=35 seconds) was applied to the observed time to convert it to Ephemeris Time with which The Astronomical Ephemeris for 1963 was entered to obtain the position and parallax of the Moon. The apparent places of the stars of the 1962-63 occultations were provided by H.M. Nautical Almanac Office. Table I gives the observational material. The serial numbers follow on from those of the previous report (Sims, 1963). The observers were W. H. Robertson (R), K. P. Sims (S), and H. W. Wood (W). In all cases the phase observed was disappearance at the dark limb. Table II gives the results of the reductions which were carried out in duplicate. The Z.C. numbers given are those of the Catalog of 3539 Zodiacal Stars for the Equinox 1950-0 (Robertson, 1940). References ROBERTSON, A. J., 1940. Astronomical Papers of the American Ephemeris, Vol. X, Part II. Je Proc. Roy, Soc. N.S.W., 96, 37; Svdney Observatory Papers, 44. Sims, K. P., 1963. TABLE | Serial Vid OF No. No. Mag. Date Ue: Observer 425 1362 7°4 1962 Jun. 7 9 39 27-2 W 426 2219 6-2 1962 Jul. 13 9 57 59-0 5 427 2240 6°8 1962 Aug. 9 12 58 59-0 R 428 2760 6-7 1962 Sep. 9 174 3321 WwW 429 2908 6:9 1962 Sep. 10 1] 23 47-0 S 430 2994 6-1 1962 Oct. 8 10 28 02:4 R 431 3091 6-9 1962 Nov. 5 1] 14 14-6 R 432 3245 6-9 1962 Nov. 6 12 26 57°5 S 433 847 3°0 1963 Feb. 4 9 40 44-5 R 434 1021 6°3 1963 Feb. 5 11 37 11-6 W 435 1295 6°5 1963 Apr. 30 10 34 49-1 R 436 1296 6:5 1963 Apr. 30 10 42 34-0 R 437 2184 7:0 1963 Jul. 2 12 00 44-2 S 438 2436 6°3 1963 Jul. 4 13 30 14°3 S 439 Zoe 5:6 1963 Jul. 29 9 07 16-5 Ss 440 2245 6-4 1963 Jul. 30 8 38 56-8 R 441 3171 3°8 1963 Sep. 2 8 43 17°8 R 442 3190 3°0 1963 Sep. 2 13 01 28-9 S) 443 2291 55 1963 Sep. 23 10 42 34-2 R 444 2838 5:6 1963 Sep. 27 10 11 09-8 R 445 2964 6-6 1963 Sep. 28 8 41 45-8 W 446 3113 5:4 1963 Sep. 29 10 09 58-7 W 447 2785 6-8 1963 Oct. 24 9 35 43-1 W 448 3069 6-2 1963 Oct. 26 12 18 09-5 W 184 Keres Sins TABLE II Serial Luna- Coefficient of No. tion Pp q Dp pq ae Ac pAs qAs Aa Ad 425 488 +55 +84 30 +46 70 —1:8 —1-0 —1-5 +10-1 +0:71 426 489 +44 +90 19 +40 81 —1-7 —O0°-7 —1:5 + 9:3 +0:76 427 490 +51 +86 26 +44 74 —1-9 —1-0 —1-6 +10°3 +0-70 428 491 +65 —76 42 —49 58 —0-l —0-l +0-1 + 9-4 —0:75 429 491 +84 +55 70 +46 30 +0-2 +0:2 +0:1 +11-0 +0:63 430 492 +98 —20 96 —20 4. —3°8 —3-°-7 +0:8 +14-] —0:05 431 493 +31 +95 10 +29 90 —0:9 —0:3 —0:9 + 1-4 +0-99 432 493 +86 — 52 13 —44 DIE +0:8 +0:7 —0-4 +14-1 —0:26 433 496 +92 +39 5 +36 15 —1:°3 —1-2 —0°5 +12-1 +0-50 434 496 +100 + 100 +. ] 0 —1:-7 —1-7 0-0 +13-9 +0:04 435 499 +73 —68 53 —50 47 +0°3 +0:-2 —0Q-2 + 8:5 —0:80 436 499 + 64 el, 41 —49 59 +0:3 +0:2 —0:2 + 7-0 —0:87 437 501 +85 +53 Phy +45 28 —1-9 —1-6 —1-0 +14-] +0:-25 438 501 Serf —70 51 —50 49 —1-3 —0-9 +0°9 + 8:0 —0:82 439 502 +92 +39 85 +36 15 —0:9 —0:8 —0-4 +14-6 +0:-:07 440 502 +100 + 8 99 + 8 1 —0-6 —0-6 0-0 414-2 —0-20 441 503 +97 —23 95 —22 5 —4:-0 —3-9 +0:9 +14°3 +0:02 442 503 +99 —17 97 —17 3 —2-8 —2-8 +0-5 +14:3 +0-09 443 504 +89 +45 80 +40 20 —1:8 —1-6 —0:8 +14-] +0-20 444 504 +77 +64 59 +49 41 —]-7 —1:3 —l-l +10:2 +0-68 445 504 +38 —93 14 —35 86 —0:9 —0:3 +0:8 +7 0 —0:87 446 504 +98 +18 97 +18 3 —1:-0 —1-0 —0-2 +13-1 +0-40 447 505 +83 —56 69 —46 Bl —0-2 —Q-2 +0°1 +11-8 —0°53 448 505 +99 —13 98 —13 2, —]+4. —]-4 +0-2 +14-1 +0-:08 Journal and Proceedings, Royal Society of New South Wales, Vol. 97, pp. 185-191, 1964 James Dwight Dana in New South Wales, 1839-1840 ANN MOZLEY Basser Library, Australian Academy of Science, and Dept. of History, Research School of Social Sciences, Australian National University, Canberra ‘A sandstone bluff, from one hundred and fifty to two hundred feet in height, forms the North and South Heads of Port Jackson. The rock lies in nearly horizontal beds, brought out in bold relief by the partial removal of occasional softer beds, or by natural excavations along the junction of the several layers. Passing the narrow entrance between the capes, the same light gray or grayish-yellow sandstone is seen bordering the bay throughout its extent, stretching far away around its deep sinuous coves, and advancing into prominent head- lands that often confine the view to a small portion of this large expanse of waters. The sandstone usually presents a low bluff front to the bay: the upper layers retreat either by terraces or a gradual slope, into rounded elevations covered with a sparse growth of shrubbery or forest trees. These slopes continue in many places to the water’s edge, especially at the head of the coves, where they terminate below in a broad sand-beach, or a small marsh, more or less changed to meadow-land by washings from the adjoining declivities.”” (Dana, 1849, p. 449.) In these terms, James Dwight Dana described Sydney Harbour, which he entered aboard the U.S. man-of-war Peacock on 29 November 1839. Dana was then twenty-six, and destined within the decade to succeed Benjamin Silliman as Professor of Natural History at Yale and to become for the next half century the dominating figure of American geological science. Dana had already demonstrated his great ability as a mineralogist before he arrived in Australia in 1839. He had studied geology and mineralogy under Silliman at Yale, but the opportunity of foreign travel prompted him to abandon his studies before graduation in 1833 and to take the post of mathematical instructor on the Mediterranean cruise of S.S. Delaware. It was not, however, mathematics but geology that stimulated his perceptive mind, and Dana’s description of a visit to Vesuvius posted to Silliman from abroad, won him a_ personal assistantship to the Professor on his return in 1836. Two years later he published A System of Mineralogy, widely regarded as his most original work, and a classic of mineralogy. It was Asa Gray, Professor of Botany at Harvard, who persuaded Dana to join the United States Exploring Expedition as geologist and mineralogist in 1838. Commissioned under Captain Charles Wilkes, the Expedition was the first hydrographic and scientific survey to be undertaken by the United States Government in the international sphere, and had as its object the exploration and survey of the Antarctic coastline, the Pacific Islands and the north-west American coast, and the preparation of scientific reports. Its carefully selected corps of civilian scientists included, in addition to Dana, two men of considerable reputation in their fields, Horatio Hale, the philologist, and Dr. Charles Pickering, chief zoologist to the Expedition and a former Curator of the Academy of Natural Sciences. The six vessels sailed from Norfolk, Virginia, in August 1838, and after a sixteen months’ cruise of South American waters and the Pacific, the flagship Vincennes and the sloop-of-war Peacock carrying the scientific contingent arrived off Port Jackson on 29 November 1839 at 8 p.m. Their arrival was unexpected, and no pilot met them at the entrance of Sydney Heads, but Wilkes was anxious to avoid loss of time and to catch the favourable wind. Thus on a dark night, unknown to the harbour authorities and relying on their own charts to negotiate the channel, the two ships stole silently into harbour and at 10.30 p.m. “ quietly dropped anchor off the Cove, in the midst of the shipping, without anyone having the least idea of our arrival”’ (Wilkes, 1852, p. 208). When the people of Sydney looked abroad the following morning, they were astonished to see two men-of-war anchored among their shipping directly below the Fort. ‘“‘ What a scrape should we have been in’’, exclaimed one citizen in his diary, “had there been war’”’ (Clarke, Diary, entry 4 Dec. 1839). 186 Despite their unorthodox arrival, the residents greeted the Squadron with hospitality and enthusiasm. There was much in the Colony that reminded the visitors of home: “ The acquisition of wealth ’’, Captain Wilkes noted, “seems the only object of exertion here, and speculation was as rife as we had left it in the United States * (Wilkes, 1852,\p; (211), she officers observed the arrival of a convict ship and were struck by the healthy aspect of the disembarking passengers. ‘“‘ They were treated in all respects ’’, Wilkes recorded in some wonder, vast they were free” (p,.277). Dana did not remain long in the town and the day after their arrival accepted the invitation with Dr. Charles Pickering, to visit the estate of W. Stephens at Puenbuen, some 120 miles from Newcastle near the source of the Hunter River (Pickering, 1850). The two scientists travelled by steamer to Newcastle and thence overland up the Hunter Valley through Maitland, Patrick Plains and Muswellbrook to Stephens’ station, and it was here that Dana began his careful examination of the Australian landscape and, in his own words, sought “ to gratify but partially, in a geological point of view the curiosity which so strange a land may well excite (Dana, 1849, p. 458). To the small coterie of scholars and scientific amateurs in the Colony, cut off from the currents of discovery and research, the advent of the civilian corps of the United States Exploring Expedition offered the stimulating opportunity for discussion and scientific exchange. “I wish I could meet with Mr. Dana ’’, the Rev. W. B. Clarke wrote in his diary on December 16th. Next morning, the Expedition’s Chaplain introduced him to the geologist, back that day from the country, on board the Peacock. William Branwhite Clarke was a graduate of Cambridge, where he had studied geology under Professor Adam Sedgwick, and was already known in geological circles in London when poverty and long delay in Church preferment drove him to accept a parish in New South Wales. He had arrived in the Colony in May 1839 with the eager recommendations of his colleagues of the Geological Society of London to turn his particular attention to the coal deposits of Australia and to investigate the stratigraphy of this little known land. With the exception of Charles Darwin, who called briefly aboard the Beagle in 1836, Clarke was the first university trained geologist to reach Australia, where his pioneering work over vast tracts of New South Wales was to earn him the title of the “Father of Australian Geology” and a ANN MOZLEY Fellowship of the Royal Society towards the — close of a long and energetic life. His meeting with Dana who, while fifteen years his junior, had already demonstrated the quality and originality of his mind, gave an exhilarating start to Clarke’s geological researches in the Colony and was the beginning of a long friendship maintained by corres- pondence until the end of the clergyman’s life. It is indeed Clarke’s diary, which he kept faithfully during his first two years in Australia and into which he poured his graphic impressions of Colonial life, that provides the main source of information of Dana’s now forgotten visit to New South Wales. Three days after their first meeting Dana and Clarke were together again at the elaborate luncheon given by the United States Squadron on the lawns at Fort Macquarie, where, under marquees decked with flags and evergreens, they met another scientific visitor, the Polish Count Strzelecki, who arriving in the Colony in April 1839 with the avowed intention of con- ducting a mineralogical survey of New South Wales, had just returned from an excursion across the Blue Mountains to Bathurst and told Clarke and Dana that he had found “ the geology of that country very tame” (Clarke, Diary, 20 Dec. 1839). It was a verdict the clergyman was to remember with interest when Strzelecki asserted his claim to have discovered gold in the region, as the rushes of 1851 pre- cipitated a lively scramble for priorities in the early discovery of Australian gold. Clarke’s own interest was more than academic; he too had found traces of gold in the mountains in 1841. It was also in Clarke’s company that Dana visited the house of Mr. (later Sir Charles) Nicholson where, Clarke enthusiastically reported, ‘‘ Dana and I went all over the geology of America and Europe ”’ (Diary, 23 Dec. 1839). From there they drove to Elizabeth Bay to — call on W. S. Macleay. “ The ride from Sydney to South Head ”’, Dana wrote later (0p. cra p. 450), ““. . . may be recommended as offering strong attraction to the lover of the beautiful in nature, especially as the noble bay throws its own life into many of the fine views”. Alexander Macleay’s home,. set in its spacious garden of rare shrubs and creepers, flowers and imported trees, afforded delight to many visiting scientists to New South Wales. Yet, from their own records, it appears that the geologists found keener satisfaction in the coal traces they identified in the rocks behind the garden and in the ripples of sand shale on the shore JAMES DWIGHT DANA IN NEW SOUTH WALES, 1839-1840 than in the botanist’s paradise of the home at Elizabeth Bay (Clarke, Diary, 23 Dec. 1839 ; Dana, 1849, p. 461). On Boxing Day, the ships of the United States Exploring Expedition weighed anchor and stood to sea to begin their cruise of the Antarctic. James Dana, however, with other members of the scientific corps, remained behind, and it was during these next two months of leisure in the Colony that his major geological work was done. At the beginning of the New Year, he travelled to Wollongong by steamer with the Expedition’s artist, Mr. Drayton, and here on 2nd January Clarke joined them, riding overland from his rectory at Parramatta in anticipation of meeting his friends. During the several days the two geologists spent in Wollongong, they closely examined the coastline, where they found fossils of shells and wood in abundance in the argillaceous sandstone cliff; they found also a raised beach in which they marked Tvochus austvauis. On their last evening they were invited to attend a corroboree of tribes drawn from as far afield as Moreton Bay, and Clarke in his Diary records his “feelings of wild sublimity as firé after fire blazed up and I found myself among at least one hundred native savages in a state of perfect nudity and looking most unearthly ”’ (Clarke, Diary, 6 Jan. 1840). Next day they were on their way to Kangaroo Valley in the company of a guide. Clarke has left a lively record of this excursion on horseback through the fertile valleys and steep defiles, where the richness of the forest made “a sort of moonlight ”’ and the shadowy groves offered a cool retreat from the midsummer heat. “ This bush riding has quite an air of romance about it’ he recounts in his Diary (7 January 1840). You gallop along over a green but not level turf, studded with splendid trees through which you wind your way... Suddenly you come upon some dry water course with lofty banks, the bed of which is strewn with large fragments of rocks over which and through which one must ride. . . Then, again, you cross rivers full of water, gliding along under a canopy of branches and having a thick jungle of ferns upon their edges, affording spots of most cooling aspect amidst the sultry heat of a noon- day. ..Occasionally we had to leap innumerable trees fallen across [the route] so that the ride had more of the character of a steeple chase than anything else and frequently recalled to my mind our boyish game of “follow the leader”’ as we saw 187 the stockman guide cantering along in the van without slackening his speed, over this, through stumps, suddenly disappearing down a steep hump and then suddenly rising again up the opposite bank. In this fashion they crossed the Macquarie River and ascended the rapidly rising slope of Illawarra mountain to the vertical wall of rock which topped its last three hundred feet. Here, clambering “‘on all fours sometimes, dragging our horses after us, we gained the summit, where we had a splendid view of the lake and sea and mountains and the deep defiles with thick forests which we had passed. Just at the summit we passed a trap dyke ” (Clarke, Diary, 6 Jan. 1840). By nightfall, they had made the zigzag descent into Kangaroo Valley which Dana characterized as “‘a narrow patch of land. . . scarcely averaging three miles in breadth, lying between abrupt mountain walls, from one thousand to eighteen hundred feet in height ’’ (Dana, 1849, p. 452). Dana, Clarke reported, thought the sea had occupied the valley “as a gulph”’ but he had abandoned this false deduction when he came to write up his Report on the Geology of New South Wales. Clarke’s own opinion was that it had recently been a fresh water lake from which the barriers had been burst. In Kangaroo Valley the travellers were received hospitably at Mr. Meare’s station where, reassured by the comfort of a great log fire, they slept soundly after their long ride. Neither mosquitoes nor bugs, Clarke was happy to report, troubled their repose; ‘“‘a few fleas only danced a welcome to the Kangaroo Grounds ”’. During the next days, Dana and Clarke were engaged in an intensive exploratory investi- gation—the first to be undertaken in any detail—of the Illawarra region from Broughton’s Head to Coolangatta Mountain and along the coast to Black Head and Kiama ; a spectacular area of basalt interstratified with the sandstone and cutting the shoreline in deep, intersecting dykes. At Broughton’s Head they came upon the «trap, the very rock’, wrote Clarke, “we had been in search of ’’, and they were to trace its outcrop in the Coolangatta Mountain down to a deep dyke running through the beach at Black Head. The two men _ evidently differed in their opinion of “trap”. Clarke reports an argument with Dana over a particu- larly hard specimen found at the river mouth at Black Head “ but we at last agreed that it was true trap’’. Dana wrote later, “It is doubtful whether the igneous rocks under 188 consideration are wholly basalt, or are in part trap, that is, whether they always contain augite with the feldspar or sometimes hornblende. Some ambiguous rocks may be referred to either variety’ (1849, p. 497). He himself adopts basalt throughout his Report. At Black Head they came upon the rich fossil beds of shells and wood which they had met earlier at Wollongong. “Our surprise was great ’’, Clarke noted, “‘ to find the whole of the low cliff which forms Black Head and the flat rocks below filled out with innumerable con- cretions as at Wollongong, shells and corralines and with masses of granitic and porphyritic rock embedded and divided by iron seams in every direction. Many of the shells were completely agatered.’”” Here too they found a fossil tree, whose exposed part measured three feet long by seven inches wide. Although many had seen the Blow Hole at Kiama by 1839, Dana and Clarke were the first to observe and record this phenomenon in geological terms (Clarke’s long diary entry is recorded by Jervis, 1945, p. 34). Both men sketched the columnar basalt rising in beautiful order from the sea (Dana’s elegant sketch is reproduced in his Report), and both pronounced it the very Staffa of New South Wales. The wildness of the coastal scenery where the sea hollowed out the basalt flows and dykes and hammered noisily against the narrow channels it had carved clearly attracted the two men and Dana writes evocatively of a dark cavern, eight or ten feet high, [which] extends into the cliff a hundred yards or more. The sea dashes in below and may be heard hurrying on, for a while becoming nearly still—when suddenly a sound like thunder roars through the cavern as the water strikes the farther walls, and a few rays of light are seen amid the darkness, sparkling from scattered foam (Dana, 1849, p. 496). At Kiama the two geologists parted ; Clarke to find his way overland through the Illawarra Mountain back to Parramatta; Dana to travel a short distance south, returning along the coast to Bulli and Mount “‘ Keerah ’’, where he examined the coal measures before turning inland to complete his homeward journey by way of Appin and Campbelltown. On 16 January he reached Clarke’s home at Parramatta and the following day rode out with his friend to inspect the Prospect intrusion. It was Clarke’s last Diary entry about the American. “Mr, Dana and i erode toi erospectaan. ANN MOZLEY Examined the basalt and traced a dyke of — syenite, black and hard all along the ridge’”’ (Clarke, Diary, 17 Jan. 1840; cf. Dana, 1849, p. 516). From his own evidence, Dana appears to have spent the remainder of his stay in the Colony in the Hunter River District»in a meticulous investigation of the coal deposits at Nobby Island and Telegraph Hill, and at Lake Macquarie. From James Steel, Super- intendent of the Coal Works at Newcastle, he received substantial help, and he made the acquaintance of the Rev. C. P. Wilton, one of the early promoters of Australian science. Wilton was the founder and energetic president of the Newcastle Mechanics’ Institute whose object was the encouragement of colonial science, and it was among the geological collection at the Institute that Dana saw the one fossil specimen of marine life found in the upper Newcastle coal beds. He himself observed none im situ and of the many plant remains he encountered in the formations he reports that the simple leaved Glossopteris Browniana made up four-fifths (1849, pp. 482-3). By the middle of March 1840, the American Squadron had returned from the Antarctic, where the discovery of Wilkes Land com- memorates their work, and after a week’s refitting in Sydney, they sailed for New Zealand on March 19. The scientific members, followed aboard the Peacock a few days later, and, in the last stage of their journey were wrecked off the mouth of the Columbia River. The company, however, escaped in the boats with their reports and specimens and_ returned overland to Washington in June 1842. It was not for ten years after his Australian visit that James Dana published his Report on the Geology of the Expedition, with its — masterly chapter on the geology of New South Wales. In the same year of 1849, he was appointed to the Chair of Natural History at Yale. Despite the briefness of his visit, Dana made a number of important contributions to the foundations of Australian geological science. Having travelled with him through the basaltic region of the Illawarra it is instructive to turn to the highly lucid account he has left of this fortnight’s geological reconnaissance which pro- vided a firm starting point for later detailed surveys of that area. | The basaltic rock occurs both in layers interstratified with the sandstone, and in dikes. By its occurrence, both underlying some layers below the coal, and also pro- truding through the Sydney sandstone, JAMES DWIGHT DANA IN NEW SOUTH WALES, 1839-1840 it appears to be of different ages. The alternation of sandstone and basalt may be seen in many of the cliffs from Black Head to Point Bass, six miles north of Kiama. . . At Black Head, the basalt does not occur in the cliff itself, but may be seen overlying the argillaceous sandstone a few hundred yards back. Going to the northward from this cape, the basalt soon appears capping the bluffs, and dipping with the sandstone below to the northward and westward. This layer of basalt, further north, dips to the water just north of Stony Cove, three miles south of Kiama, where the lower sandstone layer is no longer in sight. The next bluff north is wholly basaltic. The next beyond is capped with red sandstone ; this rock does not appear on the following cliff (at Kiama), which is very low, but composes the whole of the next one, with the exception of a small basaltic portion near the water’s surface at the south end. The basalt thus dips beneath the water like the layer of sandstone before mentioned. Continuing our course northward, in the next cliff, the sandstone becomes capped with a second layer of basalt. Farther on the sandstone disappears and leaves the basalt alone. There are hence, in this coast section, two distinct layers of sandstone, and two of basalt interstratified with them; they disappear in succession as we go northward from Black Head, excepting the upper basalt (Dana, 1849, p. 499). More important however were the conclusions Dana formed from his examination of Kangaroo Valley of the origins of the deep walled gorges of New South Wales. Writing five years after the publication of Darwin’s thesis that these gorges were original escarpments of the sand- stone (Darwin, 1844), Dana dismissed Darwin’s conclusion and argued for the effects of running water in denuding the soft rock over long periods of geological time. In doing so he substantially anticipated modern views of valley making in New South Wales. It is, however, in his observations of the coal measures of the Colony that Dana made his most enduring contribution to the geology of New South Wales. Publishing a decade after the collection of his material it was inevitable that he was anticipated to some extent, but his stratigraphical and lithological descriptions of what he called the “Sydney sandstone”’, the coal formation and the sandstone below the coal from the Hunter Basin to Wollongong and 189 Dapto, indicate the extraordinary grasp and accuracy of Dana’s evidence and the penetration he was able to bring, even as a very young man, to his geological work. The palaeontological findings of others, notably Morris, Lonsdale and McCoy, he incorporated in his Report. Significantly, Dana’s evidence appeared at a time when serious conflict had developed in geological circles on the age of Australian coal. Dana’s former companion, W. B. Clarke, from his own extended researches in the Colony, challenging the widely held view that Australia was a country of recent geological age, had asserted the greater age of the Illawarra and Newcastle coal formations of New South Wales than those of Europe and India. He assigned them to the Devonian or lower Carboniferous ; and he further argued that the marine beds of fossiliferous sandstone underlying the coal and those of predominantly plant fossils above were conformable with the coal seams and belonged to the same geological period. (Evidence before N.S.W. Legislative Committee on Coal, 1847, and published note, 1848.) But the Cambridge palaeontologist, Frederick McCoy, from the evidence of Clarke’s own fossils from the Illawarra and the Hunter, insisted that a vast interval of geological time separated the lower Carboniferous marine deposits beneath the coal, the coal seams themselves and the beds above whose plant fossils, he considered, most nearly resembled the coal fields of India and the true Oolitic fields of Europe. McCoy’s verdict rested on the absence of animal remains in the upper beds of sandstone. From his sanctuary at the Woodwardian Museum he maintained, and was to continue to maintain for many years after he came to Australia to assume the Melbourne University Natural History Chair, that the lower marine beds and the beds of plant fossils above the coal were not conformable and belonged to widely different geological systems (McCoy, 1847). Into this arena of conflict, Dana brought positive evidence from his own observations in the Colony of the conformability of the Australian coal beds. Both in the [lawarra- Wollongong area and at Nobby and Telegraph Hill, he had found the sedimentary deposits below and above the coal conformable and passing in gradual transition into one another in an unbroken series (Dana, 1849, pp. 459, 484). He supported the earlier judgment which Morris had given on Strzelecki’s specimens in 1845, that the flora of the southern hemisphere differed from the northern at the “ carboniferous period’ (Strzelecki, 1845). Louis Agassiz, 190 moreover, in his identification of Dana’s repro- duction of the Newcastle fossil fish found in the overlying sandstone, referred it to the upper Carboniferous or transition Permian, and in Dana’s analysis, this best accorded with the observed facts. Dana therefore concluded his survey of the N.S.W. coal deposits in the following terms (1849, p. 495) : While the coal plants point to the upper carboniferous, or still higher, the fossils below the coal seem to correspond most perfectly with the lower carboniferous epoch. Yet the conformity and continuity of the series of beds, (including the sand- stones below the coal, and the coal layers) observable in various places, the frequent occurrence of conifer logs, like those of the coal beds, in the fossiliferous sandstones at different localities, together with the characters of the fossil fish, leave little doubt that the whole is of one prolonged age, referable to the upper carboniferous, or partly the lower Permian era. It was an accurate and timely contribution to the elucidation of the history of the Permo- Carboniferous systems in New South Wales. As soon as W. B. Clarke read Dana’s Report, he wrote at once to his old friend to compliment him on his work and to re-establish contact between them. Dana’s reply from New Haven is dated 1 September 1851 (W. B. Clarke Papers). I was much gratified with the reception of your excellent letter of 19 December last, and glad to feel assured that we might carry on a correspondence although half the globe lies between us. It was a pleasure to know that with all your opportunities for investigation so thoroughly pursued, you find reason to confirm in the main the ground I have taken respecting New Holland geology. My time there was short, but it was spent most agreeably and most instructively to myself ; and that Nlawarra District is a perfect gem of a place for Geology as well as for landscape beauty ; it is one of the loveliest spots on the Globe. I shall look forward with great interest for the published account of your labours, in which you have made so many and important discoveries. Of McCoy’s work, Dana observed a tactful restraint. “I was satisfied McCoy had made some errors as to localities’’, he commented. “You will set us all to right in whatever is wrong through haste, inadvertence or imperfect ANN MOZLEY knowledge. . . Those places we visited together — are remembered by me with deep feelings of pleasure.”’ James Dana’s next letter to Australia is dated 1854. He had followed some accounts of Clarke’s recent researches into the gold fields of New South Wales, and looked forward to receiving the Report which Clarke had promised him. I trust you will reap some golden results from your labours on behalf of the Gold in Australia. I should enjoy very much another ride over the hills and through the valleys of the country. Will you never come to Yankee land? I should be much pleased to see you here. I wish that you would write a work on the geology of New South Wales and publish it at Government expense. I know you have had this in view. And how long before it will be accomplished ? You must have a vast amount of material for such a work, and it would make a most valuable contribution to Science—Australia is the land for queer things, and therefore a grand place for Scientific Exploration. I should rejoice to take it up with you if and if—and if— there are three ifs, and one long one beside. Clarke had sent Dana a drawing of a fossil fish from Parramatta which the American geologist had forwarded for identification to Agassiz. The enclosed reply to Dana, found among the Clarke Papers, is in Agassiz’s hand, and reports that the aging palaeontologist had journeyed to Cambridge, Massachusetts, to consult his own work on fossil fishes “ not having looked at the subject for many years and wanting to give a precise answer to the enquiries of Mr. Clarke, as the subject is so highly interesting ”’ Agassiz identified the fish positively as belonging to the Oolitic series. “ TI am satisfied ’’, he wrote, “ they are of more recent date than he [Clarke] supposes. This would however render his investigations only more important in a geological point of view.” Dana’s own opinion on the age of the Australian coal measures was to undergo some change as later fossil evidence came to light. In a letter to Clarke of 15 January, 1858, he: observed, “I think you will have to lift the. Australian coal measures up to the Triassic at least. The Illawarra fossils below the coal may be Permian, and the coal itself Triassic.’’ “‘ How I should enjoy another stroll over your hills and into your valleys!’ he concluded this letter, ‘““ But I have done roaming.”’ JAMES DWIGHT DANA IN NEW SOUTH WALES, 1839-1840 It was a theme that was to run through all Dana’s letters to New South Wales. As late as 1872, he confided to his old friend, ‘‘ The few weeks of intercourse which I had with you in Australia were amongst the happiest days of my life and I shall never forget your kindness, or the scenes we enjoyed together’’. Danas last letter is dated 3 January 1876; Clarke was then 78 and within two years of his death. It was thirty-six years, Dana reminded him, since they had met, and he closes their long correspondence with words which marked his own firmly held faith in the purposes of God : “, . .the verses you enclosed and for which I thank you, show that you are ready for whatever is in store, having that blessed hope that makes even death a victory.”’ References CLARKE, W. B., 1848. On the Genera and Distribution of the Plants in the Carboniferous System in New South Wales. Quart. J. Geol. Soc. Lond., 4, 60-63 (read 16° June 1847). CLARKE, W. B. Diary. Mitchell Library, Sydney. Oa CLARKE, W. B. Papers. Mitchell Library, Sydney ; microfilm copies of Dana Correspondence, Basser Library, Aust. Academy of Science, Canberra. All the letters quoted belong to this collection. Dana, J. D., 1849. United Siates Exploring Expedition during the Years 1838, 1839, 1840, 1841, 1842 under the command of Charles Wilkes. Volume X, Geology. Philadelphia. (Royal Society of N.S.W. library ; microfilm copy Basser Library, Canberra.) Darwin, C., 1844. Geological Observations on the Volcanic Islands visited during the Vovage of H.M.S. Beagle; together with some brief notices on the Geology of Australia and the Cape of Good Hope. London. J@RVvis, 7], 19455 orev. WB. Clarke, MiA., Fanes.; F.G.S., F.R.G.S. The Father of Australian Geology. Sydney: Ford. McCoy, F., 1847. On the Fossil Botany and Zoology of the Rocks associated with the Coal of Australia. Ann. & Mag. Nat. Hist., 20. PICKERING, C., 1850. ‘The Races of Man. London: Bohn. Chapter 5. STRZELECK], P. E,, DE., 1845. Physical Description of New South Wales and Van Diemen’s Land. London. WILKES, C., 1852. Narrative of the United States Exploring Expedition 1838-1842. London: Ingram. Vol. I. (Received 9 January, 1964) Journal and Proceedings, Royal Society of New South Wales, Vol. 97) pp. 193-215, 1964 Lower Carboniferous Faunas from Wiragulla and Dungog, New South Wales JOHN ROBERTS Geology Department, University of Western Australia, Nedlands, W Acs AgpstTract—The Middle to Upper Viséan (Cu III,_g) faunas from Wiragulla and Dungog are examined and their palaeoecology discussed. district is briefly considered, The including a first description of the Wiragulla Beds which occur stratigraphy of the Wallarobba-Dungog between the Ararat and Wallaringa Formations on the eastern limb of the Wallarobba Basin. Species described are: Introduction Marine fossils were first collected in 1960 from the Dungog and Wiragulla localities during geological investigations in the Wallarobba- Dungog district. No previous record of collec- tions from either locality has been found in the literature, although Benson (1921) gave Dungog as a Carboniferous fossil locality. However, a more precise locality was not defined and from a search of the literature it now appears that he referred to several different localities, all of which were south of those dealt with in this work. Grid references quoted in this paper are taken from the Dungog One Mile Military Sheet. All fossil and locality numbers refer to the palaeontological register at the University of New England, Armidale, N.S.W. The L.235 Dungog fossil locality is situated 3 miles south of Dungog, three-quarters of a mile west of the main Dungog-Maitland road, and the L.234 Wiragulla locality occurs immedi- ately north-east of Wiragulla railway siding, approximately 4 miles south of Dungog (Text-fig. 1). A northward extension of the L.234 horizon crops out 150 feet stratigraphically above the L.235 Dungog locality. Both horizons are particularly important because they are contained in stratigraphic sections which extend into the non-marine Wallaringa Formation. The occurrence of Delepinea aspinosa (Dun) on both horizons suggests that they can be correlated with one 800 to 1,000 feet above the base of the ‘‘ Lower Kuttung Series” in the Rouchel Basin (Campbell and Roberts, 1964 in press). * Present address: Wanberra, A.C.T. Bureau of Mineral Resources, Chonetes cangonensis n.sp., Gigantoproductus tenuirugosus n.sp., Inflatia elegans n.sp., Echinoconchus gvadatus Campbell, n.sp., Kitakamithyris sp., Balanoconcha elliptica Campbell, Athyris wiragullensis n.sp., Spirifer osborner Streblopteria sp., and Aviculopecten sp. Regional Stratigraphy The geology of the Gresford district has been considered in a previous paper (Roberts, 1961). Text-figure 2 illustrates the stratigraphic nomenclature of the formations in the Gresford- Dungog district. The stratigraphy of the district is briefly summarized below. The Bingleburra Formation (approximately 3,000 feet in thickness) consisting of mudstones, siltstones, oolitic and crinoidal limestones and interbedded sandstones and conglomerates, is overlain by the Ararat Formation (1,500 feet in thickness). This formation is composed of calcareous tuffaceous sandstone with minor mudstones and oolitic and crinoidal limestone lenses. ae toe Ni AWirogulla Gresford e Fuolicrobbo ile (Greenhills avd en) Railways Fig. 1 194 Southern Area Glacial Stage Northern Area Mt Johnstone Beds CARBONIFEROUS Gilmore Volcanics ? UPPER Flagstaff Sandstone Wallaringa Formation Bonnington Formation Ararat Ararat Formation Formation w > .o) x ly ka =~ 2 @) Q q x OG Bingleburra Bingleburra Formation Formation LOWER KirGs es Following Ararat sedimentation marine conditions continued without interruption in the north of the area, and the Bonnington Formation (400 feet in thickness), consisting of siltstones and mudstones, underlies the coarse tuffaceous Flagstaff Sandstone (5,500 feet in thickness). To the south, following the deposition of the Ararat Formation, conditions changed in parts to a non-marine environment due to the uplift of a narrow belt stretching from Hilldale to Mt. Ararat (Roberts, 1961). However, away from the influence of the uplift, for example at Wiragulla near Dungog, a thin marine mudstone and siltstone sequence (Wiragulla Beds) is inter- bedded between the Ararat Formation and the JOHN ROBERTS non-marine Wallaringa Formation. The Wal- _ laringa Formation (950 feet in thickness) is overlain by the Gilmore Volcanics, the Mt. Johnstone Beds (Sussmilch and David, 1920) and rocks of the Glacial “ Stage’’ (Osborne, 1922). Local Stratigraphy Sediments exposed in the Wiragulla-Dungog district crop out on the eastern limb of the Wallarobba Basin. The geology of the district is illustrated in Text-figure 3 and a stratigraphic section from the eastern limb of the basin given in Text-figure 4. Rocks of the Bingleburra Formation crop out a short distance north of the area dealt with in this paper and are overlain by those of the Ararat Formation. Faunal evidence suggests that Ararat sedimentation in the Dungog district may have been prolonged compared with that further to the north and that the Ararat Formation is a time-transgressive unit. Faunas containing Delepinea aspinosa (Dun) occur in the upper beds of the Ararat Formation and the lower part of the overlying Wiragulla Beds on the eastern limb of the Wallarobba Basin. A. fauna in tthe basal beds {of the Bonnington Formation, which overlies the VENT NS NaS NS DAT ee EN fe ene Volcanics Waltaringa Formation Sy x Wallarobba £@4 Conglomerate Wiragulla Beds L234 Wiragulla mudstone L235 Dungog sandstone tuffaceous sediments Pens! conglomerate Ararat tr oolitic limestone — andesite [eth S| LOWER CARBONIFEROUS FAUNAS FROM WIRAGULLA AND DUNGOG 195 ant ‘ PH By , nee ees RANA NAGA i 5 2 ie S Ce ie ee aay Ss , NENA SAENGER NG NEES \N cane IMG orc eed! Coe wgt PE ae IONS AES WAN IDI eS ak: \ ce ks 7 Be i . lis (Ss NAAN ¥ 1O.\ NNAGNSCN Ss yi Math Ap ee a ; VANARRAS AN UNS SN SARS Si 1 ane eee : . an 10 : ae a SNA NSA NSLS NAS SoA .¢ tite Nie \ Viylat Ny space Yoo eek Oe Le 7 a oe Oana ee. . . Ori - Be ie 3 A ESS =< - \ ~~ x / Valen \ \ \ want \ \ an yey Cy \ \ \ Vo ae WX \ Nee \\ \ a \ \ Ne \\\ a eer} L234 horizon ~ ° = \L235 ea Ra 4234 Swiragulla 204 2% 9 See 3324 WALLAROBBA B84 CONGLOMERATE MARTINS CREEK hee] FLAGSTAFF SANDSTONE GILMORE V_} VOLCANICS ANDESITE 2 \A7 WALLARINGA OOLITIC = \~ S4 FORMATION LIMESTONE —— FAULTS WIRAGULLA — = BEDS ARARAT FORMATION BINGLEBURRA FORMATION | MILE —— BOUNDARIES ROADS RAILWAY The Ararat Formation in the Lewinsbrook Syncline 10 miles to the north-west, is distinctly older and is more closely related to the Middle Viséan (Cu III,) L.53 Greenhills assemblage (Roberts, 1964). The Wiragulla Beds occur in an area south of Dungog where they occur between the Ararat and Wallaringa Formations. Wallaringa Formation crops out strongly on the hills forming the eastern flank of the Wallarobba Basin and is overlain by the Martins Creek Andesite, the basal member of the Gilmore Volcanics. Tuffaceous sandstones belonging to the Gilmore Volcanics crop out in the centre of 196 aee| Wallarobba 24 Conglomerate Wallaringa Formation Wiragulla Beds 234 Wiragulla a foeen haem Cl Ararat Formation Wiragulla — Wallarobba Road Section Eastern JOHN ROBERTS = CO j=) = L234 fossils mudstone siltstone a ie sandstone ee oped conglomerate _ oolite lens Re ae A ao fossil horizon L235 Dungog Limb Wallarobba Basin Fig. 5 the Wallarobba Basin. To the north of the basin the coarse marine Flagstaff Sandstone interfingers with and replaces the non-marine Wallaringa Formation. Wiragulla Beds The best exposed section of the Wiragulla Beds crops out on the north-western side of the Paterson-Dungog road from 47659862, near the overhead road bridge crossing the North Coast Railway Line, to approximately 47609852 (Text-fig. 5). A small fault causes a slight disruption to the upper parts of this section immediately below the Wallarobba Conglomerate near a roadside quarry at 47609852. The remainder of the section is influenced by a fault running along the south-eastern side of the railway line and has an anomalous dip to the south. The base of the Wiragulla Beds rests on massive sandstones of the Ararat Formation cropping out to the west of the Chichester- Newcastle water pipeline. The upper limits are obscured by the small fault mentioned above, but the beds appear to gradually merge into coarse sandstones at the base of the Wallarobba Conglomerate. A more poorly exposed section occurs approxi- mately 2 miles north-west of the road section ee ee ee LOWER CARBONIFEROUS FAUNAS on the eastern Limb of the Wallarobba Basin (Text-fig. 5). Here, the Wiragulla Beds con- formably overlie the Ararat Formation and pass with apparent regular conformity into the overlying Wallaringa Formation. Thickness. The thickness of the Wiragulla Beds is approximately 450 feet. Lithology. For the most part the Wiragulla Beds are composed of distinctive grey to pale fawn mudstones and fine-grained sandstones. Lateral Variation. (1) The Gresford District. Two occurrences of the Wiragulla Beds are known from the Gresford District, but because of very poor exposures and the complex nature of the regional stratigraphy they have previously been mapped with other formations. (a) The L.210 Toryburn fossil locality, found in an isolated outcrop on the bank of MclIntyre’s Creek, is surrounded by a large area of alluvium and has been included in the Wallaringa Formation in the geological map of the Gresford district (Roberts, 1961). (b) A thin sequence of fossiliferous mudstones containing the L.211 fossil locality (Roberts, 1961) underlies massive green sandstones on the south-western side of the Colstoun Basin near the Gresford Fault. These mudstones were previously mapped with the Flagstaff Sandstone, but their stratigraphic position and lithology appear to link them with the Wiragulla Beds. (2) South-western margin of the Wallarobba Basin. In a newly exposed section in a road cutting across the Wallarobba Range the Wiragulla Beds are missing, and coarse-grained lithic sandstones appear to underlie the Walla- robba Conglomerate conformably. The absence of the Wiragulla Beds, however, can possibly be best explained by the existence, in certain areas, of an unconformity at the base of the Wallaringa Formation. Support for this suggestion comes from the Clarencetown district, where the Wiragulla Beds and _ faunas characterised by WDelepinea aspinosa (Dun) are absent from beneath the Wallarobba Conglomerate ; instead, the latter member is underlain by a sequence containing a Middle Viséan (CullII,) fauna, the same as that found at L.53 Greenhills (Roberts, 1964), which is definitely older than the Culll, , assemblages from Wiragulla and Dungog. The sandstones underlying the Wallarobba Conglomerate in the above section are coarse- grained, contain a high percentage of volcanic rock fragments, and have a dark green chloritic cement. They are usually massively bedded, but exhibit small scale cross stratification on a B FROM WIRAGULLA AND DUNGOG 197 number of horizons. The lithology changes markedly near the base of the Wallarobba Conglomerate Member from a dark green chloritic sandstone to a pink zeolitic rock. In the lower parts of the western flank of the range the sandstones are accompanied by several thin conglomerate bands. Fossil Localities The stratigraphic positions of the fossil localities discussed in this paper are illustrated in diagrammatic stratigraphic sections from the eastern limb of the Wallarobba Basin (Text-figs. 4, 5). L.235 Dungog occurs in a calcareous sandstone and impure limestone at grid reference 47439880, on the top of a ridge three-quarters of a mile west of the Dungog-Maitland road. Strati- graphically this horizon occurs 130 feet below the top of the Ararat Formation. The fossil bed can be traced some distance north and south of the L.235 collecting point and its lateral extent is shown in Text-figure 3. L.234 Wiragulla is found in pale fawn fine- grained siltstones cropping out on the roadside opposite the large gates of Wiragulla railway siding (grid reference 47659861) and in the railway cutting immediately north-east of the siding. L.234 occurs towards the base of the Wiragulla Beds, its stratigraphic position being shown in Text-figure 5. A northward extension of the L.234 horizon has been found approxi- mately 150 feet stratigraphically above L.235 Dungog. The stratigraphic sections on the eastern limb of the Wallarobba Basin have enabled the L.234 and L.235 horizons to be placed in a sequence extending upwards into the Wallarobba Conglomerate Member of the Wallaringa Formation, the Basal unit of the Kuttung Group. Dungog and Wiragulla Faunas The following is a list of all identifiable species collected during the present investi- gation. Those forms described in this paper are marked with an asterisk. L.235 Dungog. Fenestella sp. Leptagonia cf. L. analoga (Phillips) *Chonetes cangonensts n.sp. Delepinea aspinosa (Dun) *Gigantoproductus tenuirugosus N.sp. *F’chinoconchus gradatus Campbell Waagenoconcha delicatula Campbell Inflatia simplex (Campbell) Pustula sp. 198 Unispirifer striatoconvolutus (Benson and Dun) Votseyella anterosa (Campbell) Kitakamithyris sp. *Balanoconcha elliptica Campbell *Aviculopecten sp. *Streblopteria sp. Diodontopteria delicata Roberts Tentaculites sp. Straparolus sp. L.234 Wiragulla. Fenestella sp. Conularia sp. Schizophoria verulamensis Cvancara Delepinea aspinosa (Dun) *Inflatia elegans n.sp. *Spirifer osbornet n.sp. *Athyris wiragullensis n.sp. *Kitakamithyris sp. Stenoscisma laevis Roberts Diodontopteria sp. Bellerophon sp. Sivaparolus sp. Tentaculites sp. L.234 continuation, 150 feet stratigraphically above L.235. Schizophoria verulamensis Cvancara Leptagonia cf. L. analoga (Phillips) Schuchertella concentrica Roberts Delepinea aspinosa (Dun) *Chonetes cangonensts n.sp. Waagenoconcha delicatula Campbell *Echinoconchus gradatus Campbell Fluctuaria campbella Roberts *Inflatia elegans n.sp. *Spirifer osbornei n.sp. Unispirifer striatoconvolutus (Benson and Dun) *Athyris wiragullensis n.sp. Cleiothyridina sp. “ Camarotoechia’’ sp. Stenoscisma laevis Roberts *Balanoconcha elliptica Campbell *Aviculopecten sp. Bellerophon sp. The following species have restricted vertical ranges and in the Gresford-Dungog district are confined to the L.235 and L.234 assemblages : Delepinea aspinosa (Dun), Chonetes cangonensis n.sp., Gigantoproductus tenuirugosus n.sp., Inflatia elegans n.sp., Inflatia simplex (Campbell), Spirifer osborner n.sp., Athyris wiragullensis n.sp., Balanoconcha elliptica Campbell, Aviculo- pecten sp., Streblopteria sp. These constitute a faunal element which is distinct from the younger assemblages in the district (Roberts, 1963, 1964, 1965). JOHN ROBERTS Age of the Fauna = The age of the Wiragulla-Dungog fauna can be closely estimated as Middle to Upper Viséan (Culll, ,). It is younger than the Middle Viséan (Cull; to CulIII,, Brown, Campbell and Roberts, 1964) fauna from Trevallyn described by Roberts (1965 in press), and the Middle Viséan (Cu III,) fauna from Greenhills (Hilldale) described by Roberts (1964). An age closer to Middle Viséan is suggested by the presence of Schuchertella concentrica Roberts, Echinoconchus gradatus Campbell and Voiseyella anterosa (Campbell) in the Greenhills fauna, and Echinoconchus gradatus Campbell, Inflatia simplex (Campbell), Votseyella anterosa (Campbell) and Balanoconcha elliptica Campbell in the Babbinboon fauna from the Werrie Basin. The latter fauna is now considered to be at the latest Middle Viséan in age, this deter- mination being based on the presence of Upper Tournaisian goniatites in the lower part of the Carboniferous sequence in the Werrie Basin (Campbell and Engel, 1963), and on a correlation of the Babbinboon horizon with the Burlington and Keokuk Limestones of North America. Recent work by Collinson, Scott and Rexroad (1962) has shown the Burlington and Keokuk Limestones to be correlated with the Cu Ily and Cu II; zones, respectively, of Germany. Two brachiopod relationships may be con- sidered in detail. Vozseyella anterosa (Campbell) is morphologically close to Spfirifer mundulus Rowley from the Lower Burlington Limestone of the Mississippi Valley, U.S.A. (Campbell, 1957). This again suggests a Middle Viséan age. Gigantoproductus tenuirugosus n.sp. appears to be morphologically similar to G. dentifer (Prentice), which ranges from the C,S, zone to the D, zone in England and is most common in the D, of Derbyshire. In Belgium G. dentifer occurs in rocks of V,, age. Preservation and Palaeoecology L.235 Dungog. Shelly material is present in all except the extensively weathered portions of the calcareous sandstone and impure lime- stone constituting this horizon. The weathered portion of the rock is most useful in determining internal structures but is extremely friable. Leaching of unweathered material with hydro- chloric acid is a difficult process because of the calcareous nature of the rock. L.234 Wiragulla. Fossils from this locality are preserved as internal or external moulds in LOWER CARBONIFEROUS FAUNAS FROM WIRAGULLA AND DUNGOG a grey to fawn mudstone. Little trace of shell material has been found. The following observations give some indica- tion of environmental conditions prevailing during the accumulation of the two fossil beds. L.235 Dungog. (1) The L.235 horizon is characterized by an intermixed brachiopod/pelecypod fauna, brachiopods being in the majority. Polyzoa are rare and where found are always fragmentary. Solitary corals are absent. (2) Chonetes cangonensis n.sp. and Giganto- productus tenuirugosus n.sp. always have broken hinge spines, suggesting that the shells had been washed around by current action. However, the external features of the shells examined are well preserved, show no evidence of abrasion, and some forms, such as Echinoconchus gradatus Campbell and Pustula sp., still retain their delicate external spinose ornament. (3) A considerable amount of fragmentary shell debris, particularly pieces of Gzganto- broductus tenwmirugosus n.sp. shell, is found in parts of the bed. (4) Valves of brachiopods and pelecypods are usually found dissociated, having been washed apart after the death of the animal. (5) The population ranges from juveniles to adults and species of all sizes occur in the one bed. No major sorting appears to have taken place. (6) Although the bottom sediment apparently had no suitable hard areas where brachiopods possessing a pedicle could anchor themselves, many specimens of the terebratuloid Balano- concha elliptica Campbell have been collected. These show no evidence of having been washed into the bed from elsewhere and presumably attached themselves to other shelly organisms. The L.235 fauna appears to be near its original position of growth in a shallow sandy marine environment. Occasional stronger currents washed in fragments of Gigantoproductus tenui- vugosus n.sp. which may have been broken by Wave action in a region nearer the shoreline. Despite the disarticulation of the valves, most other species are probably somewhere near their original position of growth because they are unsorted and their surfaces are well preserved and show no indication of abrasion. A rapid burial soon after death may account for the preservation of the delicate ornament on some spinose brachiopods. BB r og, L.234 Wiragulla. (1) Most shells are disarticulated and often have worn’ external surfaces. Productid brachiopods are stripped of all external spines. Internal features, however, are excellently preserved. Solitary corals are not found in their positions of growth but lie parallel with the bedding planes. Polyzoa are rare. (2) Portions of the fossiliferous bed contain a mass of broken gastropod fragments, ostracods, broken echinoid plates and spines and crinoid columnals. The sediment accompanying the fragmentary material is noticeably coarser than the remainder of the bed and may have been washed in by stronger current action. (3) Sorting has taken place to a limited extent and though the population ranges from juveniles to adults the latter predominate. (4) Wood fragments are common. (5) The finer sediment contains fragmentary burrows formed by a sub-surface fauna. The L.234 Wiragulla fauna is not preserved in a living position. The wear shown by the exteriors of the larger productid and spiriferid shells, the disarticulated nature of the valves and the absence of productid spines suggests that currents washed the shells around for a considerable time prior to burial. Fragmentary debris associated with slightly coarser sediment may have been carried in by stronger currents. Acknowledgements The author is grateful to the following persons for their advice and comments on this work: Dr. P. J. Coleman, University of Western Australia, Nedlands, W.A.; Dr. K. S. W. Campbell, Australian National University, Canberra, A.C.T.; and Dr. R. Goldring, University of Reading, Reading, England. The cost of the plates was subsidized by a grant from the University of Western Australia. SYSTEMATIC PALAEONTOLOGY Brachiopoda Suborder CHONETOIDEA Muir-Wood, 1955 Superfamily CHONETACEA Shrock and Twenhofel, 1953 Family CHONETIDAE Bronn, 1862 Subfamily CHONETINAE Bronn, 1862 Genus CHONETES Fischer de Waldheim, 1830 TYPE SPECIES: Terebratulites sarcinulatus Schlotheim, 1820, by subsequent designation of Verneuil, 1845. Dr1aGnosis : An emended diagnosis for the genus has been given by Muir-Wood (1962). 200 REMARKS: This material is referred to Chonetes sensu stricto as redefined by Muir-Wood. The most characteristic features supporting this designation include the two poorly defined septa in the brachial valve, the strong median septum in the pedicle valve and the relatively flat nature of the shell. The transverse form of the shell is the only departure from the characters pre- sented in the emended diagnosis. Chonetes cangonensis n.sp. Plate I, figs. 1-10 Diacnosis: Shell flat to slightly plano-convex ; twice as wide as long, sub-rectangular in shape with rounded cardinal margins ; 20-24 capillae occur per 3 mm. at the anterior margin of the shell. Pedicle valve has 3 or 4 spines on either side of the umbo; median septum extends to the mid-point of the valve. Brachial valve possesses strong socket plates ; 2 long divergent spinose septa extend from the muscle field almost to the anterior margin; a median septum has not been observed. DESCRIPTION : EXTERNAL. The shell is small, extremely flattened, approximately twice as wide as long, and sub-rectangular in shape. The greatest width occurs a short distance in front of the hinge and the lateral margins and cardinal extremities are well rounded. Capillae are narrow, half as wide as the well rounded separating sulci, and increase by more or less regular intercalation. There are 20-24 papillae per 3 mm. at the anterior margin of the shell. Concentric and radial micro-ornament is absent. The surface ornament becomes weaker on the postero-lateral margins of the shell. The dimensions of the largest shell observed are 10 mm. wide and 6-5 mm. long. Pedicle valve is slightly convex on the postero-lateral slopes, but flattens anteriorly. The umbo is obsolete. Three or four spines are present along the hinge on either side of the umbo. An extremely faint median sinus may be developed. The cardinal area is flat and less than 0°5 mm. high at the umbo. No details of the delthyrium have been observed. Brachial valve is flat and has a lower cardinal area than that of the pedicle valve. The fold is generally obsolete. INTERNAL. Pedicle valve. The median septum is thin, extends from the umbo to the mid-point of the valve and tapers anteriorly to a sharp blade-like ridge. Two faint divergent ridges arise at the base of the septum and run a short distance laterally. They may border the muscle JOHN ROBERTS field. No details of the muscle scars or dental apparatus have been observed. The internal surface of the valve is ornamented with aspinose striae which tend to be irregular in the mid- portion of the valve. Brachial valve. Socket plates are large, arise from the base of the cardinal process, curve laterally and are slightly divergent from the hinge. Two smaller divergent ridges run from near the base of the cardinal process and enclose the muscle field. The muscle field is triangular in shape and deeply depressed below the cardinal process. Individual muscle scars are not preserved. Two slightly divergent spinose septa extend from the base of the muscle field almost to the anterior margin of the valve. The septa are low and may be almost obsolete in some specimens. The internal surface is marked with papillose radial ribs having a density of 10-12 per 2 mm. at the anterior margin. Papillae are coarsest a short distance behind the margins of the valve. No details of the cardinal process have been observed. REMARKS: “Tracing pe unsatisfactory because it is subject 1 to attack He silyerfish and also changes its shape i in sympat aad should be sent, so “that: the og es possible damage to the diagrams, whil is in t mail. ‘ eit : Dintoaraols, Plioboeaphe od be’ in-. cluded only where essential, shotild be glossy, is lost in reproduction of) half-tone ° blo Particular attention should. be paid to geological, subjects., When several photograp ) should be. mounted on a: sheet. of white b oie ae -, Geological. Pai a | eee i in sp circumstances, authors submitting manusc _ Reprints. Authors who are. Aa Bi ee 4 is ie By a yb) bs a f % y n| Pane ae hed A eel Sass aay Annual Reports Report of the Council for the Year Ended 31st March, 1964 Presented at the Annual and General Monthly Meeting of the Society held Ist April, 1964 At the end of the period under review the composition of the membership was 358 members, 18 associate members and 9 honorary members; 18 new members were elected. Eight members resigned and the names of one member and one associate member were removed from the list of members under Rule XVIII. It is with extreme regret that we announce the loss by death of the following eminent members : Dr. Edgar H. Booth (elected 1920). Protessor Richard C. L. Bosworth (elected 1939). Emeritus Professor Leo A. Cotton (elected 1909). Emeritus Professor Harvey Sutton (elected 1920). At the meeting of the Council held on 24th April it was decided to offer Life Membership to Mr. J. W. Hogarth “‘in view of meritorious service to Chemistry in the City of Sydney over a large number of years ’’. This is the only occasion on which Life Membership has been offered to a member. Nine monthly meetings were held. The abstracts of all addresses have been printed on the notice papers. The proceedings of these follow. The members of the Council wish to express their sincere thanks and appreciation to the nine speakers who contributed to the success of these meetings, the average attendance being 37. The Annual Social Function was held on 19th March at the Sydney University Staff Club and was attended by 54 members and guests. The Council has approved of the following awards : The Clarke Medal for 1964 to Dr. Joyce W. Vickery, M.B.E., of the National Herbarium. The Society’s Medal for 1963 to Prof. R. 5. Nyholm, PeikS., of London University College. The Edgeworth David Medal for 1963 to Prof. N. H. Fletcher, of the University of New England. The James Cook Medal was not awarded. The Archibald D. Ollé Prize was not awarded. The Donovan Astronomical Lecture for 1963, given under the auspices of the Royal Society of New South Wales and the N.S.W. Branch of the _ British Astronomical Association, entitled ‘“‘ Positional Astronomy ’’, was delivered by Mr. Harley Wood, Government Astronomer, Sydney Observatory. This lecture has been published in the Journal and Pyro- ceedings, v. 97, pp. 135-144. The Society has again received a grant from the Government of New South Wales, the amount being £750. The Government’s interest in the work of the Society is much appreciated. The Society’s financial statement shows a surplus of £2,211 lls. 7d., of which £2,192 10s. 6d. was the result of sales of surplus library stock, leaving as a true surplus the amount of £19 ls, Id. A The New England Branch of the Society held six meetings and the Proceedings of the Branch follow. The President was to represent the Society at the Commemoration of the Landing of Captain Cook at Kurnell. The proceedings were cacelled due to inclement weather. The President attended an exhibition of paintings of Australia and the Pacific in the Mitchell and Dixon Galleries of the Public Library of New South Wales. Both Mr. McKern and Dr. Low were present at the opening of the New Wing of the Australian Museum. The President attended the Annual Meeting of the Board of Visitors of the Sydney Observatory. On 12th July, the President and the Honorary Secretary waited on His Excellency the Governor of New South Wales. The Society’s representatives on Science House Management Committee were Mr. C. L Adamson and Mr. H. A. J. Donegan, the alternative representatives being Mr. Conaghan and Dr. Low. Six parts of the Journal and Proceedings have been published during the year. Due to costs of publication, Council decided, with regret, to wind up the Monograph Fund and to revert the funds to the General Purpose Account of the Society. The Section of Geology held five meetings, and abstracts of the proceedings will be published later. Council held eleven ordinary meetings. Five special meetings were held to discuss alterations to the Rules. Attendance was as follows: Mr. H. H. G. McKern 16; Mr. J. L. Griffith 14; Prof. R. J. W. Le Fevre (absent on leave for 4 meetings) 3; Mr. W. H. G. Poggendorff 7 ; A/Prot. W. Be Smith-White 7; Dr. A. H. Low IG; Dr. A. A. Day 14; Mr. C. L. Adamson 12; Dr. Ida A. Browne 11; Mr. H. F. Conaghan 12; Father A. G. Fynn 10; Dr. N. A. Gibson (absent on leave for 7 meetungs) 3; Mr H. G. Golding 6; Mr. 2” Ws: Humphries 14; Dr. A. Keane 13; Mr. J. Middlehurst 8: Dr. R. L. Stanton 1; Dr. A. Ungar (absent on leave for 3 meetings) 4. A major undertaking of the Council was a complete revision of the Rules. To this end a sub-committee was formed to which Mr. A. F. A. Harper was co-opted. The Library—Periodicals were received by exchange from 398 societies and institutions. In addition an amount of £105 Os. 3d. was expended on the purchase of 11 periodicals. Mr. A. F. Day resigned from the position of Assistant Librarian on 24th March. Due to Mr. Day’s efforts the reorganization of the library has now been completed. Renovations to the office and library carried out during the year included painting and new floor covering. Among the institutions which made use of the library through the inter-library loan scheme were : N.S.W. Govt. Depts.—Department of Main Roads, Department of Mines, Department of Public Health, 218 State Fisheries, Sydney County Council, Water Conservation & Irrigation Commission, Division of Wood Technology. Commonwealth Govt. Depts.—C.S.1.R.O. 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Ltd.; Australian Consolidated Industries : Australia Electrical Industries; Australian Gaslight Co. Ltd.; Australian Iron and Steel Ltd.; B.H.P. Co. Ltd. ; C.S.R. Co. Ltd. ; Commonwealth Industrial Gases; Johnson & Johnson; Lysaght Ltd.; Mauri Bros. & Thompson Pty. Ltd.; Phillips Electrical Industries; Stawfer Chemical Co.; Titan Manu- facturing Co.; Wheat Industries (Aust.) Pty. Ltd. ; W.D. & H.O. Wills Ltd. Research Institute—Bread Research Institute. Museum—rThe Australian Museum. Miscellaneous—Australian Medical Association ; Institution of Engineers, Aust.; Linnean Society of New South Wales; The Reserve Bank; Standards Association of Australia; Department of Works, Brisbane; The Government Geologist, Brisbane ; Geological Survey of Western Australia. Total borrowings—517 items. A. H. Low A. Au DAY Hon. Secretaries. ANNUAL REPORTS 219 Financial Statement BALANCE SHEET AS AT 29th FEBRUARY, 1964 LIABILITIES 1963 ou. Used: £ Sng: 1,000 Accrued Expenses ‘ sf es ee —- 26 Subscriptions Paid in Advance i 30 9 O Life Members’ Subscriptions — Amount. ‘carried OF forward =n 89 5 O Trust and Monograph Capital Funds (detailed below)— Clarke Memorial .. on 7 ae .. 2,092 4 7 Walter Burfitt Prize wea is is .. 1164 1 4 Liversidge Bequest a4 oH fn 714 0 6 Monograph Capital Fund ee an oak — 8,760 Ollé Bequest - : ea as i 223 17 7 ————— 4,194 4 0 22,839 Accumulated Funds .. ime 29,692 15 4 160 Employees’ Long Service Leave Fund Provision = 184 19 8 Contingent ‘Liability (in connection with Per- petual Lease). £32,882 £34,191 13 O Aso TS 1,986 Cash at Bank and in Hand .i. ae — 2 2,858 15 3 Investments— Commonwealth Bonds and Inscribed Stock— At Face Value—held for : Clarke Memorial Fund ae aay .. 1,800 0 0O Walter Burfitt Prize Fund a, if 1000 0 O Liversidge Bequest .. Pe is - LOO» 805-0 General Burposes . ans ae 2. 09,160 -0 0 8,460 —_——— 8,660 0 0 160 Fixed Deposit—Long Service Leave Fund 8 184 19 8 Debtors for Subscriptions .. oe ae Bee 116 138 0 fecsswixccenve 101, Bad Debts.» 2. ae oa 116 13 OO 14,835 Science House—One-third Capital Cost... a 14,8385 4 4 6,800 Library—At Valuation Ae 6,800 0 O Furniture and Office Equipment —At Cost, less 626 Depreciation : ae 838 8 O 14 — _ Pictures—At Cost, less Depreciation — os on 13 5 9 1 Lantern—At Cost, Jess Depreciation ie es 0) £32,882 £34,191 13 0 220 ANNUAL REPORTS Me TRUST AND MONOGRAPH CAPITAL FUNDS Walter Clarke Burfitt Liversidge Ollé Memorial Prize Bequest Bequest 5 1s Ge t's. id: £ Sade f° 4s. ids Capital at 29th February, 1964 -», 4,800. 0: 107 17000, °0 O02 7TO0sR0 RD — Revenue— Balance at 28th February, 1963 .. 214 0 8 195 14 11 16 10-773) TS toad Income for twelve months .. wis io Oe 43 ll 5 30 10 9 42 5 0O 292 9 7 2389 6 4 14 0 6 223 17 7 Less Expenditure ate ar 0 5 0 75, Yor O — = Balance at 29th February, 1964 .. £292 4 7 £164 1 4 . $14 "O16 “£22357 ACCUMULATED FUNDS x 9S. od. £ Sande Balance at 28th February, 1963 .. ar ee 22,8389 2 5 Add— Transfer of Monograph Capital Fund .. 3,000 0 0 Monograph Fund—Revenue Account .. 1688 9 4 Sundry Receipt .. aie ce es 015 O Surplus for Twelve Months ice Pee 2,21 V7 29,739 18 4 Less— Increase in Reserve for Bad Debts =... 1738 26 Transfer for Long Service Leave Fund Provision er oF ns oka peco ero en@ Subscriptions Written Off ae -- 414 6 — 47 3 0 £29,692 15 4 Auditors’ Report The above Balance Sheet has been prepared from the Books of Account, Accounts and Vouchers of The Royal Society of New South Wales, and is a correct statement of the position of the Society’s affairs on 29th February, 1964, as disclosed thereby. We have satisfied ourselves that the Society’s Commonwealth Bonds and Inscribed Stock are properly held and registered. HORLEY & HORLEY, Chartered Accountants. Prudential Building, Registered under the Public Accountants 39 Martin Place, Sydney, Registration Act 1945, as amended. 19th March, 1964. (Sgd.) C.:L. ADAMSON, Honorary Treasurer. ANNUAL REPORTS INCOME AND EXPENDITURE ACCOUNT Ist March, 1963, to 29th FEBRUARY, 1964 Advertising Annual Social . Audit .. Branches of the Society Cleaning : Depreciation Electricity : Entertainment Insurance ‘ Library Purchases Miscellaneous .. Postages and Telegrams Printing— J ournal— Vol. 96, Parts 2-6 Vols 9%; Part I .. Reprints ‘ Postages Binding Less— Provision for Vol. 96, Parts 2-6 Sale of Reprints Subscriptions (to Journal) — Back Numbers Refund Postages Printing—General Rent—Science House Management Repairs Salaries Telephone Surplus for the “Twelve Months Membership Subscriptions Proportion of Life Members’ Subscriptions Government Subsidy Science House Management—Share ‘of Surplus . Interest on General Investments ; Sale of Periodicals ex the eee Donations Sundry Receipts Deficit for Twelve Months . Ss 1,863 10 10 jam — — ODOOFrNNAOCOSHw Ss. 19 10 0 12 8 10 4 15 £6,170 0 p. — Orono tWWwoorcoeo NOANAONW — COannoon & I Obituary Edgar Harold Booth, M.C., D.Sc., a member of the Society since 1920, and President in 1936-37, died in Sydney on 18th December, 1963, at the age of 70. The son of James Booth, formerly of Montrose in Scotland, Dr. Booth was born in Sydney on 12th February, 1893, and was educated at the Fort Street School, Observatory Hill, and the University of Sydney. He graduated Bachelor of Science in Physics and Mathematics in 1914. In 1915 he was appointed Assistant Lecturer and Demonstrator in Physics in the University of Sydney but resigned in the same year to join the A.I.F., with which he served in France and Belgium until 1919. He won the Military Cross in action at Ypres in 1917 and was also mentioned in dispatches. From 1919 to 1937 Dr. Booth was Lecturer in Physics at the University and during this period took an active interest in the methods of geophysical exploration which were just beginning to be applied to the search for mineral resources in Australia. From 1929-1931 he acted as a consultant to the seismic section of the Imperial Geophysical Experimental Survey which carried out a series of pioneer test surveys; the results were published in 1931. The developments he further discussed in his Presidential address to this Society, while in 1935 he submitted a paper on a magnetic survey of the Mt. Gibraltar district surrounding his country residence, “ Hills and Dales ’’, Mittagong. In 1931, with Miss P. M. Nicol, he published the textbook ‘‘ Physics, Fundamental Laws and Principles ”’ which has been used by many generations of students and reached its sixteenth edition in 1962. In 1932 he published ‘‘ Elementary Physics ’’, which also ran to a number of editions. The Government of New South Wales appointed him consulting physicist in 1930. In 1936 he was awarded the degree of D.Sc. by the University of Sydney. In 1937 Dr. Booth was appointed by the University as a Warden, to be responsible for the formation, direction and control of a College to be called the University College of New England. To him belongs much of the credit for the successful establishment of the College and for the impact which the College had on the spread of education in northern New South Wales. He remained in this position until 1945. His diverse talents were now to be exhibited in an environment of a kind totally different from that in which he had moved hitherto, for in 1945 he accepted an invitation to become the overseas representative of the Australian Wool Board and chairman of the International Wool Secretariat. While in London he became a Vice-President of the Incorporate Society of London Fashion Designers and took a keen interest in promoting the use of wool by leading designers. In 1948 he was forced by ill-health to resign his appointment and returned to Australia. From 1950 he was at. various times a member of the Councils of the Standards Association of Australia, the National Research Council of Australia and the Australian and New Zealand Association for the Advancement of Science. In 1924 Dr. Booth married Jessie Wilcox and she, a son and a daughter survive him. Richard Charles Leslie Bosworth was born in 1908 and died on 24th March, 1964. The late Professor Bosworth was educated at the University of Adelaide, South Australia. In 1933 he was awarded an 1851 Exhibition Scholarship and proceeded to Trinity College Cambridge, England, where he worked under Sir Eric K. Rideal for five years, receiving his Ph.D. from Cambridge University in 1935. In 1938 he received) the) degree of D-Se! from the University of Adelaide. After returning to Australia in 1938 he was appointed Research Chemist to the Colonial Sugar Refining Co. Ltd., Sydney, N.S.W., and in 1948 became Manager of this company’s Research Department, which position he held until he resigned in January, 1957, to take up the appointment at the University of New South Wales on 12th March, 1957, as Associate Professor and Head of the Department of Physical Chemistry, which position he held at the time of his death. He was guest Professor to the University of Canterbury, New Zealand, and guest lecturer to the New Zealand Chemical ‘Society, Auckland, in September, 1961. He attended the conference at Hobart in February, 1963, of the Electro-Chemical Society, and was on the Executive Committee. The late Professor was to have been the guest speaker at the British Rheological Meeting at Brown University, U.S.A., but owing to ill-health could not attend, but his paper was read and is now in the process of being published by Pergamon Press. He also had accepted a visiting Professorship to the University of Illinois, U.S.A., for 1962, but had to withdraw on account of ill health. He was offered the position of Head of the School of Chemical Engineering at Monash University, Victoria, but had to turn down the invitation on account of ill health. In 1951, Professor Bosworth was joint participant in the award ot the H. G. Smith Memorial Medal and in 1957 he was awarded the Medal of the Royal Society of New South Wales for his distinguished contributions and services to the Society. A member of the Royal Society of New South Wales since 1939, he served on the Council as an ordinary member and as Honorary Secretary and was elected President in 1951. PUBLICATIONS Papers published in the Journal and Proceedings of the Royal Society of New South Wales : 1940 Adsorption of Hydrogen by an Ideal Metal, v. 74, pp. 538-548. 1944 Bessel’s Formula in relation to the calculation of the probable error from a small number of observations, v. 78, pp. 81-83. Thermal Conductivity from Measurements of Convection, v. 78, pp. 220-225. Contact Potential Difference as a Tool in the Study of Adsorption, v. 79, pp. 53-62. Radiant Heat Loss as a Problem in Effusion, v. 79, pp. 63-66. A Convenient Vacuum Method for the Prepara- tion of Nitrogen, v. 79, pp. 116-117. 1945 OBITUARY 1945 Evaporation of Oxygen from a Tungsten Surface, v. 79, pp. 190-195. Properties of Nitrogen on Tungsten Films, veo pp. 166-171. 1946 A Simple Demonstration of the Difference between Film and Nuclear Boiling, v. 80, pp. 20-21. 1947 Dimensional Methods in the Design of Industrial Chemical Research, v. 81, pp. 15-23. A New Method for the Comparison of the Thermal Conductivities of Fluids, Pt. 1, v. 81, pp. 156-166. A New Method for the Comparison of the Thermal Conductivities of Fluids, Pt. 2, v. 81, pp. 210-215. Corrosion of Surfaces Heated Above the Boiling Point of the Corrodant, v. 81, pp. 206-209. 1948 The Incomplete Nature of the Symmetry Relations between Thermodynamical Quantities, v. 82, pp. 175-182. The Concepts of Resistance, Capacitance and Inductance in Thermal Circuits, v. 82, pp. 211-217. 1949 The Effect of Diffusional Processes on the Rate of Corrosion, v. 83, pp. 8-16. The Influence. of Forced Convection on the Process of Corrosion, v. 83, pp. 17-24. The Influence of Natural Convection on the Process of Corrosion, v. 83, pp. 25-30. The Formation of Mobile and Immobile Films of Oxygen on Tungsten, v. 83, pp. 31-38. A Note on the Sigma Phenomenon, v. 83, pp. 39-43. Anodic and Cathodic Polarisation of Copper in Acetic Acid, v. 83, pp. 124-133. (with P. R. Johnson) A New Method of Measurement of the Surface Tension of Viscous Liquids, v. 83, pp. 164-169. 1950 The Five Properties Concerned in the Transport of the Active Corrodant Agent, v. 84, pp. 53-58. 1952 Presidential Address: Transport Processes in Applied Chemistry, v. 86, pp. 3-13. 1960 (with C. M. Groden) Kinetics of Chain Re- actions, v. 94, pp. 99-108. 1962 (with C. M. Groden) Conditions for Stability in Chain Reactions, v. 95, pp. 189-194. Books Published : “Physics in Chemical Industry’’, MacMillan & Co., London (1950). “Heat Transfer Phenomena’’, Associated General Publications Ltd., Sydney. John Wiley, Inc., New York (July, 1952). “Transport Processes in Applied Chemistry ’’, Associated General Publications Ltd., Sydney. John Wiley, Inc., New York (April, 1956). Contributor to: ‘‘ Principles of Sugar Technology ”’, edited by P. Honig, published by Elsevier Publishing Co., N.Y., Amsterdam, London, New York, Princeton—‘‘ Determination of Heat Trans- mission as an Indirect Method for the Deter- mination of the Viscosity and Supersaturation of Technical Sugar Solutions ’’, Chapter 8, Volume Ht, 859; and “Heat Transfer’’, Chapter 1, Volume III, 1963. Further Publications : Studies in Adsorption. Part 1. Adsorption of Carbon Dioxide, Sulphur Dioxide and Water. Trans. Far. Soc., 28, 12, 896-902, 1932. 223 Studies: im Adsorption.. Part IT. Lower Fatty Acids. Trans. Far. Soc., No. 139, 28, 901-912, 1932 (Part 12). New Types of Linear Bolometers. Trans. Far. Soc., 30, 7, 554-560, 1934. The Electrical Resistance of Thin Films of Nickel Prepared by Electro-Deposition. Trans. Far. Soc., 30, 7, 549-554, The Mobility of Sodium on Tungsten. Proc. Roy. Soc., London, A, 150, 50-76, 1935. The Photo-Sensitisation of Films of Potassium by Means of Hydrogen. Trans. Far. Soc., 32, 9, 1369-1375, 1936. The Mobility of Potassium on Tungsten. Proc. Roy. Soc., London, A, 154, 112-123, 1936. A Study of the Properties of Hydrogen Films on Tungsten by the Method of Contact Potentials. Proc. Cambridge Phil. Soc., 33, 1937. Intermolecular Forces in Two-Dimensional Systems. R. C. L. Bosworth and F. K. Rideal. Physica, 4, 10, 925-940 (1937) (The Hague). Studies in Contact Potentials—The Condensation of Potassium and Sodium on Tungsten ; The Evapora- tion of Sodium Films. Proc. Roy. Soc., London, A, 162, 1-49, 1937. The Photoelectric Schottky Effect. Trans. Far. Soc., 33, 590-6, 1937. The Evaporation of Concentrated Films of Sodium. Proc. Cambridge Phil. Soc., 34, Part II, 1938. The Surface Tension of Mercury by the Maximum Bubble Pressure Method. Trans. Far. Soc., 34, 12, 1501-1505, 1938. The Adsorption of Acetic Acid by Mercury. Trans. Far. Soc., 35, 1349-52, 1939. The Contact Potential of Nickel. Trans. Far. Soc., 34, 397-402, 1938. A Note on the Effect of Carbon Dioxide on the Surface Tension of Mercury. Trans. Far. Soc., 35, 1853-4, 1939. Surface Diffusion. Part 1 Experimental. Part 2 Theoretical. Aust. Chem. Inst. Proc., 9, 134-142 and 169-178, 1942. Synthetic Liquid Fuels. Aust. J. Sc., 5, 1, 28-33, 1942. Basic Science in Industry. Aust. J. Sc., 5, 4, 110-113, 1943. The Physicist in the Chemical Industry. J. Scientific Instruments, 20, 142-5, 1934. Thermal Inductance. Nature, 158, No. 4009, p. 309, Aug. 31, 1946. Unsteady State Adsorption in Spray Equipment. J. and Proc. Aust. Chem. Inst., 13, 53-9, 1946. A Definition of Plasticity. Nature, 157, 447, 1946. The Thermal Ohm, Farad and Henry. Phil. Magazine, 37, 7, 803-808, 1946. An Interpretation of the Sigma Phenomena. Phil. Magazine, 38, 7, 592-601, 1947. Chemical Similarity in Heterogeneous Catalysis. Trans. Far. Soc., 43, 7, 399-406, 1947. An Interpretation of the Viscosity of Liquids. Trans. Far. Soc., 44, 5, 308-317, 1948. Distribution of Reaction Times for Laminar Flor in Cylindrical Reactors. Phil. Magazine, 39, 7, 847-862, 1948. Thermal Mutual Inductance. Nature, 161, 166-7, 1948. Adsorption of the 1934. 224 The Second Viscosity Coefficient in Rheological Systems. Aust. J. Sc. Res., Series A—Physical Sciences, 2, 3, 394-404, 1949. Distribution of Reaction Times for Turbulent Flow in Cylindrical Reactors. Phil. Magazine, 40, 7, 314-224, 1949. The Mechanisms of Diffusional Processes. Aust. Chem. Inst. Proc., 460-482, 1949. The Measurement of Pan Circulation. Proc. Internat. Soc. Sugar Cane .Technologists. 7th Congress, 1950, 644—-€54, 1951. Sucrose as a Raw Material in Chemical Industry. Rev. Pure and Applied Chem., 2, 4, 212-228, 1952. Measurement of Pan Circulation. Proc. I.S.S.C.T. 8th Congress, 1953, 782-793. The Kinetics of Collective Sedimentation. J. Colloid. Sci., 11, 4 and 5, 496-500, 1956. Irreversible Processes in Physical Theory. Nature, 181, 402, 1958. The Use of Non-dimensional Groups. The Engineer, London, March 6th, 1959, 9, 381-2. The Boiling of Liquids. Rev. Pure and Applied Chem., 9, 213-223, 1959. Thermal Transients Associated with Natural Con- vection. R.-C. L. Bosworth and C. M. Groden. Aust. J. Phys., 13, No. 1, 73-83, 1960. Attempts to Measure the Inductive Element Associated with the Natural Convection of Heat. Aust. J. Phys., 13, No. 1, 84-94, 1960. Consideraciones Sobre Los Efectos Termicos de Las Operaciones de Los Tachos. Proc. XXXIV Meeting of Asociacion de Tecnicos Azucareros de Cuba in Habana, Nov. 1960. Cellulose as a Radiation Dosimeter. K.-C: 1 Bosworth, 1. Ernst and J7L. Garnett: Proc. Conf. Tech. Uses Radiation, Sydney, May 23-25, 1960. Melbourne Press, p. 53. Gas Films on Metals. J. of the Aust. Inst. of Metals, 7, No. 1, 67-70, 1962. Some Current Developments in Chemistry and the Chemical) Industries; Chapter 13, p. 147; of “A Goodly Heritage ’’, A.N.Z.A.A.S. Jubilee Publication, 1962. The Effect of Resident Time Distribution on the Rate of Advancement of a Reaction. ReaC, UL. Bosworth and.C. M. Groden: Aust. J. Chem., 15, 443-52, 1962. Rheology in Australia and New Zealand. Nature, 196, No. 4853, 421-422, 1962. The Mechanical Properties of Emulsions. Australasian J. of Pharmacy, Supplt. 44, No. 523, 1963. Damped Waves Associated with Thermal Convection. R. C. L. Bosworth, C. M. Groden and O. S. Wecksler. Aust. J. Phys., 16, No. 3, 353-59, 1963. Thermal Properties of Systems Exhibiting Optimum Countercurrent Heat Exchange. R. C. L. Bosworth and C. M. Groden. Aust. J. Phys., 17, No. 1, 26-36, 1964. Optimum Thermal Efficiency in Countercurrent Heat Exchangers. R. C. L. Bosworth and C. M. Groden. Aust. J. Phys., 17, No. 1, 37-44, 1964. Rate of Advancement of Reactions in Turbulent Flows. R. C. L. Bosworth and C. M. Groden. (In press—to be published shortly in Aust. J. Chem.) No. 7, OBITUARY Spatial Distribution of Stresses in Shearing Motion. (In press—to be published by Pergamon Press as a contributed paper in the Proceedings of the Fourth International Congress on Rheology, held at Brown University August, 1963.) Leo Arthur Cotton, M.A., D.Sc., Edgeworth David Professor of Geology and Physical Geography (1925-1948) and Professor Emeritus since 1949, died in Sydney on 12th July, 1963. Son of Francis Cotton, engineer and inventor, Leo Arthur Cotton was born at Nymagee (N.S.W.) on llth November, 1883. When fourteen years of age, he came to Sydney with his parents and entered Fort Street High School where, however, his studies were interrupted by the family’s temporary translation to the Forbes and Hillgrove districts. Later he resumed his studies at the same school and in March, 1903, matriculated as an evening student in the Faculty of Arts of the University of Sydney. After a distinguished undergraduate career, Leo Cotton graduated in 1206 as Bachelor of Arts with First Class Honours in Mathematics. Entering the Faculty of Science, he graduated as Bachelor of Science in 1908 with First Class Honours in Geology-Mineralogy, being awarded in this period the Smith Prize in Physics, the Slade Prize for Practical Physics, the Professor David Prize for Geology, the Deas-Thompson Scholar- ship in Physics, the Deas-Thompson Scholarship in Geology, and the John Coutts Scholarship for distinction in Science. In December, 1907, Leo Cotton became a member of the Shackleton Antarctic Expedition, sailing from Lyttleton (N.Z.) in the “‘ Nimrod ’’, and returning in March, 1908, to take up his duties as Demonstrator in Geology, University of Sydney, where Dr. Woolnough was acting as head of the Department during the absence of Professor David occasioned by his exploration and scientific work in Antarctica. In 1908 Leo Cotton was awarded a Linnean Macleay Research Fellowship which he held for two years while engaged in an investigation of ore deposition with particular reference to the New England district. In 1911 he was appointed to the permanent establish- ment of the Department of Geology of the University of Sydney as Lecturer and Demonstrator, beginning a long period of distinguished University service. His appointment as Assistant Professor in 1920 made public acknowledgement of his outstanding work as Acting Head of the Department of Geology during the absence of Professor David on War Service overseas in the period January, 1916, to April, 1919. Leo Cotton’s appointment in 1925 as Professor and Head of the Department of Geology in succession to Professoz Sir Edgeworth David was a fine tribute to his evident qualities as a scientist and leader, further proven in 1921 and 1923-24 when he had again acted as Head of the Department of Geology during the absence of Professor David. In addition to his outstanding work as Professor and Head of the Department of Geology over a period of twenty-four years, Leo Cotton served with distinction as Dean of the Faculty of Science between 1944 and 1946. Despite extended periods of considerable and often difficult responsibility, Leo Cotton nevertheless estab- lished and developed an outstanding reputation for scholarship. His research interests lay particularly in the mathematical aspects of geology and geophysics. In 1916 he was awarded the degree of Master of Arts in Mathematics, and in 1920 received the degree of Doctor of Science with First Class Honours and the EHO A; COT LO OBITUARY University Medal, for his thesis entitled “‘ Earthquake Frequency with Special Reference to Tidal Stresses in the Lithosphere ’’. He represented the University of Sydney at the First Pan-Pacific Science Congress at Honolulu in 1920, and the Third Congress at Tokyo in 1926; he was also Secretary of the Geology Section at the Second Pan- Pacific Congress which met in Sydney in 1923. He was elected to membership of the Royal Society of New South Wales in 1909, was President in 1929 and served on the Council of the Society for a number of years. During his active geological career, Leo Cotton was a Fellow of the Geological Society of London, A Fellow of the Geological Society of America, and a member of the Linnean Society of New South Wales. He delivered the Clarke Memorial Lecture to the Royal Society in 1946. As a member of the Australian National Research Council, Leo Cotton served on many scientific com- mittees, including those on Seismology and Geodesy and Geophysics. For several years he was an active member of the Editorial Sub-Committee of the parent body, and Chairman of the Council in 1943. Professor Cotton was also actively concerned in the affairs of the Australian Association for the Advancement of Science, being Vice-President of Section C in 1923 (Wellington) and 1924 (Adelaide) and President of the Section in 1928 (Hobart) ; in 1937 he was elected a Fellow of the Association. The distinction of Honorary Membership of the Geological Society of Australia was conferred upon him in 1958. During World War II, Professor Cotton was Chairman of the Advisory Committee on Scientific Manpower (General). The new L. A. Cotton School of Geology of the University of New England, so named in honour of the man and his outstanding contributions to the geological sciences in Australia, was opened by him in 1960, a most fitting tribute to his hfe and work. Florence Channon, whom Leo Cotton married in 1910, died in 1930 leaving with him their three sons and two daughters, consolation and_ responsibility accepted and fulfilled to the utmost of his warm and generous nature. In 1946 he married Lilian Kead, with whom he enjoyed many years of quiet retirement in their home at Newport. Other than family, professional and academic interests, Leo Cotton enjoyed as recreations lawn bowls and chess, at which he was particularly skilled. In both his private and professional life, Leo Cotton was a gentle, most considerate and understanding man, whose friendship and counsel were sought by many and valued most highly by all those who had the privilege of knowing him well. PUBLICATIONS Metasomatic Processes in a Cassiterite Vein from New England. Proc. Linn. Soc. N.S.W., 34, 1909, 220-232. Note on the Guyra Lagoon, N.S.W. Proc. Linn. Soc. N.S.W., 34, 1909, 233-237. The Tin Deposits of New England, N.S.W. Pt. I. The Elsmore-Tingha District. Proc. Linn. Soc. N.S.W., 34, 1909, 733-781. The Ore Deposits of Borah Creek, New England, N.S.W. Proc. Linn. Soc. N.S.W., 35, 1910, 496-520. 225 Note on the Limitations of De Chaulnes’ Method of Determining Refractive Index. A.A.A.S. Report, 13, 1911, 120-124. Some Crystal Measurements of Chillagite. Roy. Soc. N.S.W., 46, 1912, C. D. Smith.) Note on the Relation of the Devonian and Carboniferous Formations West of Tamworth, N.S.W. Proc. Linn. Soc. N.S.W., 37, 1912, 703-708. (With A. B. Walkom.) The Diamond Deposits of Copeton, N.S.W. Proce. Linn. Soc. N.S.W., 39, 1914, 703-838. Some Geophysical Observations at Burrenjuck, N.S.W. J. & Proc. Roy. Soc. N.S.W., 49, 1915, 448-462. Petrological Description of Some Rocks from South Victoria Land. Brit. Antarctic Exped. 1907-09, Repts. on Scientific Investigations (Geol.), II, Pt. 13, 1916, 235-237. The Calculation of Refractive Index J. & Proc. 207-219. (With in Random Sections of Minerals. & Proc. Roy. Soe. N.S.W., 55, 1920, 177-187. (With M. M. Peart.) The Kurrajong Earthquake of August 15, 1919. J. & Proc. Roy. Soc. N.S.W., 55, 1921, 83-104. Report of the Determination of Gravity in Certain Critical Localities Committee. A.A.A.S., 15, 1921, 294-296. Earth Movements at Burrenjuck as Recorded by Horizontal Pendulum Observations. J. & Proc. Roy. Soc. N.S.W., 55, 1921, 143-149. Some Fundamental Problems of Diastrophism and their Geological Corollaries. Pyvocs. lst Pan- Pacific Sci. Conf., Honolulu, III, 1921, 886-888 (Abstract). Seismology in Australia. Pyrocs. lst Pan-Pacific Sct. Conf., Honolulu, II, 1921, 409-410. (With E. F. Pigot.) Report of the Committee for the Study of Earth Movements by Horizontal Pendulum. 4A./4.A.S., 16, 1923, 47. Investigations of Structural Features and Landforms in Australasia: N.S.W. and S.A. Avaya 16, 1923, 58. Earthquake Frequency, with Special Reference to Tidal Stresses in the Lithosphere. Amer. Bull., 12, 1922, 48-198. Some Fundamental Problems of Diastrophism and their Geological Corollaries, with Special Reference to Polar Wanderings. Amer. J. Sct., 1923, 453-503. Notes on the Horizontal Pendulums for the Study of Earth Movements at Burrenjuck. Guide Book, Pan. Pac. Congress, 1923, 32-34. Notes on the Geology of the Yass-Canberra Area. Guide Book, Pan. Pac. Congress, 1923, 27-32. Notes on the Geology of the Canberra Area. Proc. Pan. Pac. Cong., 1923, 2, pt. vi. Notes on the Earthquake at Murrumbateman during March and April, 1924, and January to April, 1925... Js @ Proc. Roy. (Soc. N.S. WW. SoeNO25; 325-328. Age of Certain Radium-Bearing Rocks in Australia. Amer. J. Sct., 12, 1926, 41-46. Pleistocene and Post-Pleistocene Movements of the Strand in Australia. Proc. Pan-Pac. Sci. Cong., 1926, II, 1928, 1777-8. Notes on Relations of Earthquake Frequency and Earth Tides, and Their Significance in Earthquake Forecasting. Proc. Pan-Pac. Sci. Cong., 1926, IT, 1928, 1511-16. Sets... Soc. 226 Causes of Diastrophism and their Status in Current Geological Thowsht., AAA Ss a a9) L928, 171-218. Pre-Cambrian Formations of Australia. Presidential Address, J. & Proc. Roy. Soc. N.S.W., 64, 1930, 10-64. Notes on the Life of a Great Australian Scientist [T. W. E. David.] Aust. Med. Pub. Press, 1934. (With W. R. Browne.) The Constitution of the Earth’s Interior. Sci., 6, 1944, 101-104. The Pulse of the Pacific. Clarke Memorial Lecture. J. & Proc. Roy. Soc. N.S.W., 89, 1946, 41-76. Aust. J. Emeritus Professor Harvey Sutton, O.B.E., M.D., Ch-b boc.) H.K.o.H., FIReA:C.Ps who was formerly Director of the School of Public Health and Tropical Medicine and Professor of Preventive Medicine in the University of Sydney, died at his home in Sydney on 21st June, 1963, at the age of 81. Professor Sutton was born in Victoria. He re- ceived his early education at St. Andrew’s College, Bendigo, and proceeded as a medical student to the University of Melbourne. He graduated M.B., Ch.B. in 1902, having gained honours in every subject and the Scholarship in Pathology. He had a distinguished record as a sportsman, for he excelled in most games. He represented his University in lacrosse, athletics and cricket, and Trinity College in rowing, cricket, football and athletics. At various times he held the University half-mile record, the Victorian and Australasian half-mile and Victorian one mile records. He represented Australia in the 1908 Olympiad in London. Also, he represented Oxford University in lacrosse and athletics. After his graduation Professor Sutton served for two years at the Children’s Hospital, Melbourne, and then gained the Rhodes Scholarship for Victoria. He took up residence at New College, Oxford, in 1906, graduating M.D. before he left Melbourne. At Oxford he spent two years under J. S. Haldane in physiology, gaining a research degree in Science. After a period at Charing Cross Hospital he returned to Melbourne. He had become interested in Public Health, and after qualifying for the D.P.H. he joined the School Medical Service. He became Chief Medical Officer of the Education Department of Victoria and remained in this position until the outbreak of the First World War. He enlisted in the A.I.F. in 1915 and served with the Australian Light Horse in the desert campaigns in Sinai, Palestine and Syria. He was in the hygiene service at first, reaching the rank of major, and was involved in Allenby’s anti-malarial campaign in the Jordan Valley and in the constant fight against epidemic G@ysentery. | Ele: ‘later, "became, (Oo: A.D. Mes” “of tsthe ANZAC Mounted Division. He served with distinc- tion, was awarded the O.B.E., and was twice mentioned in dispatches. On his return from the war Professor Sutton joined the New South Wales Education Department as Principal Medical Officer. He held this position for nine years, and for much of the period he was also part-time Lecturer in Public Health and Preventive Medicine at Sydney University. In 1930 the Commonwealth Government and the University of Sydney jointly founded the School of Public Health and Tropical Medicine. He became OBITUARY Director of the School and at the same time was appointed by the University to the newly founded Chair of Preventive Medicine. He held these positions until retirement in 1947. Professor Sutton’s teaching was enlivened by wide scholarship and was always entertaining. He gradually extended his instruction beyond the undergraduates and post-graduate studies of the Medical School and introduced courses in hygiene and allied subjects in architecture, social studies, education and physical education. He added colour to the place with his open-air classes, held among the rose hedges of the delightful sunken garden he had designed at the School. His interests were wide and extended into the personal, family and social aspects of community health and welfare that are now generally called social medicine. His thinking in this was beyond the environmental sanitation and other activities of the health services of the time—that is, of public health as narrowly defined. This was the new public health of which he was an Australian forerunner. Professor Sutton wrote extensively on a wide range of subjects, especially the development, nutrition, health and welfare of children and young people. Mental hygiene, also the subject of many papers, also claimed his attention and advocacy as both a study and community responsibility. Other publications dealt with climatic physiology, delinquency, alcoholism, public health nursing and the geographical distribution of disease. In 1944 he published a textbook on preventive medicine. Medical history also furnished subjects for a series of papers. His influence extended beyond the University, and he was associated with most of the local community health and welfare movements of his time. He enthusiastically supported numerous voluntary bodies whose objects were social or health improvement, a number of which he helped to found. He accepted this as an important public responsibility, realising that through its channelling of civic thought and enthusiasm the work of such groups often formed the basis and later testing ground of general advances. From his work in the community, his frequent and assertive public statements on health questions, and the numerous popular lectures which it delighted him to give, he became a public figure, and of the University staff was the one perhaps best known to the man in the street. Professor Sutton was elected to membership of the Society in 1920. He is survived by his wife and three sons and four daughters. Thomas Griffith Taylor, Emeritus Professor of Geography of the University of Toronto, Canada, died on 5th November, 1963, at the age of 82. Professor Taylor was born in London, came at the age of 13 with his parents to Sydney, and was educated at Sydney Grammar School, The King’s School, Sydney University and Cambridge University. As Physiographer in the Australian Meteorological Service, he was seconded to Capt. Scott’s Antarctic Expedition in 1910. He was a pioneer of academic geography in three countries. In 1921 he was appointed Associate Professor of Geography in the University of Sydney, in 1928 Professor of Geography in the University of Chicago, and in 1935 Professor of Geography in the University of Toronto, where he remained until retire- ment in 1950. He returned to Sydney and added MEDALLISTS some further publications to his already large tally of books and papers (some 40 of the former). One of these later writings was ‘‘Sydneyside Scenery ”’ which proved very popular with the growing body of lay persons interested in geology and geomorphology. Within his lifetime he was honoured in many ways, notably by the University of New England in naming its new Geography Department after him, and by the University of Sydney which bestowed his name on the 227 fine new building in which the Geography Department is housed. He was a member of the Royal Society of New South Wales in the periods 1921-1928 and 1954-1960 and was a member of its Council. The Society conferred its Medal on him in 1960 in recognition of his outstanding services to science and his work for the Society. Increasing deafness caused him _ to resign from membership in 1960. Medallists, 1964 Clarke Medal for 1964 WOVEE “VICKERY, Disc., M.B-E. Joyce Winifred Vickery, a member of the Society since 1935, was born at Homebush, New South Wales, and educated at the Methodist Ladies’ College, Burwood, and at the University of Sydney, from which she graduated in 1931 as Bachelor of Science with Honours in Botany. She carried out post-graduate work in the Botany Department for the next five years, receiving the degree of Master of Science in 1933 for research on vegetative reproduction in the insecti- vorous genus Dyvoseva and on aspects of grass seed germination. During the next few years three joint papers with Dr. Lilian Fraser on the ecology of the Upper Williams River and Barrington Tops area were published in the Proceedings of the Linnean Society of New South Wales. This is regarded as most important pioneer work on_ subtropical rainforest ecology. A study of comparative anatomy of grass leaves during these years led to the realisation of the need for a thorough taxonomic reinvestigation of the native Gramineae. In August, 1936, Miss Vickery joined the staff of the National Herbarium of New South Wales, where her influence, under the Directorship of Mr. R. H. Anderson, has resulted in a great increase in the quantity and improvement in the standard of taxonomic research as well as in the provision of accurate botanical information to the scientific and general public. Although retaining a wide botanical interest, she has specialised in the taxonomy of Australian grasses, particularly those of her home State, and is known as a foremost authority in this field. This has involved periods of work at the Royal Botanic Gardens, Kew, the United States National Herbarium, Washington, and other institutions abroad. Among her many papers are Australia-wide revisions of Festuca, Deveuxia, Agrostis, Amphipogon and Danthonia, as well as a treatment of the new genus Dryopoa J. Vickery, all published in the Contributions from the New South Wales National Herbarium. In 1959 Joyce Vickery Feceived the degree of Doctor of, Science of the University of Sydney, for her published work on grass systematics and in other fields. Currently, Dr. Vickery, now Special Botanist, is occupied with the continuation of the semi-mono- graphic account of the Gramineae for the new Flora of New South Wales, and is preparing a monograph of the notoriously difficult and ecologically significant genus Poa in Australia. Not least among her achievements has been her generous and enlightening assistance to younger botanists and scientific colleagues in her own institution and elsewhere. Editing of the Flora of New South Wales and contributions to the scientific side of conservation work are also among her notable activities. The Society’s Medal for 1963 PROFESSOR Ronald S. NyvHuoitm, M.Sc., Ph.D., D.Sc. (cond. wok Ae Ca” FRE, Ronald Sydney Nyholm, Professor of Chemistry, University College, London, has been a member of the Society since 1940. He was a member of Council for the years 1944-1948, 1953, and was President in 1954. Professor Nyholm was born at Broken Hill on 29th January, 1917, and was educated at Broken Hill High School, Sydney University and University College, London. He was Lecturer and Senior Lecturer in Chemistry at Sydney Technical College, 1940-1951; I.C.I. Fellowship to London University, 1947 ; and Associate Professor of Inorganic Chemistry, N.S.W. University of Technology, 1952-1954. In 1952 he was awarded the Corday Morgan Medal and Prize of the Chemical Society of London ; in 1955 the H. G. Smith Medal of the Royal Australian Chemical Institute; and he delivered the Chemical Society’s Tilden Lecture in 1950. Professor Nyholm has made many contributions to and greatly increased our understanding of the chemistry of the transition elements, in particular to their stereochemistry, magneto-chemistry and to our knowledge of their unusual oxidation states. Twenty-six of his papers have been published in the Society’s “‘ Journal and Proceedings ’’, and he is one of the contributors to a book entitled “ Chelating Agents and Metal Chelates’”’ (Academic Press) which is an all-Australian effort in a field of chemistry to which Professor Nyholm has also made _ notable contributions. Edgeworth David Medal for 1963 PROFESSOR NEVILLE H. FLETCHER Professor Fletcher is distinguished for his contribu- tions to the physical theory of the solid state. His early work was concerned with the understanding of the behaviour of transistors and other semi-conductor devices and for the last eight years he has carried out theoretical research into the properties of ice, water and related materials, particularly with regard to the nucleation of ice crystals by foreign substances such as silver iodide, and the behaviour of these in “ cloud seeding ’’. Professor Fletcher already has an _ international reputation as a cloud physicist, and his book ‘‘ The Physics of Rainclouds ”’ is regarded as a standard work on the subject. Abstract of Proceedings, 1963 3rd April, 1963 The ninety-sixth Annual and seven hundred and eighty-second General Monthly Meeting was held in the Hall of Science House, Gloucester Street, Sydney, at 7.45 p.m. whe President, Assoc. was in the chair. and visitors. Frederick A. Everett was elected a member of the Society. The Annual Report of the Council and the Financial Statement were presented and adopted. The following awards of the Society were announced : The Society’s Medal for 1962: Mr. Harley Wood. The Clarke Medal for 1963: Dr. Germaine A. Joplin. Prof. W.B. Smith-White; There were present 65 members The Walter Burfitt Prize for 1962: Dr. M. F. Glaessner, F.A.A. The Edgeworth David Medal for 1962: Mr. R. F. Isbell. Office-bearers for 1963-64 were elected as follows: President: H. H. G. McKern, M.Sc. Wiee-Presidénts: |..L. Gritith, BA. Mose. > Ka) y.. LeFevre, DiSc:;. BRS. FAA. WW. HevG: Poggendorff, B.Sc.Agr. ; W. B. Smith-White, M.A. Hon. Secretaries: A. H. Low, Ph.D., M.Sc.; A. A. Day, B.Sc. (Syd.), Ph.D (Cantab.). Hon. Treasurer: C. L: Adamson, B.Sc. Members of Council: Ida A. Browne, D.Sc., H. F. Conaghan,M.Sc., A. G. Fynn, B:5c., N: A.’Gibson; PheD.,. 41. .G. Golding, M:.Sc.,, J: W.. tfumpheres: .o¢;,. A.) seane, | Ph. D.,.)).,. Middlehurst., Mise, iL. stanton,-Ph. Dy, A.-Ungar;, Dr.-Ing: Messrs. Horley & Horley were re-elected as Auditors of the Society for 1963-64. The retiring President, Assoc. Prof. W. B. Smith- White, delivered his Presidential Address entitled ““The Mathematical Sciences in the Changing World ’’. Modern living in advanced civilised countries is dependent on a vast application of the results of scientific study of the natural world. The material necessities, comforts and luxuries of our age derive especially from and are by-products of the study of physics, chemistry and geology, the so-called exact sciences. New developments and new applications mount at a fast growing rate. To keep abreast of this progress and to maintain and service existing and expanding facilities civilised states need a greater and greater proportion of their population trained in numerous special techniques of the most varied kinds. This is possible only on the basis of a general scientific education more widely spread and of greater depth than was ever necessary before. So it is that an ever increasing number of people require a_ scientific education at secondary and tertiary levels. State expenditure in this cause must be seen in a proper perspective. Enormous increases in expenditure cannot be avoided; no state can afford to be parsimonious with the scientific education of its citizens. But states, like individuals, must operate within their means. The money spent must be well spent so as to gain the maximum benefits. Education must be efficient. Students must acquire and retain more or less permanently the principles expounded and the skills taught. All reforms in systems of education are no doubt directed towards gaining greater benefits more efficiently in time and more economically in cost. How can Wwe approximate the best possible results in the domain of the natural sciences? At the conclusion of the address the retiring President welcomed Mr. H. H. G. McKern to the Presidential Chair. Ist May, 1963 The seven hundred and eighty-third General Monthly Meeting was held in the Hall of Science House, Gloucester Street, Sydney, at 7.45 p.m. The President, Mr. H. H. G. McKern, was in the chair. There were present 50 members and visitors. The following were elected members of the Society : Christine Cienska, Bernard Adrian Howe and Eric Leslie Stevens. An address entitled ‘“‘Some Observations on Education in the U.S.S.R.’’ was delivered by A./Prof. J. F. D. Wood, of the School of Mechanical Engineering, the University of New South Wales. The Soviet educational system: its magnitude, past development and future plans, with special reference to tertiary education. The control of education in the U.S.S.R.: All-Union Ministry of Higher Education, Republican Ministries of Education. Secondary education: general and special schools ; boarding schools; part-time schools; selection of pupils; curricula; manual training; matriculation. Trade schools: entrance standard; length of courses ; quality of production. Technical colleges: entrance standards; length of courses ; specialization. Tertiary education : Types of institutions: universities ; institutes ; specialized institutes. Courses provided: entrance standards; nature and length of courses; full-time, part-time, and corres- polytechnic pondence courses; post-graduate work; industrial experience. Student conditions: selection for entry; scholar- ships ; sponsorships; residential facilities ; examina- tions; standards; failure rates; placement of graduates. Staff conditions: selection; promotion; duties; salaries. General conditions: accommodation; equipment. 5th June, 1963 The seven hundred and eighty-fourth General Monthly Meeting was held in the Hall of Science House, Gloucester Street, Sydney, at 7.45 p.m. The senior Vice-President, A./Prof. W. B. Smith- White, was in the chair. There were present 22 members and visitors. John Francis Rigby was elected a member of the Society. An address entitled ‘‘ A World-Wide Standardized Seismograph Network’’ was delivered by Father A. G. Fynn, S.J., Director of the Riverview College Observatory. ABSTRACT OF PROCEEDINGS In April, 1960, a committee of American scientists was established by the National Academy of Sciences National Research Council to advise the United States Government on the establishment of a world-wide network of seismographs. The programme which emerged from their deliberations was handed over to the Coast and Geodetic Survey to be carried out. The purpose of the programme is to encourage and maintain a high degree of international interest and co- operation in the field of seismology with the following immediate aims: (a) A better understanding of the world’s seismicity. This knowledge may ultimately lead to better prediction of destructive earthquakes. (6) Greatly improved knowledge of the Earth’s crust and mantle, with regard to the number, thickness and nature of the major layers therein. (c) Improved knowledge of wave propagation characteristics through the Earth, including the accurate determination of regional travel times. (d) Improved data for comparison of all types of seismic waves. Seismograms, written by identical instruments at 125 carefully chosen points, will be transmitted regularly to a Data Centre to be copied and stored. They will be immediately available for study to the world’s seismologists. 3rd July, 1963 The seven hundred and eighty-fifth General Monthly Meeting was held in the Hall of Science House, Gloucester Street, Sydney. The President, Mr. H. H. G. McKern, was in the chair. There were present 26 members and visitors. The following were elected members of the Society : James Edmund Banfield, Paul Coss, Elizabeth Annette Essex, William Eric Smith and Gilbert Percy Whitley. The Edgeworth David Medal for 1962 was presented to Mr. R. F. Isbell, of C.S.I.R.O., Division of Soils, Cunningham Laboratory, Brisbane, and, following the presentation, Mr. Isbell delivered an address entitled “Land Utilization in Queensland and its relation to Geology, Soil and Climate ”’ With several important exceptions, rural land utilization in Queensland is extensive rather than intensive and this is often due to factors other than physical land resources. However, within this broad scale use framework definite land use patterns are evident and the relative importance of geological, soil and climatic factors were considered in relation to the more important rural industries. The influence of geology lies chiefly in its significance as a soil parent material factor. Soils as such have in some instances determined and delineated certain rural industries but the role of climate is probably of most importance. It is further evident that certain features of the general sub-tropical climate have an important influence on the utilization of many Queens- land soils and provide a marked contrast to southern Australia. 7th August, 1963 The seven hundred and eighty-sixth General Monthly Meeting was held in the Hall of Science House, Gloucester Street, Sydney, at 7.45 p.m. The President, Mr. H. H. G. McKern, was in the chair. There were present 20 members and visitors. 229 The following were elected members of the Society ° Kenneth John Brown, Robert William Minns, Ronald James Huntbatch Morris and John Percival Pollard. An address entitled ‘‘ Stereo-chemistry of Some Non- metallic Elements and Their Compounds ”’ was delivered by Dr. D. P. Graddon, School of Chemistry, the University of New South Wales. The molecular structures of most non-metallic elements can be explained on the basis of the 8-n rule, as can those of their compounds with other elements of low electronegativity. When, however, compounds are formed between non-metals and other elements of high electronegativity, such as fluorine, the electronic structure of the non-metal may be expanded beyond that of the next inert gas and the stereochemistry of the compounds formed is determined by the total number of electrons in the expanded valency shell. Examples of both types of behaviour were discussed and extended to include the chemical behaviour of some of the inert gases themselves. 4th September, 1963 The seven hundred and eighty-seventh General Monthly Meeting was held in the Hall of Science House, Gloucester Street, Sydney, at 7.45 p.m. The President, Mr. H. H. G. McKern, was in the chair. There were present 24 members and visitors. Gregory Doherty was elected a member of the Society. An address entitled ‘“‘ Cotton Production in New South Wales ’”’ was delivered by Mr. T. E. Kitamura, Special Agronomist (Miscellaneous Crops), Department of Agriculture, N.S.W. Cotton seed was among the plant material brought to Australia by Captain Arthur Phillip. Since that time, the plant has been cultivated commercially in this country, principally in Queensland. Although research into the field characteristics and needs of cotton has been conducted over the years by the C.S.I.R.O. and the Queensland and New South Wales Departments of Agriculture, until recently only in Queensland have farmers shown an interest in commercial production. However, during the past five years considerable progress has been made in New South Wales so that in 1962-63 some 2,600 acres of commercial cotton were cultivated. _ Although Australian workers are in the happy position of being able to call upon the vast amount of cotton research already completed on a world-wide scale, the application of this information to irrigated cotton under New South Wales conditions poses problems. The solution of these is now being attempted by Departmental workers. There can be no doubt but that Australia needs this vegetable fibre, nor can there be any question as to the capacity of the environment to support the plant successfully, nor of the ability of farmers to produce it economically. 2nd October, 1963 The seven hundred and eighty-eighth General Monthly Meeting was held in the Hall of Science House, Gloucester Street, Sydney, at 7.45 p.m. The President, Mr. H. H. G. McKern, was in the chair. There were present 56 members and friends. The following were elected members of the Society : Richard Hugh Macdonald Arnot and Edward Charlton Watton. 230 The following papers were read by title only: ““Some Applications of Aerial Photographs to the Solution of Topographic and Cartographic Problems ”’, by A. Di Albani. ~ Petrology in Relation to Road Materials, Part II: The Selection of Rock for Road- making in Australia, with special reference to N.S.W.’’, by E. J. Minty. ‘‘ Minor Planets Observed at Sydney Observatory during 1962’, by W. H. Robertson. A symposium on “Science or Sciences in Schools. Curriculum for an Integrated Science Course in Schools ”’ was held. The speakers were Mr. M. Bishop, Head- master, of Cranbrook School, and Professor C. E. Marshall, Head of the Department of Geology and Geophysics, the University of Sydney. Children of secondary school age ought to be given the chance to become aware of the kind of society to which they belong and of which they will become citizens. Their opportunities, understanding, apprecia- tion and preparedness for change in society are diminished wherever their understanding of science and scientists is restricted. Secondary education today must lead as it did in the past to an instructed elite and more importantly than in the past informed citizen. Science is in its widest sense a humanity and is a compulsory subject under the Wyndham secondary school plan. To achieve the intention of the Wyndham scheme science teachers must think of science as providing for the curriculum; facts—which may be ends in themselves and means to ends; information about men and their activities ; data about the develop- ment and interplay of ideas. This concept of science stresses at the secondary school level the importance of an understanding and feeling for science and qualifies the importance of an isolated understanding of the data and theories of any one individual science. It challenges the science teachers to re-think their roles in education. 6th November, 1963 The seven hundred and eighty-ninth General Monthly Meeting was held in the Hall of Science House, Gloucester Street, Sydney, at 7.45 p.m. The President, Mr. H. H. G. McKern, was in the chair. There were present 26 members and visitors. John Robert Conolly was elected a member of the Society. The following papers were read by title only: ““Depositional Environment and _ Provenance of Devonian and Carboniferous Sediments in_ the famworth Trough, N:S.W., by jh. Ay W.UCrook: “On the Gibbs Phenomenon in n-Dimensional Trans- fonms ~,* by? J. Vle-) Guihith s+. Lepidophioi0s, and Cyrtospirifer from the Lambie Group at Mount Lambie, N.S.W.’’, by Robin M. Mackay ; ‘‘ Devonian Trilobites from the Wellington-Molong District of New South Wales: by Die *Strusz: An address entitled ‘‘ Air Pollution Research and Control in New South Wales’’ was delivered by Dr. MEMBERS OF THE SOCIETY J. L. Sullivan, N.S.W. Department of Public Health, Division of Occupational Health, Air Pollution Control Branch, Sydney. Sydney and other industrial cities on the New South Wales coast are subject to substantial air pollution | problems which, if uncontrolled, could become severe in future years. Rapid industrial development com- bined with prolonged subsidence inversions and the Great Dividing Range are the major factors which contribute to the overall patterns, but more public attention has been directed towards specific area problems. Measurements of various contaminants such as dust-fall, smoke, sulphur dioxide, ozone, polycyclic aromatic hydrocarbons and others have been made in Sydney and elsewhere in New South Wales for several years. Some of these have been made routinely at regular monitoring stations and the results can be correlated with weather patterns and other factors. Control of air pollution is an engineering problem but legislation is needed in order that industry can have a clear definition of its responsibilities. The philosophy of the approach to the implementation of the New South Wales Clean Air Act by the recently formed Air Pollution Control Branch will be to endeavour to obtain compliance with the legislation without resort to litigation. 4th December, 1963 The seven hundred and ninetieth General Monthly Meeting was held in the Hall of Science House, Gloucester Street, Sydney, at 7.45 p.m. The President, Mr. H. H. G. McKern, was in the chair. There were present 50 members and visitors. The following papers were read by title only: “Precise Observations of Minor Planets at Sydney Observatory during 1961 and 1962’’, by W. H. Robertson; ‘“‘ Quaternary Sedimentation by Prior Streams on the Riverine Plain, S.W. of Griffith, INES W:."5 Dy, Ss els: An address entitled ‘‘ Exploration and Development of Australia’s Mineral Resources’’ was delivered by Dr. E. O. Rayner, Assistant Under-Secretary, Depart- ment of Manes; IN.S.W., Sydney: The importance of Australia’s mineral industry and the requirements and outlook for certain minerals were discussed. Discovery of surface deposits is still possible as attested by recent major finds of iron ore and other minerals. However, exploration is largely passing to _ large-scale investigations by companies and governmental organizations. The methods employed were reviewed, with particular reference to the search for sub-surface deposits. Exploration for, and some recent mining develop- ments in, such metals as copper, tin, iron, bauxite, uranium, coal, oil and gas were touched upon, and some examples were illustrated by slides. | | Members of the Society, April, 1964 The year of election to membership and the number of papers contributed to the Society’s Journal are shown in brackets, thus: (1934 ; P8). * indicates Life Membership. Honorary Members BLACKBURN, Sir Charles Bickerton, K.C.M.G., O.B.E., B.A., M.D., Ch.M., Chancellor, University of Sydney. (1960) BRAGG, Sir Lawrence, O.B.E., F.R.S., The Royal Institution of Great Britain, 21 Albermarle Street, Piccadilly, London, W.1, England. (1960) iDURNEL. Sir Frank Macfarlane, O.M., Kt., D:Sc., F.R.S., F.A.A., Director, Walter and Eliza Hall Research Institute, Melbourne. (1949) RATRIEEY, Sir Neil Hamilton, C.B.E., M.D., D.Sc., F.R.S., 73 Harley Street, London, W.1, England. (1951) FIRTH, Raymond William, M.A., Ph.D., Professor of Anthropology, University of London, London School of Economics, Houghton Street, Aldwych, W.C.2, England. (1952) FLOREY, Lord Howard; M.B:, BiS; B:Se., -M.A.; Ph.D., F.R.S., Professor of Pathology, Oxford University, England. (1949) O CONNEEIE ivev. (Daniel . 35: |, .0:5¢.. che F.R.A.S., Director, The Vatican Observatory, Rome, Italy. (1953) OLIPHANT. Sire Marcus 4, KBE. Aen De broce F.R.S., F.A.A., Professor of Physics, Australian National University, Canberra, A.C.T. (1948) ROBINSON, sir Robert, M.A.,.D.sc% EeR.S2 F.C.o. F.1.C., Professor of Chemistry, Oxford University, England. (1948) Members ADAMSON, Colin Lachlan, B.Sc., 9 Dewrang Avenue, North Narrabeen. (1944) Ee DKINS, George Earl, A.S.T.C., C/o School of Mining Engineering, University of N.S.W., Kensington. (1960) *ALBERT, Adrien, D.Sc., F.A.A., Professor of Medical Chemistry, Australian National University, Canberra, A.C.1T..- (1938; P2) ALEXANDER, Albert Ernest, Ph.D., F.A.A., Pro- fessor of Chemistry, University of Sydney. (1950) *ALLDIS, Victor le Roy. (1941) BNDERSON, Geoffrey William, B.Sc., C/o Box 30, P.O., Chatswood. (1948) ANDREWS, Paul Burke, B.Sc., 5 Conway Avenue, Rose Bay. (1948; P2) -ANNISON, Ernest Frank, Ph.D., F.R.I.C., Senior Lecturer in Chemical Pathology, School of Rural Sciences, University of New England, Armidale. (1961) ARNOT, Richard Hugh Macdonald, BoA B.Sc.Agr. (Syd.), Senior Planning Officer, Cumber- land County Council, 274 Kent Street, Sydney. (1963) ASTON, Ronald Leslie, Ph.D., Associate Professor of Geodesy and Surveying, University of Sydney. (1930; President 1948) *AUROUSSEAU, Marcel, M.C., B.Sc., 229 Woodland Street, Balgowlah. (1919; P2) BADHAM, Charles David, M.B., B.S., D.R. (Syd.), M.C.R.A., ‘‘ New Lodge ’’, 16 Ormonde Parade, Hurstville. (1962) BAGNALL, Mary, M.A. (Melb.), Mary White College, University of New England, Armidale. (1961) *BAILEY, Victor Albert, D.Phil., F.A.A., 80 Cremorne | Road, Cremorne. (1924; P3) BAKER, Stanley Charles, Ph.D., Department of Physics, Newcastle University College, Tighe’s Hill. (1934; P4) BAKER, William Ernest, B.Sc.(Hons.), 394 Kaolin Street, Broken Hill, N.S.W. (1962) BANFPIEED, James Edmund, M.Sc. Ph.D (Melb); Department of Organic Chemistry, University of New England, Armidale. (1963) BANKS, Maxwell Robert, B.Sc., Department of Geology, University of Tasmania, Hobart, Tas. (1951) *BARDSLEY, John Ralph, 29 Walton Crescent, Abbotsford. (1919) BASDEN,. Kenneth Spencer, Ph.D, Bsc” Depaa ment of Fuel, University of N.S.W., Kensington. (1951) BAXTER john” Philip, C.VuG., O-6.b eae? F.A.A., Vice-Chancellor and Professor of Chemical Engineering, University of New South Wales, Kensington. (1950) BEAVIS, Margaret, B.Sc., Dip.Ed., 2/94 Beach Street, Coogee. (1961) BECK, Julia Mary (Mrs.), B.Sc., Department of Geophysics, University of Western Ontario, London, Ont., Canada. (1950) BELL, Alfred Denys Mervyn, B.Sc.(Hons.), School of Applied Geology, University of New South Wales, Kensington. (1960) *BENTIVOGLI®, Ssydney - Ermest, Telegraph Road, Pymble. (1926) *BISHOP, Eldred George, 26A Wolseley Road, B.Sc.Agr., 42 Mosman. (1920) BLANKS, Fred Roy, B.Sc., 19 Innes Road, Greenwich. (1948) BLUNT, Michael) Hlugh, M.R.C.V.S., Surgeon, 185 Markham Street, Armidale. Veterinary (1961) 232 BOLT, Bruce Alan, Ph.D., Professor of Seismo- graphic Stations, University of California, Berkeley, U.S.A. (1956; P3) BOOKER, Frederick William, D.Sc., Government Geologist, Geological Survey of N.S.W., Mines Department, Sydney. (1951; PI) BOOTH, Brian Douglas, Ph.D., A58 Telegraph Road, Pymble. (1954) BOSSON, Geoffrey, M.Sc., Professor of Mathematics, University of New South Wales, Kensington. (1951; P2) BRENNAN, Edward, 'B.E. (Appl. Geology), C/o Bee P: | Prospecting Party, Torrington, «via Deepwater, N.S.W. (1962) BREYER Bruno, M.D.,. Ph.D,, Department. of Agricultural Chemistry, University of Sydney. (1946; Pl) BRIDGES, David Somerset, 19 Mount Pleasant Avenue, Normanhurst. (1952) “BRIGGS, George Henry, D:Sce:, 13 Findlay Avenue, Roseville. (1919; Pl) BROWN, Desmond J., D.Sc., Ph.D., Department of Medical Chemistry, Australian National Uni- versity, Canberra, A.C.T. (1942) BROWN, Kenneth John, A:‘S.7:C., A.R.A.CT., 3 Karda Place, Gymea. (1963) BROWNE, Ida Alison, D.Sc., 363 Edgecliff Road, Edgecliff. (1935; P12; President 1953) *BROWNE, William Rowan, D.Sc., F.A.A., 363 Edgecliff Road, Edgecliff. (1913; B23. President 1932) BRYANT, Raymond Alfred Arthur, M.E., Nuffield Professor of Mechanical Engineering, University of New South Wales, Kensington. (1952) BUCKERY, (Windsay sArthur, Se," 9 »«Eulbertie Avenue, Warrawee. (1940) BULLEN,” Keith: "Edward, Sc.D... FURS, .AGAs, Professor of Applied Mathematics, University of Sydney. (1946; P2) BURG, Raymond Augustine, Senior Analyst, Depart- ment of Mines, N.S.W.; p.r. 17 Titania Street, Randwick. (1960) iS WRINS; YBrace Bertram, 5.D:S:, Box 60, Armidale. (1961) BUPLAND,; 'Gilbert James; B2A.,. PhDs EsR-Gis; Professor of Geography, University of New England, Armidale. (1961) CAMERON,. John Craig, M.A., B.Sc. (Edin.), 15 Monterey Street, Kogarah. (1957) CAMPBELL, Ian Gavin Stuart, B.Sc., C/o Barker College, Hornsby. (1955) *CAREY, Samuel Warren, D.Sc., Professor of Geology, University of Tasmania, Hobart, Tas. (1938; P2) CAVILL, George William Kenneth, Ph.D., D.Sc., Professor of Organic Chemistry, University of New South Wales, Kensington. (1944) *CHAFFER, Edric Keith, 27 Warrane Road, Roseville. (1954) CHALMERS, Robert Oliver, Australian Museum, College Street, Sydney... (19335 (Pl) CHAMBERS, Maxwell Clark, B.Sc., 58 Spencer Street, Killara. (1940) CHAPPELL, Bruce William, B.Sc., Geology Depart- ment, Australian National University, Canberra, mG A ( LOGO: Pa) Dentist: “E20: MEMBERS OF THE SOCIETY CHRISTIE, Thelma Isabel, B.Sc., Chemistry School, University of New South Wales, Kensington. (1953) CHURCHWARD, John Gordon, B.Sc.Agr., Ph.D., C/o The Australian Wheat Board, 528 Lonsdale Street, Melbourne, C.1. (1935 732) CIENSKA, Christine, M.Econ. (Warsaw), Librarian, Sydney Technical College, Ultimo ; p.r. Flat 511, 54 High Street, Kirribilli. (1963) CLANCY, Brian Edward, M.Sc., C/o Australian Atomic Energy Commission, Lucas Heights. (1957) COALSTAD, Stanton Ernest, B.Sc., Metallurgical Chemist, 54 Bridge Street, Sydney. (1961) COHEN, Samuel Bernard, M.Sc., 35 Spencer Road, Kallara. (1940) COLE, Edward Ritchie, B.Sc., Associate Professor of Organic Chemistry, University of New South Wales, Kensington. (1940; P2) COLE, Joyce Marie (Mrs.), B.Sc., 7 Wolsten Avenue, Turramurra. (1940; Pl) COLE, Leslie Arthur, 61 Kissing Point Road, Turra- murra. (1948) COLEMAN, Patrick Joseph, Ph.D., Geology Depart- ment, University of Western Australia, Nedlands, W.A. (1955) COLLETT, Gordon, B.Sc., 16 Day Road, Cheltenham . (1940) CONAGHAN, Hugh Francis, M.Sc., Senior Analyst, Department of Mines, N.S.W.; p.r. 104 Lancaster Avenue, West Ryde. (1960) CONOLEY, John Robert, B.S. (eyd.s Ph.D. (N.S.W.), Lamont Geological Observatory, Palisades, N.Y., U.S.A; 3(19637, 320) COOK, Cyril Lloyd, Ph.D., C/o Propulsion Research Laboratories, Box 1424H, G.P.O., Adelaide, S.A. (1948) *COOMBS, F. A., FE.C.S., Bannerman iG@rescenm Rosebery: J(1T9lSs VES) CORBETT, Robert Lorimer, C/o Intaglio Pty. Ltd., Sirius Road, Lane Cove. (1933) CORTIS-JONES, Beverley, M.Sc., 65 Peacock Street, Seaforth. (1940) COSS, Paul, B.Sc., 10 Lucia Avenue, St:-Ives. (1963) CRAWFORD, Edwin John, B.E., ‘‘ Lynwood ”’, Bungalow Avenue, Pymble. (1955) CRAWFORD, Ian Andrew, Cr. Barker and O’Grady Streets, Havenview, via Burnie, Tas. (1955) *CRESSWICK, John Arthur, 101 Villiers Street, Rockdale. (1921; Pl) CROFT, James Bernard, 24 Judson Road, Norman- hurst. (1956) CROOK, Keith Alan Waterhouse, Ph.D., Geology Department, Australian National University, Canberra, A.C.T. (1954; P9) DAVIES, George Frederick, 57 Eastern Avenue, Kingsford. (1952) DAVIS, Gwenda Louise, B.Sc., Ph.D., Associate Professor, Department of Botany, University of New England, Armidale. (1961) DAVIS, Iain Horwood, B.Sc. (Lond.), Department of Geography, University of Queensland, St. Lucia, Brisbane. (1961) DAY, Arthur Alan, Ph.D., Department of Geology and Geophysics, University of Sydney. (1952) DENTON, Leslie A., Bunarba Road, Miranda. (1955) MEMBERS OF THE SOCIETY: 233: DIVNICH, George, Engineer Agronom. (Yugoslavia), Engineering Analyst, 7 Highland Avenue, Punch- bowl. (1960) DOHERTY, Gregory, B.Sc.(Hons.), C/o Australian Atomic Energy Commission, Lucas Heights. (1963) *DONEGAN, Henry Arthur James, M.Sc., Chief Analyst, Department of Mines, N.S.W., C/o Mining Museum, George Street North, Sydney. (1928; Pl; President 1960) DRAKE, Lawrence Arthur, B.A.(Hons.), B.5Sc., Director, Riverview College Observatory, River- view. (1962; P1) DRUMMOND, Heather Rutherford, B.Sc., 2 Gerald Avenue, Roseville. (1950) DULHUNTY, John Allan, D.Sc., Department of Geology and Geophysics, University of Sydney. (1937; P17; President 1947) DURIE, Ethel Beatrix, M.B., Ch.M., Institute of Medical Research, Royal North Shore Hospital, St. Leonards. (1955) EADE, Ronald Arthur, Ph.D., School of Organic Chemistry, University of New South Wales, Kensington. (1945) EDGAR, Joyce Enid (Mrs.), B.Sc., 22 Slade Avenue, Lindfield. (1951) EDGELL, Henry Stewart, Ph.D., Geological Survey of Western Australia, 26 Francis Street, Perth, W.A. (1950) ELKIN, Adolphus Peter, Ph.D., Emeritus Professor, 15 Norwood Avenue, Lindfield. (1934; P2; President 1940) ELLISON, Dorothy Jean, M.Sc., 45 Victoria Street, Roseville. (1949) EMMERTON, Henry James, B.Sc., 37 Wangoola Street, East Gordon. (1940) ENGEL, Brian Adolph, M.Sc., Geology Department, Newcastle University College, Tighe’s Hill, 2N. (1961; Pl) *ESDAILE, Edward William, Arncliffe. (1908) ESSEX, Elizabeth Annette, B.Sc.(Hons.), Physics Department, University of New England, Armidale. (1963) EVERETT, Frederick A., B.Sc. (Syd.), C/o Jannali Boys’ High School, Jannali. (1963) FALLON, Joseph James, 1 Coolong Road, Vaucluse. (1950) FAYLE, Rex Dennes Harris, Pharmaceutical Chemist, 141 Jeffrey Street, Armidale. (1961) PINDLER, Nicholas Victor, B.E.(Hons.), Ph.D., Applied Mathematician, 39 Rembrandt Avenue, Middle Cove. (1962) FISHER, Robert, B.Sc., 3 Sackville Street, Maroubra. (1940) FISHER, Stephen, M.D., B.Sc., Director of Clinical Pathology, Kanematsu Memorial Institute, Sydney Hospital. (1962) FLEISCHMANN, Arnold Walter, Flat 4, 36 Mitchell Street, Bondi. (1956) FLETCHER, Harold Oswald, M.Sc., The Australian Museum, College Street, Sydney. (1933) FLETCHER, Neville Horner, B.Sc., M.A., Ph.D., Professor of Physics, University of New England, Armidale. (1961) 4 Towers Place, FORMAN, Kenn P., C/o 52 Pitt Street, Sydney. (1932) FRENCH, Oswald Raymond, 78 Hercules Street, Dulwich Hill. (1951) FRIEND, James Alan, Ph.D., Department of Chemistry, University of Tasmania, Hobart, Tas. (1944; P2) FURST, Hellmut Friedrich, D.M.D. (Hamburg), 158 Bellevue Road, Bellevue Hill. (1945) FYNN, Anthony Gerard, B.Sc., Director, Riverview College Observatory, Riverview, N.S.W. (1959) GALLOWAY, Malcolm Charles, B.Sc., Geologist, 17 Johnson Street, Chatswood. (1960) GARAN, Teodar, Young Road, Ourimbah. (1952) GARKRREDTRY, ~Michael Duhan, = Dose.) \~ Siutrey, Lodge’’, Mitcham Road, Mitcham, Victoria. (1935; P2) GASCOIGNE, Robert Mortimer, Ph.D., Department of Philosophy, University of New South Wales, Kensington. (1939; P4) GIBSON, Neville Allan, Ph.D., 103 Bland Street, Ashfield. (1942; P6) GILES, Edward Thomas, M.Sc., Ph.D., D.L.C., Poko. »oenior, Lecturer, Department apon Zoology, University of New England. (1961) *GILL, Stuart Frederic, 45 Neville Street, Marrickville. (1947) GLASSON, Kenneth Roderick, B.Sc., Ph.D., 70 Beecroft Road, Beecroft. (1948) GOLDING, Henry George, M.Sc., School of Applied Geology, University of New South Wales, Kensington. (1953; P4) GOLDSTONE, Charles Lillington, B.Agr.Sc., Uni- versity of New South Wales, Kensington. (1951) GORDIJEW, Gurij, Engineer Hydro Geology (Inst. Hydro Meteorology in Moscow, 1936), 41 Abbots- ford Road, Homebush. (1962) GORDON, William Fraser, B.Sc., 10 Warren Road, Double Bay. (1949) GRAHAME, Mervyn Ernest, B.A., Schoolteacher,. 161 Parry Street, Hamilton, N.S.W. (1959) GRANT, John Narcissus Guerrato, Dip.Eng., 37 Chalayer Street, Rose Bay. (1961) GRAY, Charles Alexander Menzies, B.E., M.E. (Syd.), Professor of Engineering, Wollongong University College, Wollongong. (1948; Pl) GRAY, Noel Mackintosh, B.Sc., 1 Centenary Avenue, Hunters ball. (1952) GRIFFIN, Russell John, B.Sc., C/o Department of Mines, N.S.W., Sydney. (1952) GRIFFITH, James Langford, B.A., M.Sc., School of Mathematics, University of New South Wales, Kensington. (1952; P14; President 1958) GRODEN, Charles Mark, M.Sc., School of Mathe- matics, University of New South Wales, Ken- sington. (1957; P3) GUTMANN, Felix, Ph.D., Associate Professor of Physical Chemistry, University of New South Wales, Kensington. (1946; Pl) GUTSCHE, Herbert William, B.Sc., Research Assistant, Geology Department, University of New England, Armidale. (1961) HALL, Norman Frederick Blake, M.Sc., 16A Wharf Road, Longueville. (1934) HAMPTON, Edward John William, 1 Hunter Street, Waratah, 2N, N.S.W. (1949) Y34 HANCOCK, Harry Sheffield, M.Sc., 21 Constitution Road, Dulwich Hill. (1955) HANLON, Frederick Noel, B.Sc., 4 Pearson Avenue, Gordon. (1940; P14; President 1957) HARPER, Arthur Frederick Alan, M.Sc., National Standards Laboratory, University Grounds, City Road, Chippendale. (1936; Pl; President 1959) HARRIS, Clive Melville, Ph.D., Associate Professor, School of Inorganic Chemistry, University of New South Wales, Kensington. (1948; P6) HARRISON, Ernest John Jasper, B.Sc., C/o N.S.W. Geological Survey. Mines Department, Sydney. (1946) HAWKINS, Cedric Arthur, B.Sc.Agr., Chemists’ Branch, : N:S.W. Department, of Agriculture, Victoria Road, Rydalmere. (1956; P38) SHAY ES Daphne, (Mrs.), B.Sc; 98 “Lang | Koad, Centennial Park. (1943) HIGGS, Alan Charles, C/o Colonial Sugar Refining Co. Ltd., Building Material Division, 1-7 Bent Street, Sydney. (1945) HiMineDorothy, D.sc., F.A.A., Professor, Department of Geology, University of Queensland, St. Lucia, Brisbane. (1938; P6) *HOGARTH, Julius William, B.Sc., Unit 4, “ Hills- more ’’, 20 Joubert Street, Hunter’s Hill. (1948 ; P6) HOLM, Thomas John, 524 Wilson Street, Redfern. (1952) HORNE, Allan Richard, 7 Booralee Street, Botany. (1960) HOSKINS, Bernard Foster, B.Sc., .Cjo Chemical Crystallography Laboratory, South Parks Road, Oxford, England. (1959) HOWE, Bernard Adrian, c/o Exploration Physics, 265 Old Canterbury Road, Dulwich Hill. (1963) EU MEER LES, ? john. *Walliam, “B:Se | Physicist, National Standards Laboratory, University Grounds, City Road, Chippendale. (1959 ; President 1964) Tip waNES, Harold John; IDsc.Agr,. Director, Nis WwW. Department of Agriculture, Sydney. (1923; P3) TREDALE, Thomas, D.Sc: 8—-Nulla*-Nulla Street, Turramurra. (1943) IZSAK, Dennis, 5 Ormond Gardens, Coogee. (1961) JACKSON, Robert) “James,” MA A(@Oild))) > Mabe Ch.M. (Syd.), Medical Practitioner, 132 Faulkner Street, Armidale. (1961) JAEGER, John, Conrad, D.Sc:, E.A.A,, Geophysics Department, Australian National University, Canberra, A.C. 1. (19425, Py) JAMIESON, Helen Campbell, 3 Hamilton Street, Coogee. (1951) JENKINS, Thomas Benjamin Huw, Ph.D., Depart- ment of Geology and Geophysics, University of Sydney. (1956) JONES, James Rhys, 25 Boundary Road, Mortdale. (1959) JOPLIN, Germaine Anne, D.Sc., Geophysics Depart- ment, Australian National University, Canberra, Ano. Te e(l93o5) 9) KEANE, Austin, Ph.D., Professor of Mathematics, Wollongong University College. (1955; P4) KEMP, William Ronald Grant, B.Sc., Physicist, 16 Fig Tree Street, Lane Cove. (1960) ABSTRACT OF PROCEEDINGS *KENNY, Edward Joseph, 65 Park Avenue, Ashfield. (1924; Pl) KIMBLE, Frank Oswald, 31 Coronga Crescent, Killara. (1948) KIMBLE, Jean Annie, B.Sc., 383 Marrickville Road, Marrickville. (1943) *KIRCHNER, William John, B.Sc., 18 Lyne Road, Cheltenham. (1920) KITAMURA, . Torrence ~/Edward) By (tionus,), B.Sc.(Agr.), Special Agronomist, N.S.W. Depart- ment of Agriculture, Sydney. (1964). KOCH, Leo E., D.Phil.-Habil., School of Applied Geology, University of New South Wales, Kensington. (1948) KRYSKO v. TRYST, Moiren (Mrs.), School of Applied Geology, University of New South Wales, Kensington. (1959) LAMBETH, Arthur James, s5'Se,) Talanea se Picton Road, Douglas Park, N.S.W. (1939; P3) LANDECKER, Kurt, D.Ing. (Berlin), Department of Physics, University of New England. (1961) LANG, Thomas Arthur, M.C.E., Bechtel Corporation, 537 Market Street, San Francisco 5, California, U.S.Ay (1955) LAWRENCE, Laurence James, Ph.D., Associate Professor, School of Applied Geology, University of New South Wales, Kensington. (1951; P38) LEACH, Stephen Laurence, B.Sc., C/o Taubmans Industries Ltd., P.O. Box 91, Chatswood. (1936) LEAVER,-,Gaynor Eiluned (Mrs.); “B.se.(Wales), F.G.S. (Lond.), 30 Ingalara Avenue, Wahroonga. (1961) LE FEVRE, Raymond James Wood, D.Sc., F.R.S., F.A.A., Professor and Head of the School of Chemistry, University of Sydney. (1947; P2; President 1961) LEMBERG, Max Rudolph, D.Phil., F.R.S., F.A.A., Assistant Director, Institute of Medical Research, Royal North Shore Hospital, St. Leonards. (1936; P3; President 1955) LESLIE, Rupert Thomas, M.A.,, Ph.D., Statistician National Standards Laboratory, University Grounds, City Road, Chippendale. (1960) LEWIS, Philip Ronald, J.P., Design Engineer, 13 River View Road, Woolooware. (1962) *LIONS, Francis, Ph.D., Department of Chemistry, University of Sydney. (1929; P56; President 1946) LIONS, Jean Elizabeth (Mrs.), B.Sc., 160 Alt Street, Haberfield. (1940) LLOYD, James Charles, B.Sc., C/o N.S.W. Geological Survey, Mines Department, Sydney. (1947) LOCKWOOD, William Hutton, B.Sc., C/o Institute of Medical Research, Royal North Shore Hospital, St. Leonards. (1940; Pl) LOVERING, John Francis, Ph.D., Department of Geophysics, Australian National University, Canberra, A.C.T. (1951; P3) LOW, Angus Henry, Ph.D., Department of Applied Mathematics, University of Sydney. (1950; P2) LOWENTHAL, Gerhard, Ph.D., M.Sc., 17 Gnarbo Avenue, Carss Park. (1959) LYONS, Lawrence Ernest, Ph.D., Professor of Chemistry, University of Queensland, St. Lucia, Brisbane. (1948; P2) MEMBERS OF THE SOCIETY MACCOLL, Allan, M.Sc., Department of Chemistry, University College, Gower Street, London, W.C.1, England. (1939; P4) McCARTHY, Frederick David, Dip.Anthr., Principal, Institute of Aboriginal Studies, Box 553, City P.O., Canberra, A.C.T. (1949; Pl; President 1956) McCLYMONT, Gordon Lee, B.V.Sc., Ph.D., Professor of Rural Science, University of New England. (1961) McCOY, William Kevin, C/o Mr. A. J. McCoy, 4 Hall Avenue, Thornleigh. (1943) McCULLAGH, Morris Behan, 23 Wallaroy Road, Edgecliff. (1950) McELROY, Clifford Turner, Ph.D., M.Sc., School of Applied Geology, University of New South Wales, Kensington. (1949; P2) McGREGOR, Gordon Howard, 4 Maple Avenue, Pennant Hills. (1940) McKAY, Maxwell Herbert, M.A., School of Mathe- matics, University of New South Wales, Kensington. (1956; P1) McKERN, Howard Hamlet Gordon, M.Sc., Senior Chemist, Museum of Applied Arts and Sciences, Harris Street, Broadway, Sydney. (1943; P10; President 1963) McMAHON, Barry Keys, B.Sc., 2 Bella Vista, N.S.W. (1961) McMAHON, Patrick Reginald, Ph.D., Professor of Wool Technology, University of New South Wales, Kensington. (1947) McNAMARA, Barbara Joyce (Mrs.), M.B., B.S., 167 John Street, Singleton, N.S.W. (1943) MACKAY, Robin Marie, B.Sc., Department of Geology and Geophysics, University of Sydney. (1962) MAGEE, Charles Joseph, D.Sc.Agr., Division of Science Services, N.S.W. Department of Agri- culture, Victoria Road, Rydalmere. (1947; Pl; President 1952) MALES, Pamela Ann, 13 Gelding Street, Dulwich Hill. (1951) MARSDEN, Joan Audrey, 203 West Street, Crow’s Nest. (1955) MARSHALL, Charles Edward, D.Sc., Professor of Geology and Geophysics, University of Sydney. (1949; Pl) MEARES, Harry John Devenish, 27 Milray Avenue, Wollstonecraft. (1949) *MELDRUM, Henry John, B.Sc., 116 Sydney Road, Fairlight. (1912) *MELLOR, David Paver, D.Sc., Professor of Inorganic Chemistry, University of N.S.W., Kensington. (1929; P25; President 1941) PO DLERURST, Jack, M.Sc., C.S.I.R.O., Division of Food Preservation, Delhi Road, North Ryde. Peter Place, (1960) MILLERSHIP, William, M.Sc., 18 Courallie Avenue, Pymble. (1940) MINNS, Robert William, Industrial Chemist, C/o @. Ts Lempriere & Co. Ltd., Box. 117, G.P.O., Sydney. (1963) MINTY, Edward James, M.Sc., B.Sc., Dip.Nd,, 2 Dowel Street, Chatswood. (1951; P2) MORGAN, Jascha Ann, M.Sc., Department of ee University of New England, Armidale. 1961) 235 MORRIS, Ronald James Huntbatch, M.Sc. (Melb.), Department of Physiology, University of New England, Armidale. (1963) *MORRISON, Frank Richard, 4 Mona _ Street, Wahroonga. (1922; P34; President 1950) MORRISSEY, Matthew John, M.B., B.S., 152 Marsden Street, Parramatta. (1941) MORT, Francis George Arnot, 29 Preston Avenue, Fivedock. (1934) MOSHER, Kenneth George, B.Sc., 9 Yirgella Avenue, Killara. (1948) MOSS, Francis John, M.B., B.S., 37 Avenue Road, Mosman. (1955) MOYE, Daniel George, B.Sc., Chief Geologist, C/o Snowy Mountains Hydro Electric Authority, Cooma, N.S.W. (1944) MULHOLLAND, Charles St. John, B.Sc., 5 Garth- owen Avenue, Lane Cove. (1946) *MURPHY, Robert. Kenneth, Dr.Ing.Chem., © 68 Pindari Avenue, North Mosman. (1915) MURRAY, Patrick Desmond Fitzgerald, D.Sc., F.A.A., Department of Zoology, University of New England, Armidale. (1950) NASHAR, Beryl, Ph.D., 23 Morris Street, Mayfield West, 2N, N.S.W. (1946; P2) NAYLOR, George Francis King, Ph.D., Department of Psychology and Philosophy, University of Queensland, St. Lucia, Brisbane. (1930; P7) *NEUHAUS, John William George, 32 Bolton Street, Guildford. (1943) NEWMAN, Ivor Vickery, Ph.D., Botany Department, University of Sydney. (1932) NEWMAN, Thomas Montague, Flat 9, ‘“‘ Red Hill Court’’, Monaro Crescent, Red Hill, A.C.T. (1962) NOAKES, Lyndon Charles, B.A., C/o Bureau of Mineral Resources Geology and Geophysics, Canberra, A.C.T. (1945; Pl) *NOBLE, Robert Jackson, Ph.D., 324 Middle Harbour Road, Lindfield. (1920; P4; President 1934) NYHOLM, Ronald Sydney, D.Sc., F.R.S., Professor of Inorganic Chemistry, University College, Gower Street, London, W.C.1, England. (1940; P26; President 1954) O’FARRELL, Antony Frederick Louis, A.R.C.Sc., B.Sc., Professor of Zoology, University of New England, Armidale. (1961) OLD, Adrian Noel, B.Sc.Agr., Chemist, N.S.W. Department of Agriculture, Victoria Road, Rydalmere. (1947) OXENFORD, Reginald Augustus, B.Sc., 75 Alice Street, Grafton. (1950) PACKHAM, Gordon Howard, Ph.D., Department of Geology and Geophysics, University of Sydney. (1951; P4) *PENFOLD, Arthur Ramon, Flat 516, Baroda Hall, 6A Birtley Place, Elizabeth Bay. (1920; P82; President 1935) PERRY, Hubert Roy, B.Sc., 74 Woodbine Street, Bowral, 15, N.S.W. (1948) PHILLIPS, Marie Elizabeth, Ph.D., Soils Conserva- tion Section, ~S.M).H.E.A., Cooma, N.S:W-- p.r. 4 Morella Road, Clifton Gardens. (1938) PHIPPS, Charles Verling Gayer, Ph.D., Department of Geology and Geophysics, University of Sydney. (1960) 236 PINWILL, Norman, B.A., The Scots College, Victoria Road, Bellevue Hill. (1946) PLUMMER, Brian Alfred George, M.A*, F.G:S;, Department of Geography, University of New England, Armidale. (1961) POGGENDORFF, Walter Hans George, B.Sc.Agr., Chief, Division of Plant Industry, N.S.W. Department of Agriculture, Victoria Road, Rydalmere. (1949) POLLARD, John Percival, Dip.App.Chemistry (Swinburne), Mathematician with Australian Atomic Energy Commission; p.r. 25 Nabiac Avenue, Gymea. (1963) *POWELL, Charles Wilfred Roberts, 1127 Barrenjoey ifroad, Palm Beach;- (1921; P2) *PRICE, Wiliam. Lindsay, B.Sc., 107 Spring Street, Killara. (1927) PRIDDLE, Raymond Arthur, Crescent, Pymble. (1956) PRIPSMLEY, John Henry, M.B:, B:S!;iB.Sc., Medical Practitioner, 137 Dangar Street, Armidale. (1961) PROKHOVNIK, Simon Jacques, B.A., B.Sc., School of Mathematics, University of New South Wales. (1956; P38) *PROUD, John Seymour, B.E., Finlay Road, Turra- murra. (1945) PULTOCK, Maurice’ James, .Sc.(Fng.),. A:inst.2. Principal Research Officer, C.S.I.R.O., Sydney ; p.r. 2 Montreal Avenue, Killara. (1960) PYLE, John Herbert, B.Sc., Analyst, Mines Depart- ment, Sydney. (1958) *QUODLING, Florrie Mabel, B.Sc., Geology Depart- ment, University of Sydney. (1935; P4) RADE, Janis, M.Sc., Box 28A, 601 St. Kilda Road, Melbourne. (1953; P4) tRAGGAT DL, Sir Harold’ George, -Kt.,-C.B.E., D.Sc, F.A.A., Secretary, Department of National Development,” Acton; Canberra: vA-C. 1. (19227, P8) RAMM, Eric John, Experimental Officer, Australian Atomic Energy Commission, Lucas Heights, N.S.W. (1959) *RANCLAUD, Archibald Boscawen Boyd, B.E., 79 Frederick Street, Merewether, N.S.W. (1919; P3) RAYNER, Jack Maxwell, B.Sc., Director, Bureau of Mineral Resources, Canberra, A.C.T. (1931; PI) READ}. Harold Walter; B.Sc (B:EUP) Prospecting Party, Groote Eylandt, N.T. (1962) REICHEL, Alex, Ph.D., M.Sc., Department of Applied Mathematics, University of Sydney. (1957; P4) RIGBY, John Francis, B.Sc. (Melb.), Geology Depart- ment, Newcastle University College, Tighe’s Hill, 2N, N.S.W. (1963) RIGGS, Noel Victor, B.Sc. (Adel.), Ph.D. (Cantab.), F.R.A.C.I., A/Professor of Organic Chemistry, University of New England, Armidale. (1961) RITCHIE, Arthur Sinclair, M.Sc., Senior Lecturer in Geology, Newcastle University College, Tighe’s Hill, 2N, N.S.W. (1947; P2) RITCHIE, Ernest, D.Sc., F.A.A. Chemistry Depart- ment, University of Sydney. (1939; P19) B.E., 7 Rawson MEMBERS. OF THE SOCIETY ROBBINS, Elizabeth Marie (Mrs.), M.Sc., Waterioo Road, North Ryde. (1939; P3) ROBERTS, Herbert Gordon, C/o Bureau of Mineral Resources, Childers Street, Turner, Canberra, ALC. dee (1957) ROBERTS, John, Ph.D., Bureau of Mineral Resources, Childers Street, Turner, Canberra, A.C.T. (1961 ; P2) ROBERTSON, William Humphrey, B.Sc., C/o Sydney Observatory, Sydney. (1949; P20) ROBINSON, David Hugh, 12 Robert Road, West Pennant Hills. (1951) ROSENBAUM, Sydney, 5 Eton Road, Lindfield. (1940) ROSENTHAL-SCHNEIDER, Ilse, Ph.D., 48 Cambridge Avenue, Vaucluse. (1948) ROSS, Victoria (Mrs.), B.Sc.(Hons.), 26 Gold Street, Blakehurst. (1960) ROUNTREE, Phyllis Margaret, D.Sc., Royal Prince Alfred Hospital, Sydney. (1945) ROYLE, Harold George, MB.) BiSa(Syd.)) 16h Rusden Street, Armidale. (1961) RYAN, D. J., School of Anthropology, University of Western Australia, Nedlands, W.A. (1959) *SCAMMELL, Rupert Boswood, B.Sc., 10 Buena Vista Avenue, Clifton Gardens. (1920) SCHOLER, Harry Albert Theodore, M.Eng., Civil Engineer, C/o Harbours and Rivers Branch, Public Works Department, N.S.W., cnr. Bridge and Phillip Streets, Sydney. (1960) SEE, Graeme Thomas, B.Sc., School of Applied Geology, University of New South Wales, Kensington. (1949) SELBY, Edmond Jacob, Box 175D, G.P.O., Sydney. (1933) *SHARP, Kenneth Raeburn, B.Sc., (C/o Smo E. Ae Cooma, N.S.W. (1948) SHERRARD, Kathleen Margaret (Mrs.), 43 Robertson Road, Centennial Park. P6) SHERWOOD, Arthur. Alfred, B.Sei(zug)) Cla Department of Mechanical Engineering, Uni- versity of Sydney; p.r. 9 Whitton Road, Chatswood. (1959; P1) SIMMONS, Lewis Michael, Ph.D., C/o The Scots M.Sc., (1936 ; College, Victoria Road, Bellevue Hill. (1945; P3) SIMONETT, David Stanley, Ph.D., Assistant Professor of Geography, University of Kansas, Lawrence, Kansas, U.S.A. (1948; P8) SIMS, Kenneth Patrick, B.Sc., 24 Catherine Street, St. Ives. (1950; P10) SLADE, George Hermon, B.Sc., C/o W. Hermon Slade & Co. Pty. Ltd., Mandemar Avenues Homebush. (1933) SLADE, Milton John, B.Sc., 20 Dobie Street, Grafton. (1952) SMITH, Ann Ruth (Mrs.), B.Sc., Box 134, P.O. Queenstown, Tasmania. (1959) SMITH, Glennie Forbes, B.Sc., Queenstown, Tasmania. (1962) SMITH, Roger Albert Alfred, 62 Budyan Road, Gray’s Point. (1960) SMITH, William Eric, M.Sc. (Syd.), B.Sc. (Oxon.), School of Applied Mathematics, University of New South Wales, Kensington. (1963) Box 134, P.O. MEMBERS OF THE SOCIETY SMITH-WHITE, William Broderick, M.A., Associate Professor, Department of Mathematics, University of Sydney. (1947; P3; President 1962) SOMERVILLE, Jack Murielle, M.A., D.Sc., Professor of Physics, University of New England, Armidale. (1959) SOURRY, Charles, Laboratory Manager, Zoology Department, University of New England, Armidale. (1961) *SOUTHEE, Ethelbert Ambrook, O.B.E., M.A., Trelawney Street, Eastwood. (1919) SPITZER, Hans, Dr.Phil. (Vienna), Senior Research Chemist, Monsanto Chemicals (Aust.) Ltd., Rozelle ; p.r. 35 Redan Street, Mosman. (1961) STANTON, Richard Limon, Ph.D., Associate Pro- fessor, Geology Department, University of New England, Armidale. (1949; P2) STAPLEDON, David Hiley, B.Sc., 61 Francis Street, Brighton, South Australia. (1954) *STEPHENS, Frederick G. N., M.B., Ch.M., 133 Edinburgh Road, Castlecrag. (1914) STEPHENS, James Norrington, M.A. (Cantab.), University of New South Wales, Broken Hill Division, Argent Street, Broken Hill. (1959) STEVENS, Eric Leslie, B.Sc., Lot 17, Chaseling Avenue, Springwood. (1963) STEVENS, Neville Cecil, Ph.D., Geology Department, University of Queensland, Brisbane. (1948 ; P5) STOCK, Alexander, D.Phil., Ph.D., Associate Pro- fessor of Zoology, University of New England, Armidale. (1961) STOKES, Robert Harold, Ph.D., D.Sc., F.A.A., 45 Garibaldi Street, Armidale. (1961) *STONE, Walter George, 26 Rosslyn Street, Bellevue EG) (1916 5: Pl) STRUSZ, Desmond Leslie, Ph.D., B.Sc., Department of Geology, University College of Townsville, Pimlico, Townsville. (1960; P1) STUNTZ, John, B.Sc., 511 Burwood Road, Belmore. (1951) *SUTHERLAND, George Fife, A.R.C.Sc., 47 Clan- william Street, Chatswood. (1919) SWANSON, Thomas Baikie, M.Sc., C/o Technical Service Department, ICIANZ, Box 1911, G.P.O., Melbourne. (1941; P2) SWINBOURNE Ellice Simmons, Ph.D., 69 Peacock Street, Seaforth. (1948) MAYLOR, Brigadier Harold B., M.C., D.Sc., 12 Wood Street, Manly. (1915; P3) TAYLOR Nathaniel Wesley, M.Sc. (Syd.), ib D.(N.E.), - Department of Mathematics, University of New England, Armidale. THEW, Raymond Farly, 88 Braeside Wahroonga. (1955) THOMAS, Penrhyn Francis, Suite 22, 3rd Floor, 29 Market Street, Sydney. (1952) THOMSON, David John, B.Sc., Geologist, 61 The Bulwark, Castlecrag. (1956) THOMSON, Wivian Endel, B.sc., Cfo S.M.H.E.A., Geological Laboratory, Scientific Services Division, Cooma North, N.S.W. (1960) (1961) Street, 237 THWALIE. Eric Graham, B:Sc., West Ryde. (1962) THURSTAN, Arthur Wyngate, A.S.T.C., A.R.A.C.L., Metallurgist, 99 Stoney Creek Road, Beverly Hills. (1964) TICHAUEBK, Erwin Kk., D.Se.(dech.), Dipl.ing,, Department of Industrial Engineering, Texas College, Lubbock, Texas, U.S.A. (1960) TOMPKINS, Denis Keith, Ph.D., M.Sc., C/o Depart- ment of Geology and Geophysics, University of Sydney. (1954; Pl) TOW, Aubrey James, M.Sc., C/o Community Hospital, Canberra, A.C.T. (1940) TREBECK, Prosper Charles Brian, 54 Great North Road, Fivedock. (1949) UNGAR, Andrew, Dr.Ing., 6 Ashley Grove, Gordon. (1952) VALLANCE, Thomas George, Ph.D., Department of Geology and Geophysics, University of Sydney. (1949; Pl) VAN DIJK, Dirk Cornelius, D.Sc.Agr., 2 Lobelia 8 Allars Street, Street, O’Connor, Canberra, A.C.T. (1958) VEEVERS, John James, Ph.D., C/o Bureau of Mineral Resources, Canberra, A.C.T. (1953) VERNON, Ronald Holden, M.Sc., Department of Geology and Geophysics, University of Sydney. (1958; Pl) VICKERY, Joyce Winifred, M.B.E., D.Sc., 17 The Promenade, Cheltenham. (1935) VOISEY, Alan Heywood, D.Sc., Professor of Geology and Geography, University of New England, Armidale. (1933; P11) *VONWILLER, Oscar U., B.Sc., Emeritus Professor, Rathkells, Kangaroo Valley, N.S.W. (1903; P10; President 1940) WALKER, Donald Francis, 13 Beauchamp Avenue, Chatswood. (1948) WALKER, Patrick Hilton, M.Sc.Agr., Research Officer, C.S.I.R.O., Division of Soils, Canberra, A.C.T. (1956; P38) *WALKOM, Arthur Bache, D.Sc., 5/521 Pacific Highway, Killara. (1919 and previous member- ship 1910-1913; P2; President 1943) WARD, Judith (Mrs.), B.Sc., 50 Bellevue Parade, New Town, Hobart, Tasmania. (1948) *WARDLAW, Hy. Sloane Halcro, D.Sc., 71 McIntosh Street, Gordon. (1913; P5; President 1939) *WATERHOUSE, Lionel Lawry, B.E., 42 Archer Street, Chatswood. (1919; Pl) *WATERHOUSE, Walter L., C.M.G., M.C., D.Sc.Agr., F.A.A., 30 Chelmsford Avenue, Lindfield. (1919; P7; President 1937) *WATT, Sir Robert Dickie, M.A., Emeritus Professor, 5 Gladswood Gardens, Double Bay. (1911; Pl; President 1925) WATTON, Edward Charlton, B.Sc.(Hons.), A.S.T.C., 2/116 Maroubra Road, Maroubra. (1963) *WATTS, Arthur Spencer, ‘‘ Araboonoo ’’, Glebe Street, Randwick. (1921) WENHAM, Russell George, B.Sc., B.E., 17 Fortescue Street, Bexley North. (1960) WEST, Norman William, B.Sc., C/o Department of Main Roads, Sydney. (1954) 238 MEMBERS OF THE SOCIETY WESTHEIMER, Gerald, Ph.D., University of California, School of Optometry, Berkeley 4, California, U.S.A. (1949) WHITLEY, Alice, Ph.D., 39 Belmore Road, Burwood. (1951) WHITLEY, Gilbert. Percy,. F.Jk:Z-S.,, Gurator) ot Fishes, Australian Museum, College Street, Sydney. (1963) WHITWORTH, Horace Francis, M.Sc., C/o Mining Museum, George Street North, Sydney. (1951 ; PA) WILKINS, Coleridge Anthony, Ph.D., M.Sc., Mathe- matics Department, Auckland University, Auckland, N:Z. (1960; PI) WILKINSON, John Frederick George, M.Sc. (Q’land), Ph.D. (Cantab.), A/Professor of Geology, Uni- versity of New England, Armidale. (1961) WILLIAMS, Benjamin, 12 Cooke Way, Epping. (1949) WILLIAMSON, William Harold, M.Sc., 6 Hughes Avenue, Ermington. (1949) WILSON, Peter Robert, Ph.D., B.A., M.Sc., Lecturer in Applied, Mathematics, University of Sydney. (1959) WOOD, Clive Charles, Ph.D., B.Sc., 60a Pleasant Road, East Hawthorn, Victoria. (1954) WOOD, Harley Weston, D.Sc., M.Sc., Government Astronomer, Sydney Observatory, Sydney. (1936; P14; President 1949) WRIGHT, Anthony James, B.Sc., Department of Geology and Geophysics, University of Sydney. (1961) WYLIE, Russell George, “Ph: D2 Wise® Physicicm 11 Church Street, Randwick. (1960) WYNN, Desmond Watkin, B.Sc., C/o Mines Depart- ment, Sydney. (1952) YATES, Harold, M.Se*(Sydvy 102 Ballarat, Victoria. (1962) YEATES, Neil Tolmie McRae, D.Sc.Agr. (QO’land)j Ph.D. (Cantab.), A/Professor of Livestock Husbandry, University of New England, Armidale. (1961) Eyre Street Associates BARNET, Michael Terence, 37 Queen Street, Revesby. (1961) - BURNS, Susan Mary (Mrs.), P.O. Box 60, Armidale. (1961) CRUIKSHANK, Bruce Ian, 16 Arthur Street, Punchbowl. (1961) DENTON, Norma (Mrs.), Bunarba Road, Miranda. (1959) DONEGAN, Elizabeth (Mrs.), 18 Hillview Street, Sans Souci. (1956) GRIFFITH, Elsie A: (Mrs.), 9 Kanoona Street, Caringbah. (1956) MEAVER, Harry, 3s4.,. 15:5¢e,,- MIB, Cai: MAR;C.0.G., BGS. 30. Imgalara “Avene, Wahroonga. (1962) LE FEVRE, Catherine Gunn, D.Sc. (Lond.), 6 Aubreg Road, Northbridge. (1961) McCLYMONT, Vivienne Cathryn, Street, Armidale. (1961) MORGAN, James Albert, 354 MRobertson Road, Centennial Park. (1961) ROSENTHAL, Hans Samuel Arthur, Dr.Ing. (Berlin), Consulting Engineer, 48 Cambridge Avenue, B.Sc., Handel Vaucluse. (1961) SHERWOOD, Joan (Mrs.), 9 Whitton Roag Chatswood. (1962) STANTON, Alison Amalie (Mrs.), B.A., 35 Faulkner Street, Armidale. (1961) STOKES, Jean Mary (Mrs.), M.Sc., 45 Garibaldi Street, Armidale. (1961) Obituary, 1962-63 Adolph BOLLIGER (1933) Anthony DADOUR (1940) Francis F. P. DWYER (1934) Burnett MANDER-JONES (1960) Obituary, 1963-64 Richard C: L. BOSWORTH (1939) Leo Arthur COTTON (1909) Franch LEECHMAN (1957) Harvey SUTTON (1920) Thomas Griffith TAYLOR (1954,previous membership 1921-28) Medals, Memorial Lectureships and Prizes awarded by The Society The James Cook Medal A bronze medal awarded for outstanding contributions to science and human welfare in and for the Southern Hemisphere. 1947 J. C. Smuts (South Africa) 1954 Sir F. M. Burnet (Australha) 1948 B. A. Houssay (Argentina) 1955 A. P. Elkin (Australia) 1950.> Sir N.-H. Fairley (U.K.) 1956 Sir I. Clunies Ross (Australia) 1951 N. McA. Gregg (Australia) 1959 -Si Bridges. Business: Symposium on “‘Spilites’’, speakers being Dr. T. G. Vallance and Dr. W. R. Browne. Abstracts : Dro 1. G. Vallance: “From spilite, as originally defined (by Brongniart, ca. 1815), two traditions are derived—neither now close to the original. The first is that still found in parts of Europe where spilite is recognized as a fine-grained non-porphyritic basalt. The other view, widely propagated in British literature, is due to Dewey and Flett. They claimed that spilites were basic igneous rocks containing albite as the typical felspar and bearing notably higher soda contents than normal basalts. Dewey and Flett further believed that the spilites were members of a soda-rich magmatic suite and that the albite of these rocks was commonly secondary after a primary calcic plagioclase. Bulking of analyses of spilitic lavas indicates com- position of normal basalts (tholeiite or olivine-basalt) plus water. The high soda contents of spilites quoted in the literature are illusory, being based on imperfect sampling. As a rule, only the ‘ fresh-looking’ cores have been analysed. The mineral adjustments observed in spilites may result from deuteric or late-magmatic activity, from deep diagenesis, or from low-grade metamorphism, There is probably no unique origin for these rocks which are most reasonably to be regarded as basalts which have undergone redistribution of components at low/moderate temperatures in the presence of excess H.,O (and sometimes COQ,).”’ Dr. W. R. Browne: Dr. Browne disclaimed any special knowledge of spilites, but pointed out that over the years he had come in contact with volcanic rocks of many geological ages, basic and acid, sub- marine and terrestrial, which showed chemical, mineralogical and other characteristics of the so-called spilitic suite. These, however, in their unaltered condition belonged to calcic, latitic and alkaline types, and thus considerable doubt was cast on the existence of a distinctive spilitic suite. MAY 17th: Address by Miss H. R. Drummond, ““ Observations in Iceland ’’. Miss Drummond summarised the stratigraphy and lithology of Iceland. The entire island is composed only of Tertiary and Recent rocks which consist of two main types—(a) volcanics, mainly basalts and pyroclastics, but with rhyolites occurring in places ; and (6) glacial and fluvioglacial, including tillites, breccias, conglomerates and outwash gravels. The volcanics are of two ages—pre-Pleistocene and Pleisto- cene-Recent. Active volcanoes occur, as well as many centres of geyser and fumarole activity. A feature of the tectonic geology of the island is the presence in Hon. SECRETARY : D.S) Bripers: many areas of pronounced and repeated faulting of the block-and-graben type, and this has had a most definite effect in the production of the present-day topography and in the locations of the present thermal areas. Some reference was made to the permanent ice-sheets which (perhaps surprisingly) cover only a_ small percentage of the area of the island. By means of some excellent colour slides, Miss Drummond exhibited and explained many aspects of Icelandic architecture, scenery and social life. JULY 19th : The meeting passed a motion expressing regret at the death of Professor L. A. Cotton, Emeritus Professor of Geology, University of Sydney. Note and Exhibit: Mr. H. G. Golding noted the occurrence at several locations within the Tumut-Coolac ultra-mafic belt of serpentinites containing disseminated native nickel-iron. Sawn specimens showing numerous megascopically visible particles of the metal were exhibited. Address by Dr. D. F. Branagan: Geology before Clarke.”’ Abstract: ‘“‘ Australian geology had its beginnings in the observations of early explorers and in the search for natural materials. Three separate groups contributed to our early knowledge: (a) the British, (6) the French, (c) the Europeans and Americans. Among the English two groups can be recognised: (a) the practical workers (explorers and miners), and (b) the academic workers. Labillardiere, Flinders, Sturt, P. King, Mitchell, Robt. Brown, Fitton, Von Buch, Busby, Platt, Humphreys, Wilton, Lhotsky and Menge were among those who contributed. Our information about these workers is still fragmentary. The geological knowledge obtained was also fragmentary and uncoordinated until Clarke’s work began to follow the stratigraphic principles introduced in Europe by Smith and others.’’ ‘* Australian SEPTEMBER 20th: sim the absence (overseas) of the Chairman (Mrs. Sherrard), Dr. T. G. Vallance was elected Acting Chairman. Abstract: Dr. L. E. Koch ‘presented sam vabstracr from a lecture entitled “ Geology~and ‘Integrated Science ’’. Dr. Koch referred to the method of “‘ concept structures ’’ and recommended its use. in order to facilitate a systematic approach to the complex problems connected with the integration of High School Certificate Science as prescribed by the new syllabus for New South Wales schools. Notes and Exhibits: Dr. T. G. Vallance reported the probable occurrence of a small volcanic neck of the Hornsby type situated under Bowen Ave., West Turramurra. The occurrence is apparently in situ, and specimens from the area were submitted for examination. Dr. Ida Browne mentioned the possibility of a similar neck being located at Muogomarra, between Cowan and the Hawkesbury River. Address by Dr. R. Curtis : ‘‘ The Geology of Graham- land, West Antarctica.’’ SECTION OF GEOLOGY 243 Abstract: Dr. Curtis described the petrography of the Graham coast and offshore islands. A small succession of siltstones, shales and felspathic grey- wackes have been correlated with the late Palaeozoic Trinity Peninsula Series and have suffered pre-Jurassic low grade metamorphism. Upper Jurassic volcanics have a minimum thickness of 5000 feet, comprised of approximately 1000 feet of andesite lavas overlain by 4000 feet of pyroclastics. The initial phase of gabbro intrusion of the Andean Intrusive Suite was followed by successive intrusions of granodiorite magma. The early intrusions of granodiorite magma incorporated large quantities of gabbroic material at depth, which resulted in their basification to a hybrid magma of dioritic composition. Basification had been completed before the magma attained its present level. Successive intrusions were progressively less modified, and the trend of intrusion diorite-tonalite-granodiorite is one of decreasing contamination. The granites and granophyres are thought to represent crystallisation-differentiation products of the granodiorite magma. The present configuration of Grahamland is possibly due to large- scale faults trending parallel to the present axis, and which developed in Pliocene times. NOVEMBER 15th: (Acting Chairman: Mr. H. G. Golding.) The meeting passed a motion expressing regret at the death of Professor Griffith Taylor, Emeritus Professor of Geography, Universities of Sydney, Chicago and Toronto. Note and Exhibit: Mr. H. G. Golding referred to occurrences in the northern end of the Gundagai-Coolac serpentine belt of variations in rock-type shown by zonation within the mass, and also to the occurrence of chromite located one mile north of the Murrumbidgee River near Coolac. Specimens relevant to _ these occurrences were exhibited. Address by Dr. L. E. Koch: ‘‘ Touchstone (Lydite), its use through the history of precious metals, and its occurrence in Australia.’’ Abstract: ‘‘ The use of the touchstone (Lydian- stone=black chert) for the determination by the ‘streak test’ of the fine content of gold alloys is one of the oldest technological and micro-analytical discoveries of ancient man (700 B.c. or earlier). The colour and reflectivity of the streak of a given gold alloy of unknown composition are visually compared with streaks made by means of ‘needles’ prepared from alloys of known gold-silver or gold-copper content. After treatment with strong nitric acid for the removal of gold and copper, the new ‘spongy’ streaks are again compared for similarity or dissimilarity. Pebbles of black siliceous chert are easily obtained from gravels (1” to 2”) of rivers in New South Wales flowing through the outcrop belt of Palaeozoic rocks (Upper Silurian, Devonian), e.g. Jenolan Creek, Belubula, Wollondilly, Nepean, etc. rivers.” DS.) BRIDGES, Hon. Secretary, Section of Geology. AUSTRALASIAN MEDICAL PUBLISHING CO, LTD. SEAMER AND ARUNDEL STS., GLEBE, SYDNEY INDEX Astronomy : Minor planets observed at Sydney Observatory during 1962. (Robertson) ———_—_—_—— observed at Sydney Observatory during 1963. (Robertson) , precise observations of, at ‘Sydney Observatory during 1961 and 1962. (Robertson) Occultations observed at Sydney Observatory during 1962-63. (Sims) Positional astronomy. Donovan astronomical lecture for 1963. (Wood) 33 177 }) 183 135 Authors of Papers: Albani, A. D. Some applications of aerial photo- graphs to the solution of topographic and cartographic problems .. Crook, K. A. W. Depositional environments and provenance of Devonian and Carboniferous sediments in the Tamworth Trough, N.S.W... Dulhunty, J. A. Our Permian heritage in Central Eastern N.S.W. (Clarke Memorial Lecture). . Griffith, J. L. On the Gibbs’ Phenomenon in n-dimensional Fourier transforms Lovering, J. F. The eclogite-bearing basic i igneous pipe at Ruby Hill near Bingara, N.S.W. Mackay, R. M. Lepidophioios and Cyrtospirifer from the Lambie Group at Mount Lambie, N.S.W. : = ae ee Minty, E. J. Petrology ‘in relation to road materials. Part II: The selection of rock for road-making in Australia, with special reference to New South Wales *. 55 Mozley, A. James Dwight Dana in New South 7 41 145 163 Wales, 1839-1840 185 Pels; 5S. Quaternary sedimentation by prior streams on the riverine plain south-west of Griffith, N.S.W. 107 Quodling, F. M. On traces of native iron at Port Macquarie, N.S.W. 8] Rade, J. Geology and sub- surface waters of the Jurassic Walloon Coal Measures in the eastern portion of the Coonamble Basin, N.S.W. Lower Cretaceous sporomorphs from the northern part of the Clarence Basin, N.S. W. : Koberts, J. A lower Carboniferous fauna from Lewinsbrook, INES. Wie Gs ee Li Lower Carboniferous faunas from Wiragulla and Dungog, N.S.W. ; 193 Robertson, W. H. Minor planets observed at Sydney Observatory during 1962 33 ——_-———_. Precise observations of minor planets at Sydney Observatory during 1961 and 1962 : 99 Minor ‘planets: observed at Sydney Observatory during 1963... 177 Sims, K. P. Occultations observed at Sydney Observatory during 1962-63 183 Strusz, D. L. Devonian trilobites from the Wellington-Molong district of N.S.W. ee Ow Voisey, A. H., and Williams, K. L. The geology of the Carroll- Keepit-Rangari area of N.S.W. 65 Wood, H. W. Positional ie ian (Donovan astronomical lecture) ne 135 Geology, Mineralogy, Palaeontology : TITLES Australian geology before Clarke (abstract) .. Dana, James Dwight, in N.S.W., 1839-1840 (Mozley) Depositional environments: ‘and ‘provenance of Devonian and Carboniferous sediments in the Tamworth Trough, N.S.W. (Crook) . : Devonian trilobites from the Wellington-Molong district of N.S.W. . (Strusz) Eclogite-bearing basic igneous pipe at Ruby Hill near Bingara, N.S. W. (Lovering) : Geology and sub-surface waters of the Jurassic Walloon Coal Measures in the eastern portion of the Coonamble Basin, N.S.W. (Rade) .. Geology of Grahamland, West Antarctica (abstract) : Geology of the Carroll-Keepit-Rangari area of N.S.W. (Voisey and Williams) : Lepidophloios and Cyrtospirifer from the Lambie Group at Mount Lambie, N.S.W. (Mackay).. Lower Carboniferous fauna from Lewinsbrook, N.S.W. (Roberts) Sc os ae Lower Carboniferous faunas from Wiragulla and Dungog, N.S.W. (Roberts) Lower Cretaceous sporomorphs from the northern part of the Clarence Basin, N.S.W. (Rade).. Permian heritage in Central Eastern N.S.W., our. (Dulhunty) : es ra Petrology in relation to road ‘materials. Part il The selection of rock for road making in Australia, with special reference to N.S.W. (Minty) Quaternary sedimentation li prior streams on the riverine plain south-west of of Griffith, INES SVVic (Pels) : Traces of native iron at Port Macquarie, N, Ss) W., on. (Quodling) ; LOCALITIES IN N.S.W. Benerembah irrigation district: quaternary sedimentation .. ae a = i Bingara: Ruby Hill igneous pipe, eclogite- bearing ae - a5 Carroll: geology lower Cretaceous sporomorphs .. notes and exhibits Clarence basin : Coolac serpentine belt : Coonamble basin: Walloon C.M. sub-surface waters Dungog: lower Carboniferous aun Griffith : Quaternary sedimentation 5.W. of Honeysuckle range: exhibit of chromitite Keepit : geology = ar Lewinsbrook : lower Carboniferous fauna. Rangari: geology ; i Ruby Hill: eclogite- beating pipe a su Tamworth Trough: depositional environments - Turramurra: Bowen Avenue volcanic neck Wiragulla: lower Carboniferous fauna geology and 133 (twice), 242, 2 246 FOSSIL GENERA AND SPECIES Acuminothyris triangularis .. Athyris wivagullensis. . Aviculopecten sp. : Balanoconcha elliptica Bibucia tubiformis Brachythyris elliptica Calymene sp. nov. Pees ‘““ Camerotoechia’’ sp. Cheirurus (Crotalocephalus) packhami Chonetes cangonensis Cladochonus sp. ; tenuicollis Cleiothyridina segmentata squamosa Conophillipsia brevicaudata . . Cyrtospirifer gneudnaensis 3 ineymis oleanensis ? Delthyris papilionis Echinoconchus gvadatus Fenestella browne Fe: gvesfordensis Ee wilsont Fistulamina inornata f. Gigantoproductus tenuirvugosus Goniocladia laxa Fs Gravicalymene australis Inflata elegans Kitakamithyris sp. Leonaspis sp. Lepidophlotos sp. Otarion munroer Productina globosa Ptilopova koninckt Pustula multispinata. . Scutellum sp. .. Spivifer osborner INDEX Streblochondria obsoleta Streblopteria sp. : Streptorhynchus spinigera ? Thomasaria voiseyi History of Science: James Dwight Dana in New South Wales, 1839-1840. (Mozley) Mathematics : On the Gibbs’ phenomenon in n-dimensional . 163 Fourier transforms. (Griffith) Proceedings of the Society: Annual report, year 1962-63 year 1963-64 Awards, 1963 1964 “hs Financial statement, 1963 .. 1964 .. Members of the Society, April 1964 : New England branch, annual ene 1963-64 Obituary, 1962-63 1963-64 : j Proceedings, abstract of, for 1962 for 1963 Section of Geology, proceedings, 1962 proceedings, 1963 Surveying : Some applications of aerial photographs to- the solution of topographic and Cane ee my ; a problems. (Albani) an et 0 aD a AZO Bee | wo Lae rr : oe eae Medals, Memorial Lectureships and Prizes, TSE) s. ae} . 241 .. 126 ips» era ge oe .. 228 .. 133 . 242 239 ae 1a sheen vf Pad a Ad Vt orary Secretaries P ty ney 7 € ba asurer | te ind’ was i yy PAY 4 A A Ma JOURNAL AND PROCEEDINGS OF THE ROYAL SOCIETY OF NEW SOUTH WALES VOLUME 98 1964-65 PUBLISHED BY THE SOCIETY. SCIENCE HOUSE, GLOUCESTER AND ESSEX STREETS SYDNEY Ji CONTENTS Part 1 Presidential Address ; Volatile Oils and Plant Taxonomy. H. H. G. McKern Chemistry; Liversidge Research Lecture : Heterocyclic Chemistry, and Some Biological Overtones. Adrien Albert Geology ; Late Quaternary Coastal gs aac of the Port avi el Lakes Area, N.S.W. Bruce G. Thom .. ; The Stratigraphy of the Hervey Group in Central New South Wales. J. R. Conolly .. A Note on the Stratigraphy of the Devonian Garra Beds of New South Wales. D. L. Strusz Part 2 History of Geology ; The Foundations of the Geological Survey of New South Wales. Ann Mozley . Geology ; Radioactive Laterites in the National Park Area. J. A. Mumme .. The Mesozoic Age of the Garrawilla Lavas in the Coonabarabran-Gunnedah District. J. A. Dulhunty .. Clay Mineralogy of Some eae Devonian Sediments from Central New South Wales. John R. Conolly.. = me e iv = a = Astronomy ; Photographic Observations of Double Stars. WK. P. Sims Minor Planets Observed at Sydney Observatory during 1964. W. H. Robertson 11 37 85 Q] 104 105 1V CONTENTS - Part 3s Presidential Addresses ; Some Units and Standards of Weights and Measures. J. W. Humphries.. The Mathematical Sciences in the Changing World. W. B. Smith-White .. Mathematics ; Average Forces in Lossy Electromagnetic Systems. W. E. Smith .. Geology ; The Marine Permian Formations of the Cracow District, Queensland. Robin Wass The Geology of the Canowindra East Area, New South Wales. W. R. Ryall The Annual Report, 1965 Part 4 The Pollock Memorial Lecture ; Current Trends in Solid State Science Frederick Seitz Palaeobotany ; On Lepidopteris madagascariensis Carpentier (Pelaspermaceae). John A. Townrow Physical Geography ; The Big Hole near Braidwood, New South Wales. J. N. Jennings Geology ; Petrography of Some Permian Sediments from the Lower Hunter ee of New South Wales. J. D. Hamilton The Geology of Mandurama-Panuara. R. E. Smith .. Astronomy ; Precise Observations of Minor Planets at es Sy mira 1963 and 1964. W. H. Robertson 139 145 151 159 169 181 203 215 221 239 263 ol hoe nes ses ster as ee idge ‘Research Lecture : ct lie Chemistry, and Some Biological Overtones. “Adrien Albert it , a j an ee: * ‘i } s L ,, - "4 i NM a4 Ra uae : » | } 4 / 5 ‘i ‘ * et ~ % so AN ce h t ; 4 } S 2 + 1 ere = 3 4 5 “ ie Ww? > } > > - . AAI ee < aternary Coastal Morphology of the Port Stephens-Myall Lakes Area, Bruce G, Thom - cE A 7 a a f eat . - Ra oo 6 Stratigr < fi ee af ie 7 ~ & +s f ~ “ * ‘ i RR 2 f ‘ ¥ i ¥ A ( hed ~ > J 3 ‘ 2 Q J, 1 4 ~ } x Ty j / ; f oo ¥ ; é , GLOUCESTER, AND ESSER s STREETS, ‘SYDNEY raphy of A teceee of e a Wales. _ PUBLISHED BY THN soctery, MN —— NOTICE TO | AUTHORS ne a us ad a General. ah ere should ‘be addressed to the Honorary Secretaries, Royal Society ‘of New. South Wales, 157 Gloucester Street, Sydney. Two copies of each manuscript are - required: the original typescript and a carbon Copy ; of the abstract typed on separate sheets. 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When several otacarpie zh are to be combined in one Plate, the photographs , should be mounted on a sheet of white bristol — I Geological - Papers, | dene ‘in “special citcumstances, authors submitting manuscripts ‘ in which new stratigraphical nomenclature is” ; proposed must also submit the letter of approval: ‘of or comment on the new names from ‘the © My appropriate -noménclature sub-committee of 2 ‘Authors who are members of the’ , Society’ receive 50: copies of each. paper free. Additional copies may be purchased. pee id they are ordered by the author whee neers: 6 gi alan: OE TAS IG AOC ee cen x ae NY Ase 1% es Hy 5 al ‘ Dy tie wee he a4 ‘ fe) fe N ist, Os Rape i Mail) EN ay ey aa PANG Deane aout eG aS Dae i I _ journal and Proceedings, Royal Society of New South Wales, Vol. 98, pp. 1-10, 1965 Volatile Oils and Plant Taxonomy* H. H. G. McKERN Museum of Applied Arts and Sciences, Sydney AgsstRact—Attempts to utilize the chemical compositions of volatile otls in taxonomy are reviewed. Attention is drawn to the weaknesses in earlier work and some guiding principles to be observed in future work in this field are suggested. Although many promising leads have so far appeared, it is considered that both chemical and botanical data are still too insufficient to enable any conclusions to be drawn. I The mid-twentieth century scene in organic chemistry shows a strong interest in what Czapek has conveniently referred to as “secondary plant substances’’, as distinct from such “primary” plant substances as cellulose and proteins. These secondary plant products—alkaloids, glycosides, flavones, gums, resins, waxes and so on—have provided many interesting problems in the elucidation of molecular structure and stereochemistry, and have brought to light many novel and useful substances. As a natural extension to these studies, there has followed enquiry into bio- synthetic mechanisms operative within plants, into speculation on the function of these substances in the plant economy, and finally, as to whether they have taxonomic significance, and it is this last-mentioned enquiry which will concern us here. Although chemotaxonomy has been the subject of two recent monographs (Alston and Turner, 1963; Swain, 1963), neither of these works contains a chapter devoted to essential oils considered as a phyto- chemical category, and the present paper is therefore supplementary to these volumes, both in dealing with this aspect of the topic, as well as in calling attention to more recent data and thought not available in the works just cited. This omission will doubtless be rectified in the work of Hegnauer (1962-) now appearing. The examination of the possible value of chemistry to plant taxonomy now dates back some considerable time: indeed, early in the 19th century it was observed that certain families displayed a high frequency of occurrence of certain chemical classes— alkaloids in Solanaceae, oleo-resins in Pinaceae, and so on. This paper deals specifically with volatile or * Presidential Address delivered before the Royal Society of New South Wales, 1 April, 1964. A “q essential oils, and here again, in this special case of a phytochemical product, it was early observed that the occurrence of volatile oils was not completely random, but characterized certain families such as Labiateae, Rutaceae, and Myrtaceae. Taking these general observa- tions a step further, chemists noted that, as a result of consideration of the various compounds present in volatile oils, there existed the possibility of a relation between oil composition and the systematic position assigned to the plant. One or two examples will suffice to illustrate this kind of indication. Baker and Smith (1910) observed in the oil steam-distilled from the foliage of Phyllo- cladus rhomboidalis Rich. (Podocarpaceae) the presence of a crystalline diterpene, C,jHgp, named by them phyllocladene (I). Subsequent workers, particularly in New Zealand, reported the presence of phyllocladene or its isomer isophyllocladene (II) in three other species of Phyllocladus ; and further, that these diterpenes are of frequent occurrence in the leaf oils of Podocarpus and Dacrydium (also Podocarpaceae), and they have been identified in such related genera as Avaucaria (Araucariaceae), Cupressus and Lzibocedrus (Cupressaceae), Sciadopitys (Sciadopityaceae), and Cryptomeria (Taxo- diaceae) (cf. Aplin, Cambie and Rutledge, 1963). Both phyllocladene and ssophyllocladene are unknown in the angiosperms. Again, consider the case of ascaridole (III). This is a most unusual and distinctive compound, being a monoterpene peroxide. It is an explosive liquid and is altogether a substance not to be expected in nature; nevertheless it is found in large percentages in the volatile oil of not only Chenopodium ambrosioides var. anthelminticum but is present also in the oils of other Cheno- podium species such as C. hircinum. Following such leads as these, investigators have studied volatile oil compositions from this viewpoint, and some have presented their 2 H. H. G. McKEKN ideas on the part which chemistry might play in plant classification, and even how it might be applied in phylogeny. Several of these attempts will be briefly examined. One of the early corpora of work in this field is that of Baker and Smith, who presented their views in two monographs, one on Eucalyptus (1920), the other on Australian gymnosperms (1910). Setting aside for reasons of space the work on the gymnosperms, their views on Eucalyptus may be summarized as follows: (1) Within the limits of variation typical of living organisms, they regarded the oil composition of a species as constant. (2) They regarded oil composition within the genus as susceptible of classification into major chemical groups. Their first group, for example, comprised those oils characterized by the presence of much a-pinene, the absence of a-phellandrene, with 1,8-cineole present in not’ more than a few per cent. “(3)) They, assumed Angophora to be the older genus, and having adduced evidence that Angophora oils resembled closely the “pinene group’”’ of Eucalyptus oils, they perceived in this a chemical link between Angophora and the more primitive eucalypts such as the “ bloodwoods ” (Series Corymbosae and Corymbosae-peltatae of Blakely, 1955), all species of which examined by them having been found to yield “ pinene oils’’. (4) They claimed a relationship between oil compositions and leaf-venation ; maintaining that pinene oils came from species whose leaves showed transverse parallel venation, the intra- marginal vein close to the margin; whilst as phellandrene contents rose, the angles made by the veins with the mid-rib diminished and the intramarginal vein tended to become removed from the margin. With these observa- tions as a starting-point, they postulated an evolutionary pathway in Eucalyptus, showing descent from Angophora, and how Eucalyptus species may have evolved from the more primitive species such as E. calophylla. A second large body of work published in this field is that of Fujita (1951 and subsequent papers), whose monograph sets forth his views on plant classification based on essential oil compositions. Unlke Baker and Smith, who personally accumulated both field and laboratory data on a few genera only, Fujita has theorized not only his own data (e.g. on Ovthodon), but accepting uncritically published chemical and II Hil taxonomic data (much of it now known to be incomplete or erroneous), has erected on this basis chemical classifications and phylogenies — of a large number of genera. A third work of some magnitude is that of | Mirov in Pinus (1961). His monograph merits attention for four reasons. Firstly, although — much of the work was carried out prior to the advent of gas chromatography, the chemical work is modern and reliable as far as it goes. | Secondly, Mirov was at pains to collect | botanically authentic material, and was aware of the biological considerations (e.g. hybridism) — affecting phytochemical work. Thirdly, he has | reported on the compositions of the volatile oils from the oleo-resins of an entire genus. Fourthly, unlike some of the earlier authors, he has preferred to review his data rather than to use them as a basis for elaborate theories. Such, then, are some examples of the collection of phytochemical data on volatile oils having VOLATILE OILS AND PLANT TAXONOMY 3 _as its objective the determination of relationship to taxonomy. Much of the earlier work, however, suffers from certain shortcomings, and that of Baker and Smith in Eucalyptus will serve to illustrate some of the errors which must be avoided in researches in this field. Firstly, chemical data have sometimes been obtained from material from plants of imper- fectly-understood or ill-defined systematic position. The genetic complexity of many populations is now familiar: in such cases species limits become blurred, and the chemical data drawn from such populations may become difficult to interpret. Thus, Baker and Smith reported on the oils of many eucalypts now known to be of hybrid origin; for example, E. vitrea R.T.Bak. (=E. pauciflora Sieber x E. dives Schau. or XE. radiata Sieber ex DC.), E. irbyi R.T.Bak. et H.G.Sm. (= E. dalrympleana Maidenx FE. gunnit Hook f.), LE. wunialata R.[.Bak. et H.G.Sm. (=E£. globulus Labill. x £. viminalis Labill.) and many others. They further overlooked the complexity in some Eucalyptus groups such as Series Psathyroxyla of Blakely (loc. cit.), the “scribbly gums ”, and reference to their herbarium specimens shows that under the name FE. haemastoma Sm. they included the variety sclerophylla Blakely and E. racemosa Cav. (syn. E. micrantha DC.). Penfold and Morrison (1927b, 1933a) demon- strated great chemical differences not only between E. haemastoma and EL. racemosa but also within E. racemosa. Other examples of groups providing genetic difficulty are the E. mannifera Mudie group (Johnson, 1962), treated by Baker and Smith in part under E. maculosa R.T.Bak., FE. lactea R.T.Bak., and E. gullicki R.T.Bak., and the FE. andrewsi Maiden-E. campanulata R.T.Bak. complex (treated as two distinct species by Baker and Smith). Secondly, some earlier theories have been based on deficient chemical data: in very many cases Baker and Smith had identified compounds comprising less than 50 per cent. of the oil (e.g. E. dawsont R.T.Bak., E. nova- anglica Deane et Maiden, FE. fibrosa F. Muell. (in loc. cit. “E. siderophloia Benth.) and E. eximia Schau. In the case of only a very few species did these authors have a knowledge of oil compositions accounting for the greater portion of the oil. Thirdly, if chemical variation within a “good ”’ species occurs, it will present problems in the accommodation of chemical data to a scheme relating them to the systematic position of a plant. This phenomenon will be referred to later, but at this juncture it may be recalled that Baker and Smith encountered variations in oil composition within a species, and that it caused them great difficulties in their schemes of classification and phylogeny. Their treatment of the phenomenon was inconsistent: in E. viminalis they simply admitted the difference, and designated the variant “variety A”; in E. camaldulensts Dehnh. (E. rostrata in loc. cit.) they formally erected the varietal taxon of borealis to differentiate those trees yielding an oil rich in cineole, but morphologically insepar- able from those of populations _ earlier encountered, but which yielded a markedly different type of oil. In FE. radiata Sieber ex DC. (im loc. cit. E. australiana R.T.Bak. et H.G.Sm., FE. phellandra R.T.Bak. et H.G.Sm., and FE. amygdalina var. nitida Benth.) separate taxa of specific rank were erected solely on chemical grounds. Finally, in E. dives Schau. the observation by these authors of a profound chemical variation (F. dives var “‘ C’”’ of Penfold and Morrison, 1927a) was so at variance with their scheme that they rejected these trees as belonging to £. dives and referred to them as “ E. australiana var. latifolia”. Finally, attempts to classify plants by chemical groups (as did Baker and Smith in Eucalyptus) may be misleading unless an adequate knowledge of oil compositions is available. These workers were compelled to establish a category for species “‘ yielding an oil not readily placed in the other groups ”’ Their theory of correlation of leaf venation with chemical composition of the oils suffered from the existence of this category : E. citriodora Hook., for example, with its venation (and all other characters) typical of Series Corymbosae- peltatae of Blakely, failed to yield an oil rich in #-pinene, but was found to contain citronellal as major component. Research continues to demonstrate the existence of species whose leaf oils are of unexpected chemical composition. Sutherland, Webb and Wells (1960), for example, showed the leaf oil of E. deglupta Blume from New Guinea to consist largely (c. 50 per cent.) of nerolidol, together with ocimene, «-pinene, a-phellandrene, /-cymene, carvatonacetone and vsovaleraldehyde ; and Hellyer, Keyzer and McKern (1964) have found that the leaf oil of E. crenulata Blakely et de Beuzeville consists largely of methyl 3,4,5-trimethoxybenzoate (c. 47 per cent.) and y-terpinene, accompanied by lesser amounts of #f-cymene, «-pinene, terpinolene, isovaleraldehyde, and_ terpen-1- en-4-ol. 4 H. H. G. MCKERN The lesson to be learned from this review of earlier work is not only that data must be interpreted more critically, but that the phyto- chemist must also collect his data more critically against a background of awareness of the biological factors involved. Willis, McKern and Hellyer (1963), for example, suggest the following experimental procedure: (1) Collect chemical data (at least initially) only within well-defined species. (2) Working always on the same organ, compare oils of individual plants within the one population, or from the same site. (3) Compare data from population to population, or from site to site. (4) Test the inheritance of both chemical and morphological characters. This procedure may then with advantage be applied to plants or populations of plants where taxonomic limits are less clear (e.g. between Pinus halepensis and P. brutia, cf. Muirov, loc. cit., pp. 111, 130-131). II The threads of chemical affinity already referred to, and which appear to link taxa already accepted from morphological considera- tions as related, undoubtedly exist and have received much attention. Not so much prominence, however, appears to have been given to the equally frequent lack of obvious chemical connection between closely-related taxa. The genus Backhousta (fam. Myrtaceae) provides an example. It is a small genus from which only nine species have been described. The genus itself is well separated from other cognate genera within the family, and further, species limits within the genus are sharply defined, so that no taxonomic difficulties are present. Of the nine species known, seven have been examined for their leaf oils ; reference to Table I demonstrates the lack amongst these species of an obvious chemical linkage of the sort being discussed. The use of the “ unusual”’ or infrequently- encountered essential oil constituent as a means of tracing affinities amongst plants has already been referred to. Some guidance as to the reliability of this procedure is provided by the work of Bowyer and Jefferies (1959, 1962) on the incidence of torquatone in Eucalyptus. This substance was first discovered by these workers in the leaf oils of EL. torquata J.G. Luehm. and of E. caesia Benth., and was shown by them to have the structure IV shown above. Of a further 40 species examined, another two showed the presence of torquatone: E. flocktoniae Maiden and E. spathulata Hook. var. gvandifiora Benth. Significant points emerging from this study are: (i) As the authors themselves remark, “the four species found to contain torquatone are considered to have TABLE I Leaf Oils of Backhousia Species Species Chief Constituents of Oil References B. angustifolia EF. Muell. (a)*Dehydroangustione ; angustifolionol. (b) Dehydroangustione. (c) Angustione ; angustifolonol. Cannon and Corbett (1962) B. anisata Vickery Anethole McKern (1949) B. bancrofitti F.M. Bail. et FE. Muell. Chiefly sesquiterpenes and sesquiterpene alcohols ; «-pinene ; esters. Lahey and Jones (1938) B. citriodova F. Muell. (a) Citral, 90-95 per cent. (6) Citronellal, 62-5-79-7 isopulegol ; citronellol ; PELpP Cent. ; esters. Penfold et al. (1951) B. hughes C... White g- and (-pinene; sesquiterpenes and sesquiterpene alcohols. Jones and Lahey (1937) B. myrtifolia Hook. f. et Harvey. Elemicin. Isoelemicin. Eugenol methyl ether. Isoeugenol methyl ether and _iso- elemicin. IPS SSUASI SS Penfold (1922) ; Penfold, McKern and Spies .(1953); > Hellyem McKern and Willis (1955). B. sciadophora F. Muell. «-pinene, 80-85 per cent. ; sesquiterpenes and sesquiterpene alcohols. Penfold (1924). * The alternative entries (a), (b), (c) or (d) in the centre column refer to differences in oil composition occasioned by the existence of chemical races or forms within the species. -- a ‘ i VOLATILE OILS AND PLANT TAXONOMY 5 very little botanical affinity’; L. caesia (series Obliquae), E. spathulata (series Cornutae) and £. torquata (series Dumosae) are widely enough separated within section Macrantherae, but FE. flocktoniae (series Subulatae of section Platyantherae) is, at least on Blakely’s classi- fication, of little affinity with the other three. (ii) The species found by Bowyer and Jefferies not to contain torquatone comprise six from series Dumosae, closely related to E. torquata, and another six from series Cornutae and having close botanical affinity with EL. spathulata. OCH; HOC S COCH; CH(CHs)> CH30 OCH; GHs IV E. griffithsia Maiden is classified as related to E. caesia, also in series Obliquae. (iii) Further, gas chromatographic examination of the oil of typical E. flocktoniae showed no indication of the presence of torquatone ; this substance was detected only in a form having ribbed fruits from the Lake King district of Western Australia. With E. spathulata var. grandiflora, only one sample (from the large-fruited form from Lake King) yielded an oil containing torquatone. Another aromatic substance, baeckeol (V), provides a further example of the inconclusive results of following the incidence of the ‘unusual’? compound: discovered first in the leaf oils of Baeckea imbricata (Gaertn.) Druce (B. crenulata R.Br. in loc. cit.) and of Darwima procera B. Briggs (D. grandiflora in loc. cit.) by Penfold (19226, 1923), the same author (1925) demonstrated its presence in B. gunmana Schau. var. latifolia F. Muell. (but not observed in B. gunniana by Smith (1922)), whilst Spoelstra (1931) later found it in the extra-Australian B. frutescens L. ; and quite recently Bowyer and Jefferies (1962) have shown it to be a component of the Western Australian Calytrix angulata Lindl. Baeckeol is thus seen, from an evolutionary point of view, to be diffused through at least three* * And four, if (as seems likely) the yellow crystalline substance of m.p. 104° found by Jones and White (1931) in the leaf oil of Leptospermum luehmannii F.M. Bail. (in loc. cit. Agonis luehmanni (F.M. Bail.) White et Francis) is baeckeol. genera of the Myrtaceae extending from south- east Asia to both the eastern and western extremes of the Australian mainland. Investi- gations on the oils of other Baeckea, Darwinia and Calytrix species have not disclosed the presence of baeckeol (Baker and Smith, 1899 ; Penfold, 1927; Jones and White, 1930; Penfold and Morrison, 1933) ; Penfold, Ramage and Simonsen, 1934; Bick and Jones, 1940 ; Jones, Lahey and Sutherland, 1949). In fact, the unusual compound is likely to be found in plants widely separated in botanical OCH; _CHs3 COCH CHs CH30 OH CH; Vy classification. Consider the aromatic ester methyl salicylate: it is not commonly met in large percentages in essential oils, but neverthe- less forms the major part of the oil of the angiosperm Gaultheria procumbens L. (Ericaceae) and of the botanically remote Asplenium lampro- phvllum Carse (Aspleniaceae), a pteridophyte (Briggs and Taylor, 1947). Furthermore, these authors record that they failed to detect this CHO CHO VI ester in A. bulbiferum Forst. f. (almost indis- tinguishable from A. lamprophyllum), in A. lucidum Forst. f., in A. flaccidum Forst. f., or in A. falcatum Lam. Again, it would appear that sesquiterpene dialdehydes are uncommon plant constituents ; nevertheless, the first two reports on a substance of this class, polygodial (VI), are from two widely separated families. Barnes and Loder (1962) first discovered polygodial in the leaves of Polygonum hydropiper L. (Polygonoceae) 6 H. H. G. MCKERN and in the same year Loder (1962) found it in the quite unrelated Drimys lanceolata (Poir.) Baill. (Winteraceae). To sum up, whilst it must be admitted that some soft of a frequency pattern of volatile oil compounds has emerged (for example, the extraordinary frequency of occurrence of a-pinene), nevertheless, the selection of an “unusual ’’ or infrequently encountered com- pound as a taxonomic tracer is scientifically unsound ; its unfamiliarity may be due simply to insufficient investigation. The eudesmols were once thought to be confined to Eucalyptus ; they are now known to occur in widely separated genera. Further, not only does it appear that the same compound is lkely to be encountered in the oils of unrelated species, but it seems that oils of very similar, if not identical, composition may be produced by plants from different species, genera, or separated by even higher taxonomic categories. McKern (1956) has suggested that, rather than attempt to link oil compositions with taxonomy, it would perhaps be better to think in terms of the biochemical system operative within the plant, on the assumption that this genetically-determined enzyme system results in the elaboration of a certain set of compounds which collectively constitute the oil. Hence it may be possible to recognize groups of oil compositions to one of which the plant may be linked, rather than to attempt to relate the composition of a single oil, or a selected component, to a taxonomic system. Unfortunately, our knowledge of the ultimate compositions of oils is still very far from complete, but there are strong indications that the compositions of oils from a number of different plants may be similar. In Eucalyptus, for example, it is not possible in our present state of knowledge, to distinguish qualitatively amongst the oils of the “ piperitone form ”’ of E. andreana Naud., of E. dives Schau., of E. radiata Sieber ex DC., of E. piperita Sm. or of E. racemosa Cav. In such work, care must be taken that artefacts (arising perhaps from the method of isolating the oil) are not confounding factors. Ill The simple correlation of volatile oil com- position with the systematic position of a plant is likely to be complicated by the frequently- reported examples of chemical variation within a species. This phenomenon appears to have been observed for most chemical classes of secondary plant products, e.g., in alkaloidal plants (Steinegger, 1957), in glycosidic plants (Van Os, 1957), and in cyanogenetic plants (Dillemann, 1957), and has been the subject of much useful review and comment (cf. Mothes, 1957 ; Hegnauer, 1957; ODillemann, 1959). These authors are concerned with the phenomenon of pronounced chemical differences existing between plants or between populations of plants within a species which is otherwise well defined by the usual morphological criteria, and where no morphological character may be seen to be linked with a chemical character. The term ‘chemical races”? has come into use for reference to these variants, which Hegnauer (1957) defines as follows: “In allgemeinen wird man von chemischen Rassen sprechen, wenn man innerhalb einer Species deutliche chemische Differenzierungen beo- bachten kann, die nicht von erkennbaren (oder erkannten !) morphologischen Differenzierungen begleitet sind.’’ Hegnauer further emphasizes that these taxa are to be regarded as of sub- specific rank. In the field of volatile oil chemistry, this phenomenon was first clearly perceived by Penfold and Morrison (1927a) as a result of their observations on E. dives, and, in the succeeding years their school in Sydney, together with many other workers in other parts of the world, have brought to light a large number of examples. Some of these have been discussed by Stahl (1957) and by Hegnauer (1957), but to emphasize the problem which this phenomenon sets the phytochemical systematist and phylo- genist, the examples selected for inclusion in Table II have been chosen because in each instance the variants were observed growing side by side on the same site. The reader is further referred to Table I where, of the seven Backhousia species listed, three (B. angustifolia, B. citriodora and B. myrtifolia) are seen to exist in different chemical forms. These examples are of like interest, inasmuch as in the case of each species the chemical variants are also to be found occurring naturally side by side under similar environmental conditions. At the time of writing, the evidence for chemical races within species showing not only quantitative chemical differences, but also those of a pronouncedly qualitative nature, is both strong and striking. However, the chemical data on which it rests must be regarded as incomplete, inasmuch as no chemist has yet accounted for every constituent of an oil. Even with the use of gas chromatography, perhaps not more than 99 per cent. of an oil has been accounted for, and in the remaining VOLATILE OILS AND PLANT TAXONOMY “1 TABLE II Chemical Variation Within Some Essential Oil-bearing Species Species Melaleuca bracteata I. Muell. Chemical variety sn ae 1 » 3 Major components of oil Eugenol methyl ether. Isoeugenol methyl Blemicin. ether. Reference Penfold, Morrison, McKern and Willis (1950). Species Melaleuca quinquenervia (Cav.) S. T. Blake Chemical variety < o I 2 3 Major components of oil Nerolidol (ca. 90 per Nerolidol and _linalool a-Pinene, 1,8-cineole, Cent, ) (15-50 per cent.). (—)-limonene, a-terpineol, — viridi- florol. Reference Hellyer and McKern (1955) under M. viridiflorva Gaertn. Species Leptospermum liversidger R. T. Bak. Chemical variety oa “ if 2 Major components of oil Cittican, linalool, Citronellal, isopulegol, o-pinene. o-pinene. Reference Penfold (1922, 1931); McKern (1956) 1 per cent. may be found compounds whose presence may modify our views. Of the great majority of essential oils whose compositions are reported in the literature, few have had more than a dozen or so components recorded. However, the most recent examinations of essential oils by gas chromatography show that an oil may contain well over 100 components, of which most are present in only minute quantities, perhaps as little as 100 parts per million or less. The application of such refined analytical techniques will undoubtedly shed much light on the nature and extent of chemical variation in essential oils, but much remains to be done. In order to disprove the theory of chemical races (differing qualitatively from each other) in essential oil-bearing plants, a great number of compounds will have to be positively identified in perhaps less than 1 per cent. of the variant oil in order to establish its qualitative identity with the norm. An instance of progressive refinement of knowledge of chemical variation within a species is provided by the recent work of Gottlieb, Magalhaes and co-workers (1959, 1960, 1962) on physiological forms in Ocotea prettosa (Nees) Mez (Lauraceae) in Brazil. The wood oil of this species had long been considered to consist principally of safrole, but in 1960 these workers announced the occurrence of a form whose oil contained the unusual constituent, 1-nitro-2-phenylethane, together with much eugenol methyl ether. However, on closer examination of the oils from individual trees they showed (1962) that the oil of the nitrophenylethane form may contain varying amounts of safrole, whilst the safrole form, apparently devoid of nitrophenyl- ethane, may contain eugenol methyl ether. The pattern, however, was further complicated by the detection of camphor in small amounts (1-4 per cent.) in some trees of the safrole form, but not in others. A re-examination of many of these variant oils is therefore clearly called for; but even should this result in the theory of qualitative variation being abandoned,* the fact of discon- tinuous variation in the percentage of a single constituent from, say, 1 per cent. in the oil of one plant to 90 per cent. in the oil of an adjoining plant of the same species, both plants occurring naturally on the same site and free to interbreed, is of great genetic interest and economic significance. This is not completely *In fact, Fliick (1963) asserts that ‘“‘ Reports of qualitative variation characterized by the fact that one or more substances are completely absent in one or more subdivisions of the taxon, and which is, therefore of interest to chemical taxonomy, should always be regarded with suspicion.”’ 3 H. H. G. McCKERN a hypothetical example; it is based on the observations of Hellyer and McKern (1955) on the leaf oils of Melaleuca quinquenervia (Cav.) S.T. Blake (en loc. cit., M. viridifiora Gaertn.) (vide Table II). These authors, working on single trees, observed, inter alia, that trees of this species yielding oils consisting almost entirely of nerolidol (ca. 90 per cent.) were growing side by side on the same site with other trees of the same species whose oils consisted of a complex mixture (1,8-cineole, viridiflorol, a-pinene, limonene, «-terpineol, etc.), in which nerolidol was not detected. MM. quinquenervia is an exceedingly well-defined species in the area studied, in fact very distinct from all other members of the genus in New South Wales and shows no hybrid tendencies with other Melaleuca species. IV Setting aside for the moment the extensive data on chemical races, and assuming a chemical constancy for the species, what appear to be the present prospects of utilizing essential oil compositions in plant systematics? Replies to this question have recently been given by two research groups in this field. The first opinion is that of Aplin, Cambie and Rutledge, who last year (1963) took up again the lead provided by the presence of phyllo- cladene and zsophyllocladene in the Gymnosperm genera already referred to. Using the more delicate technique of gas chromatography not available to earlier workers, these authors described the results of the examination of the leaf oils of 28 species of the Podocarpaceae and of nine other related Gymnosperms. They examined carefully the incidence of the diterpene hydrocarbons phyllocladene, zsophyllocladene, kaurene, zsokaurene, rimuene and cupressene. After tabulating and considering their data, they came to the following conclusion: “ It would appear from the present survey that the diterpene hydrocarbons are of doubtful taxonomic value. From the observation that these compounds were absent in five species distributed over three of the sub-sections of the genus Podocarpus and whose natural habitats aberrquite, distinct, the “presence ol aaiece compounds is not even diagnostic of the family. Moreover, no clear patterns of characteristic constituents emerge for the different genera or sub-sections of the family.”’ The second opinion on the question of the utility of chemistry in taxonomy of essential oil-bearing plants is expressed by Mirov, whose monograph (1961) on the Pinus turpentines was earlier referred to. It will be recalled that his work covers the entire genus as it is at present known, and it is considered that the following quotations from his monograph are a fair summary of the present position; and although uttered specifically in reference to the Pinus turpentines, may equally well apply to other fields of phytochemistry : “Some _ closely-related pines may possess turpentines of different compositions ; on the other hand, it is known that two _ species taxonomically remote have turpentines of almost identical composition. . . “The chemical composition of turpentine is not always correlated with the taxonomic position of a pine. One reason for absence of relationship is incomplete knowledge of chemical composition of pine turpentines. Another reason is that there is still a great deal of disagreement among botanists as to the classi- fication of pines? se ‘“ Evolutionary development may also explain certain absences of relationship. Most likely, morphological and chemical characters have followed different paths of evolution. “In correlating the composition of turpentine with the taxonomic position of a pine, one should remember that the genus Pinus of today is different from the genus of the Tertiary period. The oldest living species is probably not older than Miocene. The chemical relationship of pines that existed during the Jurassic was most likely different from what it is now. During the evolution of the genus, many ancient species became extinct, and many new species appeared. At present we have merely patches of an old biochemical pattern. Some of these patches are difficult to fit into the present structure of the genus; others fit very well and are useful in understanding the relationship of living PINES a. “At present it would be futile to develop a natural classification of pines based on their chemical characters. We can merely claim now that chemistry and taxonomy of pine species often coincide, and that when morphological characters are ambiguous, a knowledge of chemistry of the turpentines may be useful.” From what has been said, the value of the chemistry of essential oils in relation to taxonomy appears limited. However, it is submitted that much more information is needed before assessing the worth of the systematic véle of these substances. Indeed, the successes attending the application of other phytochemical products in this field should stimulate further research: a good VOLATILE OILS AND PLANT TAXONOMY 9 example is the weight of chemical evidence brought forward by Price (1963) and Ritchie (1964) to determine the taxonomic position of Flindersia. Using modern methods, therefore, and having regard for some of the principles enunciated, the systematic examination of complete taxa of generic rank and higher should be under- taken. Some co-ordination between workers in different classes of plant product is required : this paper has been confined to volatile oils ; that is, to compounds having boiling-points from, say, 150° C to 350°C. This is an arbitrary division of secondary plant products, and it is certain that the plant knows nothing of vapour pressures. The study of essential oils alone, therefore, does not present a complete bio- chemical picture. For example, Erdtman (1956), in studying heartwood extractives of Prnus, was able to distinguish not only the genus, but was also able to distinguish chemically the two sub-generic taxa, Haploxylon and Diploxylon. On the other hand, Mirov, working on the turpentines distilled from the oleo-resins, was unable to do this. The overall picture of the secondary chemical constituents of plants is needed, bearing in mind that some chemical compounds of different structure may be biochemically related, and that certain substances may arise through more than one biosynthetic pathway. Acknowledgements The author wishes to express his thanks to Mr. J. L. Willis, Museum of Applied Arts and mciences, Sydney, and-to Mr. H. C. K. Mair, Director of the National Herbarium of New South Wales, and his staff, for valuable criticisms during the preparation of the manuscript. References Aston, R. E., AND TURNER, B. L., 1963. ‘‘ Bio- chemical Systematics.’’ Prentice-Hall: Engle- wood Cliffs, N.J. APLIN, R. T., CAMBIE, R. C., AND RUTLEDGE, P. S., 1963. The taxonomic distribution of some diterpene hydrocarbons. Phytochemistry, 2, 205-214. BAKER, R. T., anp Smity, H. G., 1899. On the Darwinias of Port Jackson and their essential oils. J. Proc. Roy. Soc. N.S.W., 33, 163-176. BakeEr, R. T., AND Situ, H. G., 1910. ‘‘ A Research on the Pines of Australia.’’ Government Printer : Sydney, pp. 419-426. Baker, R. T., aND Situ, H. G., 1920. ‘‘ A Research on the Eucalypts, Especially in Regard to their Essential Oils.’’ Government Printer: Sydney. Barnes, C.S., aNnD LopER, J. W., 1962. The structure of polygodial: a new sesquiterpene dialdehyde from Polygonum hydvopiper L. Austral. J. Chem., 15, 322-327. Bick, I. R. C., anp Jonss, T. G. H., 1940. Essential oils from the Queensland flora. Part XVIII. The essential oil of Baeckea stenophylla F. Muell. Univ. of Queensland Papers, Dept. of Chem., 1, No. 16. BLAKELY, W. F., 1955. “‘ A Key to the Eucalypts ”’, 2nd ed. Forestry and Timber Bureau : Canberra. BowveEr, R. C., AND JEFFERIES, P. R., 1959. Studies in plant chemistry. I. The essential oils of Eucalyptus caesia Benth. and £. torquata Luehm. and the structure of torquatone. Austral. J. Chem., 12, 442-446. BowveEr, R. C., AND JEFFERIES, P. R., 1962. New sources and synthesis of torquatone. Aust. J. Chem., 15, 145-149. Briacs, L. H., AaAnp Taytor, W. I., 1947. The occurrence of methyl salicylate in a fern, Asplenium lamprophyllum. Trans. Roy. Soc. New Zealand, 76 (4), 597. CANNON, J. R., AND CORBETT, Nanette H., 1962. Physiological forms of Backhousia angustifolia F.Muell. Austral. J. Chem., 15, 168-171. DILLEMANN, G., 1957. Les races chimiques chez les espéces cyanogénétiques. Pharm. Weekblad., 92, 853-860. DILLEMANN, G., 1959. Les races chimiques chez les plantes médicinales. Ann. pharm. franc., 17, 214-222. ERDTMAN, H., 1956. Organic chemistry and conifer taxonomy. In “Perspectives in Organic Chemistry ’’, ed. A. Todd. Interscience Publishers Ltd.: London, pp. 453 ef seq. Fujita, Y., 1951. Fundamental studies of essential oils. Ogawa Perfume Times, No. 202, 1-627. FxLtck, H., 1963. Intrinsic and extrinsic factors affecting the production of secondary plant products. In ‘‘Chemical Plant Taxonomy ”’, ed. T. Swain. Academic Press: London, p. 169. GOTTLIEB, O. R., MAGALHAES, M. T., AND Mors, W. B., 1959. Physiological varieties of Ocotea pretiosa. I. Perf. Ess. Owl Record, 50, 26—27. GOTTLIEB, O. R., AND MaGarHass, M. T., 1960. Physiological varieties of Ocotea pretiosa. II. Perf. Ess. Oil Record, 51, 18-21. GOTTLIEB, O. R., FINEBERG, M., AND MAGALHAES, M. T. 1962. Physiological varieties of Ocotea pretiosa. III. On the presence of camphor and methyl- eugenol in Brazilian sassafras oil. Perf. Ess. Oul. Record, 53, 219-221; IV. Further data on nitrophenylethane containing specimens. Jbid., 53, 299-301. HEGNAUER, R., 1957. Die Bedeutung der chemischen Rassen ftir die Arzneipflanzenforschung. Pharm. Weekblad, 92, 860-870. HEGNAUER, Rk., 1962. ‘‘Chemotaxonomie der Pflanzen.’ Birkhauser Verlag: Basel and Stuttgart. HELLYER, R. O., McKern, H. H. G., AND WILLIs, J. L., 1955. The essential oil of Backhousia myrtfolla Hooker et Harvey. Part III. Single- tree studies on physiological forms from Queens- land. jf. Proc. Roy. Soc. N.S.W., 89, 30-36. HELLYER, R. O., AND McKeErn, H. H. G., 1955. Melaleuca viridifiora Gaertn. and its essential oils. J. Proc. Roy. Soc. N.S.W., 89, 188-193. HELLVYER, R. O., KEYZER, H., AnD McKErRN, H. H. G., 1964. The volatile oils of the genus Eucalyptus (family Myrtaceae). III. The leaf oil of E. cvenulata Blakely & de Beuzeville. Austral. J. Chem., 17, 283-285. 10 He HG? Meki ik Jounson, L. A. S., 1962. Studies in the taxonomy of Eucalyptus. Contrib. New South Wales Nat. Herbarium, 3, 105-108. JongEs, T. G.,H., anp Laney, F.N., 1937. Essential oils from the Queensland flora. XIII. Backhousia hughesit. Proc. Roy. Soc. Queensland, 49, 152-153. jones, T. G. H., Lanry, F: N., AND SUTHERLAND, M. D., 1949. Essential oils of the Queensland flora. XXIV. The essential oil of Calythrix tetvagona Lab. from the Glasshouse Mountains. Univ. of Queensland Papers, Dept. of Chemistry, 1, No. 37. JONES@ 1. 9G) T1 AND Waite; MEO T8302 “Essential oils from the Queensland flora. I. Baeckea virgata. Proc. Roy. Soc. Queensland, 42, 49-51. Jones, T. G. H., anpD WuiTE, M., 1931. Essential oils from the Queensland flora. III. Agonis luehmannt. Proc. Roy. Soc. Queensland, 43, 24—27. LaHEY, F. N., AnD Jones, T. G. H., 1938. Essential oils from the Queensland flora. XV. Backhousia bancroftii and Daphnandra yvapandula. Proc. Roy. Soc. Queensland, 50, 41-42. oper J: -W., “1962) Occurrence Voi, they sesqui— terpenes polygodial and guaiol in the leaves of Drimys lanceolata (Poir.) Baill. Austral. J. Chem., 15, 389-390. Mirov, N. T., 1961. ‘“‘ Composition of Gum Turpen- tines ot Pines:(* U.S: Dept: ot Agric. Tech: Bull: No. 1239. U.S. Government Printing Office: Washington. McKern, H. H. G., 1949. N PH4 SUBSTANCE N | O7 \N H Fic. 7 ethyl pyruvate ALBERT, A., 1957. Biochem. J., 65, 124. ALBERT, A., 1959. ‘‘ Heterocyclic Chemistry.”’ London: Athlone Press. ALBERT, A., 1963. ‘“‘ Ionization Constants’’, in the paper and re-applied, was found to correspond to one of the two original spots (see B, and C), and to have opposite optical rotations. This resolution had been effected by the cellulose. The generation of Substance T, from 4,5- diaminopyrimidine and ethyl pyruvate within a restricted pH range as shown in Fig. 7, led to its formulation as the bipteridyl-methane (X X]). This was formed from 7-hydroxy-6-methyl- pteridine (D) acting as a Michael donor, and 6-hydroxy-7-methylpteridine (R) acting as a Michael receptor. The structure was proved by degradation. The underlying assumption, that Michael additions across a C=N bond can be acid catalysed, was verified by combining simple donors (such as acetylacetone) with simple receptors (such as quinazoline) (Albert and Serjeant, 1964). In conclusion, I shall say only that, although we have ranged widely within the limits set by the title of this lecture, there are more kinds of heterocyclic chemistry with biological overtones to explore than have yet been laid hands on. ~Who can say what surprises the near future May bring? References Med. J. Aust., i, 245. J. Chem. Soc., 2690. Nature, 177, 525: 178, 1672. ALBERT, A., 1944. ALBERT, A., 1955. ALBERT, A., 1956. ‘“ Physical Methods in Heterocyclic Chemistry ”’, ed. A. Katritzky. New York: Academic Press. ALBERT, A., and ARMAREGO, W. L. F., 1963. J. Chem. Soc., 4237. ALBERT, A., and ARMAREGO, W. L. F., 1964. Advances in Heterocyclic Chemistry (ed. A. R. Katritzky), 4, 1. ALBERT, A., ARMAREGO, W. L. F., AND SPINNER, E., 1961. J. Chem. Soc., pp. 2689, 5267. ALBERT, A., AND BaRLIn, G. B., 1959. J. Chem. Soc., 2384 (cf. zbid., idem., 1962, 3129). ALBERT, A., AND BaARLIN, G. B., 1963. J. Chem. Soc., pp. 5156, 5737. ALBERT, A., Brown, D. J., AND CHEESEMAN, G. W. H., 1952. J. 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P., 1962. ‘‘ Ionization Constants of Acids and_ Bases.’’ London: Methuen. ALBERT, A., AND SERJEANT, E. P., 1964. J. Chem. SOG ooDl. ANDERSON, B., AND SwaBy, R., 1951. Austral. J. Sci. Research, B4, 275. ANGIER, R., BooTHE, J., HUTCHINGS, B., Mowat, J., SEMB, J., STOKSTAD, E., SUBBAROW, Y., WALLER, C., CosuLicH, D., FAHRENBACH, M., HULTQUIST, M., Kun, E., NorTHEY, E., SEEGER, D., SICKELS, J., AND SMITH, J., 1946. Science, 103, 667. ANGYAL, S. J., AND ANGYAL, C. L., 1952. J. Chem. Soc., 1461. ARMAREGO, W. L. F., 1961. J. Chem. Soc., 2697. BLocK, S., 1956. J. Agr. Food Chem., 4, 1042. Brown, D. J., anD Mason, S. F., 1956. J. Chem. Soc., 3443. Davin, T. W. Edgeworth, 1931. J. Chem. Soc., 1039. ALBERT GorE, P., AND PHILLIPS, J. N., 1949. Nature, 163m 690. Hopkins, F. G., 1895. Phil. Trans. Roy. Soc., B, 186, 661. LERMAN, L., 1963. Proc. Nat. Acad. Sci., Wash NORDBRING-HERTZ, E., 1955. Physiol. Plantarum, 8, 691. PERRIN, D. D., 1962. PERRIN, D. D., 1963. J. Chem. Soc., 2648. PerRIN, D. D., 1964. Advances in Heterocyclic Chemistry (ed. A. R. Katritzky), 4, 43. J. Chem. Soc., 645. PURRMANN, R., 1940. Liebigs Ann. Chem., 544, 182; 546, 98. SIJPESTEIJN, A., AND JANSSEN, M., 1959. Antonie van Leeuwenhoek, 25, 422. STEARN, A. E., AND STEARN, E. W., 1924. J. Bact.; 9, 491. VERMAST, P. G., 1921. Biochem. Z., 125, 106. WILLiaMSON, J., 1959. Brit. J. Pharmacol. Chemother., 14, 443. Journal and Proceedings, Royal Society of New South Wales, Vol. 98, pp. 23-36, 1965 Late Quaternary Coastal Morphology of the Port Stephens-Myall Lakes Area, N.S.W. Bruce G. THOM Coastal Studies Institute, Louisiana State University, Baton Rouge Lomsiana, U.S.A. ABSTRACT—A vast array of Quaternary landforms and sediments occurs in the Port Stephens- Myall Lakes area of New South Wales. A study of this region’s geomorphology, supported by some subsurface data, suggests that during late Quaternary the area experienced two main periods of deposition. with shoreline recession and lower sea level. deposits in the form of a bay-barrier. These periods were separated by a phase of entrenchment which was associated Each depositional phase is recorded by transgressive The older of these barriers (Inner Barrier) lies landward of the younger (Outer Barrier) so that, stratigraphically, embayment fill is in the form of an offlap sequence. The Inner Barrier is associated in time with a late Pleistocene high sea level stand, while the Outer Barrier is considered to have formed during the Recent period. Introduction The sand masses that connect the rocky headlands along the New South Wales coast offer great scope for research in coastal geo- morphology and late Quaternary geology. Shepard (1960) has refered to features such as these as “ bay barriers ’’, an appropriate term in that they are separated from the country rock on the landward side by shallow-water lagoons or swamps. In New South Wales there have been very few studies of sand deposits except from an economic point of view (Gardner, 1955). This is in contrast to recent work on the sand islands of southern Queensland (Coaldrake, 1962), in the Gippsland Lakes district of Victoria (Bird, 1961a), and around the shores of Tasmania (Davies, 1959, 1961; Jennings, 1959). Studies in other countries, particularly the United States, clearly show the value of geomorphic- geologic research of sand barriers. Shepard (op. cit.) has mentioned their importance in providing studies in active sedimentation, and that, as buried sand facies between two mud facies, they are potential traps for the concentration of petroleum. Also in terms of the latest period in geologic history, the Quaternary, these sand masses may represent different periods of deposition, so their study is of possible use in understanding the Quaternary, a relatively neglected period in Australian geology. Regional Setting The Port Stephens-Myall Lakes area has features that are characteristic of a drowned coast. Marine sediments, of mainly siliceous sand, fill bedrock embayments and attain depths of 100-200 feet below present sea level (cf. bore data in David, 1907, pp. 53-59; Griffen, 1959). Within the embayments sand barriers enclose lagoons whose configuration is to a large extent determined by bedrock topography. Many lagoons are now filled by freshwater swamp or estuarine sediments. QUEENSLAND BRISBANE |. pe ee Na, SYDNEY 7: ae ~ = VICTORIA ‘\ MELBOURNE > “( Hobart BiG. 1 Map showing location of Port Stephens-Myall Lakes area 94 BRUCE G. THOM The bedrock consists of folded Carboniferous strata (chiefly lithic arenites, conglomerate, mudstones and interbedded volcanics), the folds trending from due north to N 40°W (Engel, 1962). The relief inland is dominated by strike ridges up to 1,000 feet in elevation. Near the coast these ridges are dissected to below present sea level producing isolated rock outcrops, as at Broughton Island. The region has a humid temperate climate which encourages the growth of plants upon the sand barriers. Rainfall averages 52 inches per annum at Port Stephens and Seal Rocks, while at Newcastle the average is 44 inches. Average monthly temperatures along the coast vary from 50-60°F in winter to 70-80° in summer. Onshore breezes dominate in summer, but in winter westerly winds generally prevail. At all times of the year southerly winds can be expected, usually accompanying storms. Swell waves that are generated in southern parts of the Pacific Ocean are 1egarded as significant in the alignment of wave-built coastal deposits in southern Austialia (Davies, 1960; Bird, 1961a). These waves promote beach fill in this area as do waves locally generated by north-easterly winds in summer. South-easterly swell predominates in winter, and it is common in this season for local storm winds to generate high energy wave conditions, which may cause considerable destruction of beach and foredune areas. Except along exposed sections of the shoreline where active sand dunes are characteristic (Fig. 2, Plate II), sand deposits are covered by trees and shrubs varying in height from a few feet to 80 feet as in the eucalypt forest near Seal Rocks. Ja general, the soils under vegetation tend to be weakly to strongly podsolized, the intensity of podsolization varying with the age of the deposit and topographic position. Coastal Landforms FLOODPLAINS, DELTAS, AND TERRACES Within the bedrock embayments of this coastal stretch several types of landforms can be recognized which are the product of fluvial, paludal. lacustrine, estuarine, and marine pro- cesses during the late Quaternary period. Floodplain deposits consisting of levees, back- swamps and filled channels of cut-off courses, form narrow strips along steep-sided valleys of the Karuah and Upper Myall Rivers and Boolambayte Creek, while the levees of the Karuah River extend beneath the waters of Port Stephens. These levees are partially covered by mangroves. At the southern end ~ of the region the Hunter River forms a more complicated delta which is filling in an estuary produced by entrenchment during the last glacial period. Older floodplains now in the form of river terraces line the sides of the bedrock valleys. They are most extensive in the Hunter River Valley where more than one terrace can be recognized. Radiocarbon dating of intact bivalves (Anadara trapeza) from within a terrace at Largs (>37,000 B.P.) at an elevation of 18-19 feet above H.W.M.., indicates that this and higher terraces are of Pleistocene age. Largs is located 19 miles inland from the sea. Terraces also exist along the Upper Myall River upstream from the town of Bulahdelah. LAGOONS More striking physiographic features within the embayments are the coastal lagoons (locally called lakes) enclosed by sand barriers. Lagoons vary greatly in size and shape depending on proximity to bedrock and relationship to barrier systems. For instance, the Myall Lakes are a series of interconnected water-bodies of irregular shape formed behind sand _ barriers with their shorelines abutting bedrock except on the seaward side (Fig. 2). Tilligerry Creek, on the other hand, and the swamps containing tracts of open water between barriers of the Fens and Eurunderee embayments are elongated parallel to the coastline and are of relatively uniform width. Systematic data on the bathymetry, hydrology and salinity are lacking for these lagoons. However, certain general features are noted. Locally, depths in the Myall Lakes exceed 30 feet, but in general they tend to be less than 20 feet. Salinity varies from fresh in the Myall Lake to brackish in Broadwater Lake. Reversed drainage of freshwater occurs during floods as Upper Myall River discharge is directed from Broadwater Lake into the Myall. Lake. Eventually flood waters escape to the sea along the tidally influenced Lower Myall River. This is a drainage channel into Port Stephens that follows an inter-barrier lagoon, now a swamp. Lunar tides are barely perceived in Broadwater Lake, but the water-level changes during floods when it has been observed to rise as much as 9 feet (1892 and 1927, H. Legge, personal communication). Sediments in the lagoons are quite varied. Along exposed shorelines facing fetches of 1-4 miles in length, sandy beaches and beach ridges have formed. They are well developed along LATE QUATERNARY COASTAL MORPHOLOGY 25 the eastern shore of Broadwater Lake (Fig. 4, C-C’). Preliminary observations reveal that lake bottoms are composed of soft mud and fine organic debris. At the exposed north-western end of the Myall Lake near the town of Bungwahl pro- jecting promontories of country rock have been cliffed by waves. Irregularly shaped blocks rest on narrow rock platforms just above mean lake level. In the bays between promontories sand and pebble beaches are found. The pebbles are well rounded and appear to be reworked Carboniferous conglomerate observed outcropping in the country rock. The problem, however, is that both beaches and bluffs are relic features. Casuarinas grow on and in front of the rock platforms, while a reed and swamp tree fringe extends into the lake in front of the beaches. As no marine fauna or extensive aeolian deposits have been found along these shores, the writer has concluded that both cliffs and beaches are lakeshore features. Past periods of more frequent storms is one possible explanation, but within the past few decades a local resident from Bungwahl (Mr. M. Bramble) has observed that the Myall Lake is silting up in certain areas. The relic shorelines therefore suggest a decrease in the intensity of wave action accompanying the siltation of the lake. SWAMPS AND Bocs Plants fringing the lagoons appear to be encroaching upon the remaining water bodies in a manner not unlike that described by Bird (19615) in the Gippsland Lakes. In many cases little open water remains and former lagoons have been converted into peaty swamps or bogs. Elongated bogs occur in the _ inter-barrier lagoons of the Eurunderee embayment (Plate I) and in the funnel-shaped re-entrants between beach ridges of the Upper Myall valley (Plate I). A number of generalizations can be gleaned from swamps and bogs in this area. First, siltation and swamp development are more advanced behind the innermost sand _ barriers. This point is well illustrated by the low-lying areas landward of Fens and Newcastle Bight embayments. Exceptions are the Myall Lakes where river discharge, depth of water, and length of fetch have inhibited complete enclosure. Second, the nature of sedimentation and types of encroaching plants depend on the environ- ment. Clays containing shells, commonly found in estuaries, and salt marsh and mangrove plants are significant in swamp development between Fullerton Cove and Tilligerry Creek and around the shores of Port Stephens. This contrasts with the organic-rich muds, silts and peats associated with freshwater plants of the Fens, Upper Myall and Eurundecee areas. PoRT STEPHENS Port Stephens as a geomorphic feature merits separate discussion. This extensive water body trends E-W and is open to the sea at the eastern end. On the northern side it is bordered by outcropping Carboniferous sediments. There is no evidence of aeolian deposits along these shores. The southern, eastern and western limits are, however, dominantly marine-aeolian deposits whicb link isolated Carboniferous outcrops to enclose Port Stephens (Fig. 2). Therefore, Port Stephens can be considered as a barrier lagoon with a perennial opening to the sea. Lunar tides are effective within this water body; the mean tide range of 4-2 feet at Nelsons Bay, just inside Port Stephens, is the same as at Broughton Island off the coast. This fact coupled with freshwater discharge of the Karuah River and Myall Lakes drainage produces an estuarine environment in Port Stephens. The history of sedimentation in Port Stephens during the late Quaternary appears complicated. Discontinuous beds of shells up to 15 feet in thickness are scattered over the floor of the estuary. Little is known of their composition and depositional bistory. Large sand accumula- tions occur at the eastern end of Port Stephens with finer sediments dominating at the western extremity near the outlet of the Karuah River. In the discussion below of coastal barriers, a Pleistocene age will be suggested for the innermost barrier formed in the Newcastle Bight embayment. This interpretation implies that at least the western part of Port Stephens was an estuary during the last interglacial or interstadial high sea stand following deposition of the Pleistocene barrier. The estuary achieved its present form after Recent (post-glacial) deposition in the Newcastle Bight, Anna Bay, and Tomaree Hill Dune areas. BEACH RIDGES AND SAND DUNES Hardrock headlands and isolated outcrops are linked by sand beach ridges. The alignment of these ridges within embayments appears to be determined by the wave fronts of refracted dominant swell which approaches from the south-east. Systems of multiple beach ridges, composed almost entirely of quartz sand, trend parallel to the shoreline indicating active accretion along this stretch of coast during the late Quaternary. It is possible to distinguish 26 BRUCE G. THOM WZ Bulahdelah Clan ae °* NZ1I97 Raymond bares Terrace Mobile Dune Sheet Bedrock Margin Stabilized Mantle of Swamp or Bog Dune Sand over Bedrock | ja, G-l4aiSite Inner Barrier Dunes Fic. 2 Index map of the Port Stephens-Myall Lakes area showing the location of radiocarbon samples, and Outer Barrier (Recent) mer Inner Barrier (Pleistocene) Stabilized Sand Dunes LATE QUATERNARY COASTAL MORPHOLOGY 27 two beach ridge systems as separate depositional units, to be referred to as Inner Barrier and Outer Barrier (Fig. 2 and Fig. 3). In many areas the surface of the barriers has been modified by wind action forming highly varied dune forms. An interesting aspect of geomorphic study in this area has teen the recognition of this wide variety of dunes, including those referred to in the literature by such terms as longitudinal, parabolic and transverse (Thom and Simonett, in preparation). Coastal Barriers DESCRIPTION Dual barrier systems are pronounced geo- morphic features in the Newcastle Bight, Fens and Eurunderee embayments (Fig. 2). Similar systems exist along other parts of the New South Wales coast (Langford Smith and Thom, in press). South of the entrance to Port Stephens ir the Tomaree Hill Dune area and in the Seal Rocks embayment, only one barrier surface is apparent. The intervening tract of lagoon or swamp is not present in these areas where windblown sand has moved inland from the sea and blanketed beach ridges and Carboniferous rock outcrops. Field studies of morphology and soils, together with analyses of aerial photographs and bore data,’ have strongly suggested that the barriers 1 Made available to the writer by the courtesy of Hunter District Water Board (H.D.W.B.) and the N.S.W. Department of Mines. + INNER BARRIER ——— Pleistocene with their component beach ridges and dunes, are separated by a distinct time line. It is considered that these differences may be useful in distinguishing Pleistocene from Recent coastal sand deposits in other areas of south-eastern Australia. 1. Inner Barrier System. Sand beach ridges of the Inner Barrier system are characteristically of subdued relief, standing 1-6 feet above swales (Fig. 4, D-DD’). The innermost, or first- formed, ridge crest usually stands 5-15 feet above the rest of the ridge series. Character- istically, this system encloses a swamp at the head of the embayment which is a relic of a former barrier lagoon. The linear pattern of these ridges is clearly seen on the air photo- graphs (Plate [). Ridge spacing varies from 300-600 feet, and profiles in different localities show that a series of ridges may gently slope either landward or seaward. Although the higher innermost ridge is forested, most sand ridges of this system are covered by low-growing scrub or heath. Generally the swales are water-logged and contain peat 1-2 feet in thickness. Belts of the paperbark (Melaleuca leucadendron sens. lat.) delineate the alignment of swales in many cases. Inner Barrier ridges are composed of leached incoherent quartz sand, varying in depth from 2-12 feet, and overlying an organic-bound sandrock forming a hardpan. Not all hardpans in the coastal siliceous sands of eastern Australia have the same origin (Coaldrake, 1955), but the OUTER ~<~BARRIER> Recent °e TEESE e008 4 MILES Fic. 3 Hypothetical cross section of the Fens embayment illustrating the writer’s ideas concerning the relationship between Inner and Outer Barriers pee - BRUCE G. THOM Japjo 8urjynqe saspl s1OYyseyL] Io}eMpPROoIg WD jouieg Jouuy oosepuniny ,q-q ! eunp o1yoqeaed ‘ jouIeg 191nQ sudy ,q-q { JowIeg 103nO WP sIq 9SPOMON ,W-V Fold 1324 ede te ee ee SOA * - wie Peesesen*e,* oe RAL en ee as Coecect ely : i . ‘ sa8plt yoveq sso19¥ sajyoid poffeasq seBpiy e10yse40] puns pezijiqnis LATE QUATERNARY COASTAL MORPHOLOGY 29 type beneath these beach ridges is cousidered to be the B horizon of a giant ground-water podsol. Although further work is necessary to substantiate this view, it is supported by the absence of macroscopic plant remains, the presence of humic colloids, and a relatively small amount of clay as cementing agents, the presence of overlying leached sand, and by the occurrence of sandrock at a higher level beneath the ridge than beneath adjacent swales. Bore data show that sandrock occurs widely beneath beack ridges but is patchily distributed underlying areas of windblown sands, such as the longitudinal dunes of the Tomago-William- town area (Newcastle Bight embayment). The sandrock underlying beach ridges is known to vary in thickness from a few feet to 46 feet, the maximum thickness logged by the Hunter District Water Board. As the elevation of the beach ridges ranges from 5-30 feet above sea level, it is apparent that the sandrock extends below present sea level in many localities. This is observed on the cut banks of the Lower.and Upper Myall Rivers where the ridges have been truncated by erosion, exposing the sandrock as low bluffs. A further characteristic of Inner Barriers is entrenched channels, most of which are at present occupied by alluvial fill and peat. They appear to be cut channels formed at a lower base level, probably when sea level was lower than at present. Although this entrench- ment is more clearly seen in other Inner Barriers of the New South Wales coast, the beach ridges that stretch inland for 6 miles in the Upper Myall River embayment have been truncated by the river. Swales of these ridges have also been entrenched (Plate III). In the Bombah Bog, peat and wood were recovered immediately: overlying a sand horizon at approximately 15-1€ feet below mean sea level. This material is overlain by a grey clay containing marine diatoms and peat of fresh- water origin. Bore data clearly show that the peat and clay layers do not extend beneath adjacent beach ridges. The fill of clay and peat seems to increase in thickness towards the river. However, much more work is necessary before the nature of alluvial fill in these entrenched channels is fully understood. Sand dunes on Inner Barriers are also subdued relief features. In the Eurunderee embayment a complex of parabolic dunes was recognized landward of the beach ridges (Plate I). The 2 Tron oxides have been reported as a cementing agent im some hardpans found in swamps of the Newcastle Bight Inner Barrier (Maze, 1942). arms of these features are generally less than half a mile long, and tend to be in the form of imperfect crescents. Their troughs are now swamps. The dune sand is strongly podsolized. Another area of dunes formed on an Inner Barrier is in the Newcastle Bight embayment (Fig. 2) where steep-sided ridges possessing a distinct E-W alignment cut across the trend ot beach ridges. Podsol soils in this district, described by Maze (1942), are also well developed. 2. Outer Barrier System. The Outer Barrier system of sand beach ridges, located across the mouths of embayments, is separated from the Inner Barrier by a tract of shallow lagoon or swamp. The characteristic ridge of this system has a sharper appearance than the Inner Bartier type. The difference in height between crest and swale varies from 4-12 feet, although locally a portion of a ridge may be 20 feet above adjacent swales. Outer Barrier ridges are also more closely spaced, the distance between ridge crests ranging from 60-300 feet (Fig. 4 A-A’, B—bB’, Plate II). The seaward decrease in height characteristic of Tasmanian beach ridge systems (Davies, 1958, 1961) has not been observed in comparable areas between Newcastle and Seal Rocks. Except in the vicinity of the foredune, being formed behind the present beach where soil development is lacking, the soils of Outer Barrier deposits are weakly to moderately podsolized. These soils consist of an ash-grey A horizon overlying a humic-stained, barely coherent B horizon. No hardpan has been recorded beneath the ridges of this system. The water table lies below the surface of the swales and, unlike Inner Barrier swales, hydro- phytic plants are absent. The more landward ridges are covered by Eucalyptus forest. with trees decreasing in height seaward. Near the foredune Banksta-Leptospermum scrub replaces the eucalypts. The foredune of the Outer Barrier, behind the present beach, characteristically is a sand ridge attaining heights of 50 feet or more, particularly at the northern end of embayments. In most areas the seaward face has been eroded by storm waves to form a poorly vegetated sand bluff. This sand bluff is often fronted by a low ridge, or terrace, partially stabilized by pons sand binding plants. In numerous localities the continuity of the foredune may be interrupted by blowouts. Further destruction of the foredune ridge by 30 lateral expansion of blowouts may leave a row of butte-like knobs or remanié dunes. The final removal of these knobs results in the formation of a mobile sand sheet which is driven inland as a broad front by onshore winds. The stabilized equivalents of blowouts and inland-facing fronts of mobile sand sheets are well preserved as high relief dunes on Outer Barriers. In the Newcastle Bight and Eurunderee areas sand ridges, covered by eucalypts, may exceed 100 feet in elevation. Exceptionally high aeolian accumulations form- ing ridges and sand sheets mantle bedrock at Tomaree and Seal Rocks. In both localities dune sand has been observed up to 300-400 feet above sea level. In all four areas these dunes have transgressed older surfaces such as swamps, bedrock, or scrub and forested dunes. For convenience, dunes of this type, whether active or stabilized, are referred to as trans- gressive dunes. Morphological and depositional contacts are quite marked in areas where aeolian transgression has taken place (Plate II). A large exposure in the dunes behind the beach at Belmont, about 12 miles south of Newcastle, revealed a strongly podsolized soil covered in places by 30 feet of bedded dune sand. Tall trees now stabilize the surface. AGE OF COASTAL BARRIERS? The problem of barrier age applies to the development of both Inner and Outer Barriers because of the sharp morphological and pedo- logical discontinuity between the two systems. Bird (1961a, p. 466), in considering the develop- ment of the “ outer barrier” in the vicinity of the Gippsland Lakes, Victoria, commented that : “The separation of the outer barrier [from earlier formed barriers] must indicate a relatively sudden emergence during Recent times, transposing the zone of barrier formation seaward. ..Under these con- ditions the outer barrier was initiated off-shore by wave action in water shallowed by emergence, in the way described by D. W. Johnson (1919).” This hypothesis rests on two assumptions, neither of which is considered valid when applied to barriers between Newcastle and Seal Rocks. First there is the view that a postglacial eustatic fall of sea level has occurred (ibid., p. 466), and second, that all the barriers of East Gippsland are Recent in age (ibid., p. 460). 3 For further discussion of coastal barriers, especially those of the Gulf Coast of U.S.A., see Shepard (1960). BRUCE :.G. THOM The evidence from New South Wales for a— higher stand of the sea during Recent times is not very convincing (Langford Smith and Thom, in press). Detailed regional studies in Eutope by Jelgersma (1961), and in the United States by LeBlanc and Bernard (1954), Bloom (1959), Redfield and Rubin (1962), and McIntire and Morgan (1962) show a lack of evidence which would indicate submergence above present high tide level during Recent times. Russell (1963 ; and personal communication) strongly questions the eustatic interpretations of Fair- bridge and Teichert along the Western Australian coast. In that area features cited as Recent in age appear more likely to be Pleistocene (ibid., p: 7). The second assumption of Bird, that all the barriers of East Gippsland are Recent in age, also seems inappropriate to the area under discussion. A pre-Recent (Pleistocene) high sea level age is suggested for the formation of the Inner Barrier in the Port Stephens-Myall Lakes area by : (1) the hardpan that exists beneath the beach ridges and extends below present sea level, (2) evidence of incision by streams into Inner Barriers, the cut channels at present occupied by alluvial fill, (3) beach ridge systems on the Inner Barrier often attaining elevations of 20-30 feet above present mean sea level, (4) the absence of a continuum between Inner and Outer Barrier beach ridge systems, (5) the marked morphologic and pedologic contrast between the two barriers, (6) the following list (Table I) of radiocarbon dates of material from Inner Barrier sites indicating that the deposition of barrier sand wedges of this type, with their component beach ridges, took place during a stand of the sea prior to the so-called Recent “ stillstand ”’. Only sample N.Z. 197 (Ferguson and Rafter, 1959) is in a stratigraphic position which pre- dates the age of Inner Barrier deposition. The shell was reported to come from a layer of fine sediment immediately beneath the barrier sand wedge. The other six dates were recently made for the writer by the Geophysical Laboratory and Exploration Department of the Humble Oil Company, Houston, Texas. 4 Bird elaborates on this view in a more recent paper (Bird, 1962); however, based on further field work in 1963, Bird now considers that a Pleistocene age is possible for some of the Gippsland barriers (personal communication). LATE QUATERNARY COASTAL MORPHOLOGY 31 TABLE I Sample No. Location Sample Approx. Elev. Age B.P. N.Z. 197 Newcastle Bight I.B. Anadara mollusc —50 ft. M.S.L. > 33,000 (G.R. 9046 ?) 0-1859 Bombah Bog Peat —15-16 ft. M.S.L. 11,075 +230 (G.R. 303802) 0-1854 Bombah Bog Peat and seeds —6—7 ft. M.S.L. 3,675 + 120 (G.R. 303802) 0-1860 Upper Myall I.B. Humic colloids +8 ft. M.S.L. 3,630 + 120 (G.R. 258842) 0-1856 Fens I.B. Humic colloids +6 ft. M.S.L. 4,550 +130 (G.R. 231670) 0-1855 Newcastle Bight I.B. Humic colloids +15 ft. M.S.L. 3,050 +115 (G.R. 753433) 0-1853 Belmont Charcoal +30 ft. M.S.L. 13,000 + 280 (G.R. 696173) These samples are of material which post-dates barrier formation. The charcoal at the Belmont site (0-1853) rests on a barrier surface which has been buried by layers of dune sand. The channel-fill sediments from the Bombah Bog, discussed above, post-date the deposition of the beach ridges. The peat dated at 11,075-++230 is probably of freshwater origin. As information from other areas shows that sea level 11,000 years ago was much lower than 15-16 feet below present M.S.L. (Shepard, 1961), it is reasonable to argue that the beach ridges in the Upper Myall Valley were deposited during a high sea stand of the late Pleistocene period. Channel cutting would therefore have occurred during a fall in sea level associated with the last glaciation, and the Recent eustatic rise is considered to have induced alluviation of the channels. The date of 3,675+120 at the base of the uppermost peat layer just above the clay containing marine diatoms may date only local environmental change or have more general significance.® The three samples of humic colloids were collected from different embayments (Fig. 1). The colloids were extracted from hardpan (sandrock) material which lay beneath a leached zone of 2-3 feet thickness. Two of the samples (0-1860 and 0-1856) were obtained just below (18-24 inches) the top of the hardpan, 6-8 feet above M.S.L. In both cases the hardpan > Dr. A. R. H. Martin is at present undertaking a extends below sea level for an unknown depth. The third sample (0-1855) came from a hardpan exposure in the centre of the sand plain near Williamtown. [lluviation of the colloids as part of the formation of a groundwater podsol is the suggested mode of accumulation. Such a phenomenon must post-date the deposition of the barrier, and therefore the age of the colloids at the base of the hardpan is propably greater than the 3,000—4,000 year dates obtained near the top. Clearly, more sandrock material is needed for radiocarbon analysis at depths below the dated samples. The Outer Barriers of the Port Stephens- Myall Lakes region are interpreted as late Recent in age. A significant geomorphic factor suggesting this is the lack of dissection quite typical of Inner Barriers along the New South Wales coast (Landford Smith and Thom, in press). Dissection appears to be associated with a major change in sea level and hence stream base level. Systems of beach ridges comprising Outer Barriers would therefore have been formed during the late Recent when sea level was at or near its present position. It has been difficult to find dateable materials beneath Outer Barriers. However, at Belmont, 12 miles south of Newcastle, a date was obtained : Sample 0-1849 should be treated with caution because the local stratigraphy is complicated, and possibly the sample was contaminated. However, it did come from beneath a parabolic dune which on morphology and soils evidence stratigraphic and palynological study of this bog. belonged to the Outer Barrier. Stratigraphic TABLE II Sample No. Location Sample Approx. Elev. Age B.P. 0-1849 Belmont Charcoal and peat —46—48 ft. M.S.L. 8,075 +175 (G.R. 703174) B2 BRUCE G. data supplied to the writer by Dr. A. K. Temple show that the podsolized Inner Barrier surface lies landward of the site of sample 0-1849. ORIGIN OF COASTAL BARRIERS It is therefore considered valid to assume two periods of barrier formation, and that the Inner Barriers are Pleistocene in age, and the Outer Barriers have formed since the sea level rose to its present position in Recent times after lowering during the last glacial period. This assumption is a prerequisite to the following analysis of barrier origin. Unfortunately bore data are inadequate beneath the barriers to establish accurately the bedrock profile. Most H.D.W.B. bores do not extend this far. The meagre information available indicates that depths to bedrock vary greatly. David (1907) and Griffen (1959) report depths of 192, 115 and 201 feet beneath the Outer Barrier in the Newcastle Bight embayment. In these bores the thickness of undifferentiated sand, overlying clay and gravel, was recorded as 176, 95 and 110 feet respectively. The Duckhole bores beneath the Inner Barrier show 73 and 84 feet of sand with bedrock at 150 and 212 feet respectively (ibid). There are no accurate topographic controls on bores from this embayment, so differences in depth may mean variation in bedrock relief and/or variation in the elevation of bores above sea level. Two bore holes in the Fens embayment, T.G. 2 and Y.B., although not exactly located on the section XX’ of Figure 2, have been used in the construction of the hypothetical diagram of embayment fill stratigraphy (Fig. 3). T.G. 2, a Hunter District Water Board bore, struck bedrock at 90 feet. The thickness of sandrock in this bore is 44 feet. The Y.B. bore, located nearer to Yacaaba Head on the Outer Barrier, encountered clay at 91 feet and bedrock at 163 feet (ibid.). Shallow holes of the H.D.W.B. and the writer, in both barriers, are the basis for surface contacts shown in Figure 3, but the Ledrock profile is largely hypothetical. It is not possible to test the hypothesis that the barriers are anchored on a surface lying within the expected range of wave erosion. This surface is considered to be 30 feet or less ‘below mean low tide under normal conditions (Russell, 1958; McIntire and Morgan, 1962). Anchored barriers are noted in the United States along the Gulf Coast and the Atlantic Coast in the vicinity of Plum Island (ibid.). In such instances the innermost ridge is not envisaged as an emerged bar, but as an upward growing THOM beach that rose over a Pleistocene subaerial surface during the rise of sea level, and when the sea reached its present position it anchored itself on this surface within the limits of effective wave activity. Zenkovitch (1962) has suggested a similar process for the origin of barriers which involves submergence of the land, and the landward shift of a shore ridge which forms a lagoon “‘in the place which have never been a part of the sea aquatorium ”’ (p. 117). The reason for the difficulty in testing the anchored barrier hypothesis in the _ Port Stephens-Myall Lakes area is that a possible anchor, the bedrock, occurs at unknown depths beneath the Inner Barrier, especially beneath the innermost ridge. Bedrock is certainly not the anchor for the Outer Barrier, but this does not preclude the possibility of a Pleistocene uncon- solidated surface extending seaward from the Inner Barrier underneath the present Outer Barrier (dashed line in Fig. 3). As is the case of the Outer Banks, North Carolina (Dr. D. D. Smith, personal communication), the sand section appears uniform in bore logs. It may be extremely difficult to differentiate between Pleistocene and Recent sediments beneath the Outer Barrier because of apparent sediment uniformity, and the possibility of reworked Pleistocene. material. The inter-barrier lagoons of Newcastle Bight, Fens and Eurunderee embayments not only indicate a time break between periods of development of the two barriers, but also show that the sea has not come in contact with these Inner Barriers in Recent times. It is likely that a protective barrier beach existed seaward during the rising sea level stage. Near the end of this stage, approximately 3,000-4,000 years ago (Gould and McFarlan, 1959; McIntire and Morgan, 1962; Coleman and Smith, 1964) this beach reached the position of the innermost beach ridge of Outer Barriers. Subsequent to the development of this ridge the barriers have prograded forming multiple beach ridges. GROWTH OF COASTAL BARRIERS It is not intended in this paper to discuss all the possible origins of accretionary sand beach ridges. There are numerous studies on the problem, many of which were considered by Davies (1957). More recent research undertaken by members of the Coastal Studies Institute, Louisiana State University, U.S.A., ais soon — be published. There are two main problems to be a in the accretionary growth of coastal L-arriers LATE QUATERNARY COASTAL MORPHOLOGY 33 in this region. One is the development of ridge and swale topography ; the other is the difference between Inner and Outer Barriers in spacing of ridge crests. (1) Under conditions of available sediment in the nearshore zone, the beach accretes by deposition during calm weather waves. Aggressive sand-binding plants, such as Spinifex Iursutus and Festuca littoralis, may then grow seaward onto the beach until they reach a point which is frequently awash at high tides. Onshore winds move sand from the foreshore into this plant zone where it accumulates, forming a ridge parallel to the shoreline. Oscillation in the growth of the prograding beach controlling the seaward position reached by pioneer plants is suggested as the important factor in ridge and swale development. Ridges formed of a wave deposited base and an aeolian cap vary in height according to the thickness of wind-blown material. Therefore the height of the ridge is in direct relation to the length of time the strandline 1emained at a fixed position. This hypothesis, the wave-wind hypothesis, is in contrast to the view that storm-wave deposits form beach ridges as observed along the shores of the Mexican Gulf coast in Tabasco and Campeche (Thom, 1964). Evidence for the wave-wind process is not fully conclusive, and more work involving studies of beach-ridge stratification and the distinction of wave from wind deposited sand remains to be undertaken in New South Wales. However, profiles across Outer Barrier ridges (Fig. 4, A-A’, B—B’) show considerable variation in relief. These should be compared with the profiles across ridges of the eastern shore of Broadwater Lake (Fig. 4, C-C’), which have been formed by wave deposition. Wind deposition is insignificant bere where Casuarina spp. and Melaleuca spp. fringe the lakeshore. These ridges compare favourably with those observed in Mexico both in form and apparent origin. (2) Most marked in this coastal region is the difference in spacing between beach ridges of the Inner Barrier and those of the Outer Barrier. A similar difference has been observed elsewhere along the New South Wales coast, but it is not always present (Langford Smith and Thom, in press). Gill and Banks (1956) report this 6 The large ridge of Figure 4, C—C’, and associated dunes appear to ante-date the Outer Barrier which formed Broadwater Lake and the consequent diversion of Myall Lake drainage through the iuter-barrier lagoon of the Fens embayment. Cc spacing difference between iidges of apparent Pleistocene age and those of Recent age located along the coast of north-western Tasmania. McIntire (personal communication) reports a similar phenomenon from the Cockburn Sound south of Perth. Investigations by the writer in Horry County, South Carolina, U.S.A., show that ridges on older and more landward Pleistocene barriers are more widely spaced than those on younger Pleistocene barriers. At present it is not possible to generalize to the effect that the older the barrier, the wider the Spacing ; or the more landward the barrier in an embayment situation, the wider the spacing, or whether the wider spacing is simply a function of time, and that degradation processes have caused the flattening of many ridges. Much more comparative work has to be undertaken in Australia and other parts of the world. Pleistocene barriers are well preserved along the Texas Gulf Coast (Price, 1933, 1947; LeBlanc and Hodgson, 1959) and south-east Brazil (Delaney, Coastal Studies Institute. in press). LATE QUATERNARY GEOMORPHIC HISTORY At present only tentative conclusions can be made regarding this region’s geomorphic history. The basis for the following interpretation are the geomorphic and pedogenic contrasts between the two sand barriers, discussed elsewhere in this paper. A major time break is indicated by these contrasts, and this time break is considered to be the late Pleistocene fall in sea level accompanying the last glacial period. As a first approximation, the late Quaternary geomorphic history of this coastal stretch may be summarized as follows : 1. Late Pleistocene High Sea Level Stage. During this period, corresponding to an inter- glacial or interstadial, wave and wind processes operating at, or slightly above, present sea level produced the Inner Barrier. It may be that the subdued parabolic dunes landward of beach ridges in the Eurunde-ee embayment were formed as the sea 10s to this level following a previous glacial period. The Inner Barriers were constructed within embayments enclosing water bodies, many of which are now swamps. Stratigraphically it appears that beach and dune facies form a wedge tapering inland over discontinuous lenses of older Quaternary gravels and clays, which in turn rest upon a seaward- sloping bedrock surface. 2. Late Pleistocene Lowering and Low Sea Level Stage. The last glacial period (Wisconsin- —— a 34 BRUCE‘G. THOM Wurm) was characterized by a fall in sea level, possibly as much as 450 feet (Russell, 1957). Streams such as the Hunter, Karuah and Upper Myall, entrenched them valleys. The last mentioned cut through a beach ridge series. These valleys along with the shoreline extended seaward an unknown distance towards the edge of the continental shelf. Most sediment was deposited on the outer edge of the present shelf, the upper slope, and in deeper environments. Very little is known about the nature of sedi- mentation during this period. 3. Early Recent Rising Sea Level Stage. About 17,000 years ago sea level started to rise (Shepard, 1961) and transgress the subaerial Pleistocene surface. Unlike areas of the Gulf Coast of the U.S.A., it is not yet possible to identify this surface in the stratigraphic record. It may have been destroyed by reworking along the shoreline of the rising sea. The top of the clay reported from bore logs beneath Outer Barriers may be this surface. Associated with sea transgression has been the alluvial infilling of river channels and embayments by fine sediments, organics, and sand deposits. This phenomenon, referred to as alluvial drowning, has been reported from many other parts of the world (Russell, 1957). The sandrock hardpan beneath Inner Barrier beach ridges appears to have formed as sea level rose. The water table in these barriers, rising with sea level, could have been the locus of deposition of humic colloids being translated downwards through the sand. The dates of 3,000-4,500 years B.P. near the top of the hardpan obtained from different localities do not refute this hypothesis. On the contrary, they support the view that sea level, with the water table at some elevation above, reached its present elevation somewhere between 3,000 ana 5,000 years ago. 4. Recent Standing Sea Level Stage. During this period rivers have continued to alluviate their valleys, and estuaries such as that of the Lower Hunter have been greatly infilled. Sedimentation within embayments has been characterized by shoreline progradation. The Outer Barrier has formed by the accretion of multiple beach ridges which seems to have taken place in the early part of this period, probably under conditions of abundant sand supply in the nearshore zone. The giadual depletion of these supplies is a possible explana- tion for the cessation of accretion. A discussion of factors responsible for the later development of coastal dunes are beyond the scope of this paper. Acknowledgements a This work was initiated in 1960 while the writer was an Honours student in the Geography Department, The University of Sydney. Field work was continued during 1961 and early 1962. The writer discussed the problems of this study with many people. In particular, he is indebted to Mr. J. N. Jennings, Mr. P. McKenzie, Dr. T. Langford Smith, Dr. R. G. Galloway, Mr. J. L. Davies, and Dr. D. S. Simonett for them invaluable advice and encouragement while the writer was in Australia. Dr. A. R. H. Martin and the writer worked together in the Bombah Bog, and the writer is grateful to him for his helpful instruction in the field, and for numerous discussions In the laboratory. He is also grateful to the N.S.W. Department of Mines and Hunter District Water Board for provision of various facilities. At the Coastal Studies Institute, Louisiana State University, the writer has participated in many useful discussions relevant to this paper, and has received helpful comments on the manuscript from his colleagues, particu- larly Dr. W. G. McIntire. Professor G, Dury, Dr. D. S. Simonett and Mr. J. N. Jennings have also commented on the manuscript. Appreciation is also expressed to Dr. H. N. Fisk and the personnel of the Geochemical Laboratory of Humble Oil Company, Houston, Texas, for the radiocarbon assays reported in this paper. References Birp, E. C. F., 196la. The coastal barriers of East Gippsland, Australia. Geogr. J., 127, 460-468. BirD, E. C. F., 19616. Reed growth in the Gippsland Lakes. Vic. Nat., 77, 262-268. ; Birp, E. C. F., 1962. The physiography of thay, Gippsland Lakes, Australia. Zeit. fiir Geom., 7, 232-245. Bitoom, A. L., 1959. sea level in southwestern Maine. Naval fees. (Contr. N onr 609 (25). NR 288 040, 1-142. COALDRAKE, J. E., 1955. Fossil soil hardpans and coastal sandrock in southern Queensland. Aust. J. Set., 17, 132-133. CoOALDRAKE, J. E., 1962. Late Pleistocene changes of Rept. Office Project No. The coastal sand dunes of southern Queensland. Pyroc. Roy. Soc. Qam 72, 101-116. CoLEMAN, J. M., AND SmitH, W. G., 1964. Late Recent rise of sea level. Geol. Soc. Amer. Buil., 75, 833-840. Davin, T. W. E., 1907. The geology of the Hunteg River Coal Measures, New South Wales. Mem. Geol. Surv. N.S.W., 4, Part 1, Govt. Print.j Sydney. Davirs, J. L., 1957. in the development of sand beach ridges. J. Set., 20, 105-111. Davies, J. L., 1958. Analysis of height variation in sand beach ridges. Aust. J. Sct., 21, 51-52. : The importance of cut and fill Aust. LATE QUATERNARY COASTAL MORPHOLOGY 35 Sea level change and shoreline mavies, J. L., 1959. Pap. development in south-eastern Tasmania. and Proc. Roy. Soc. Tas., 93, 89-95. Davigs, J. L., 1960. Beach alignment in southern Australia. Aust. Geog., 8, 42-44. Daviess, J. L., 1961. Tasmanian beach ridge systems in relation to sea level change. Pap. and Proc. Roy. Soc. Tas., 95, 35-40. DELANEY, P. J. V. Geology and geomorphology of the coastal plain of Rio Grande do Sul, Brazil and Northern Uruguay. Coastal Studies Serves, Louisiana State University Press, in press. ENGEL, B. A., 1962. Geology of the Bulahdelah- Port Stephens district, N.S.W. J. Proc. Rov. Soc. NoS.W.,°95, 197-215. FEerGusson, G. J., AND RAFTER, T. A., 1959. New Zealand 14C age measurements—4. N.Z. /f. Geol. Geophys., 2, 208-241. GARDNER, D. E., 1955. Beach-sand heavy mineral deposits of eastern Australia. Bull. Bur. Min. Resour. Aust., 28, 1-103. Girt, E. D., anp Banks, M. R., 1956. Catnozoic history of Mowbray Swamp and other areas of north-western Tasmania. ec. Q. Victoria Mus. Launc., N.S. 6, 1-42. GouLp, H. R., anp McFar tan, E., 1959. Geologic history of the chenier plain, Southwestern Louisiana. Gulf Coast Assoc. Geol. Socs. Trans., 9, 237-260. GRIFFEN, R. J., 1959. Port Stephens area. IN. S.W., 7, 67-79. JELGERSMA, 5S., 1961. the Netherlands. Ser. C, 6, No. 7. JENNINGS, J. N., 1959. The coastal geomorphology of King Island, Bass Strait, in relation to changes in the relative level of land and sea. Rec. Q. Victoria Mus. Launc., N.S. 11, 1-39. Jounson, D. W., 1919. Shove Processes and Shoreline Development. John Wiley, New York. LANGFORD SMITH, T., AND THom, B. G. New South Wales coastal morphology. jj. Geol. Soc. Aust., in press. Groundwater resources of the Tech. Rep. Geol. Surv. Holocene sea level changes in Med. van Geol. Stichting, (Received March 17, 1964 ; LEB.anc, R. J., AND BERNARD, H. A., 1954. Résumé of Late Recent geological history of the Gulf Coast. Geol. en Mijnb. (N.W. Ser.), 16e Jaar., 185-194. LEBtanc, R. F., AnD Hopeson, W. D., 1959. Origin and development of the Texas shoreline. Pvroc. 2nd Coastal Geog. Conf., Baton Rouge, 57-101. McINTIRE, W. G., AND Moraan, J. P., 1962. Recent Geomorphic History of Plum Island Massachusetts and Adjacent Coasts. Louisiana State Univ., Coastal Studies Inst., Tech. Rept. No. 19, Cont. No. 62-7, 1-44. Maze, W. H., 1942. of the Newcastle-Sydney district. 4, 107-112. . PrRIicE, W. A., 1933. Role of diastrophism in topo- graphy of Corpus Christi area, south Texas. Bull. Amer. Assoc. Petrol. Geols., 17, 907-262. PricE, W. A., 1947. Equilibrium of form and forces in tidal basins of coast of Texas and Louisiana. Bull. Amer. Assoc. Petrol. Geol., 31, 1619-1663. REDFIELD, A. C., AND RuBIN, M., 1962. The age of salt marsh peat and its relation to Recent change Sand beds and humus podsois Aust. Geog., in sea level at Barnstable, Massachusetts. Nail. Acad. Sci. Proc., 48, 1728-1738. RUSSELL, R. J., 1957. Instability of sea level. Amey. Scientist, 45, 414-430. RUSSELL, R. J., 1958. Long, straight beaches. clog. Geol. Acilvet., 51, 591-598. RussELL, R. J., 1963. Recent recession of tropical cliffy coasts. Science, 139, 9-15. SHEPARD, F. P., 1960. Gulf Coast barriers. In Recent Sediments, Northwest Gulf of Mexico, 1951-1958. A.A.P.G., Tulsa, Olkahoma. SHEPARD, F. P., 1961. Sea level rise during the past 20,000 years. Suppl. Zeit. fiir Geom., 3, 30-35. THom, B. G., 1964. Origin of sand beach ridges. Aust. J. Sct., 26, 351. ZENKOVITCH, V. P., 1962. Some new exploration results about sand shores development during the sea transgression. De Ingenieur, No. 17, Bouw-en Waterbouw Kunde 9, 113-121. revised October 10, 1964) 36 BRUCE G. THOM 3 Explanation of Plates PLATE of Aerial photograph of the Eurunderee embayment showing parabolic dunes of the Outer Barrier separated from Inner Barrier beach ridges and dunes by a freshwater bog. (Published with permission of N.S.W. Department of Lands.) PLATE If Aerial photograph of the eastern end of Newcastle Bight embayment. The sheet of mobile sand is encroaching upon Outer Barrier beach ridges and stabilized dunes. A former phase of dune invasion is shown by a stabilized dune overlying beach ridges. (Published with permission of N.S.W. Department of Lands.) PLATE III Upper Myall River in a steep-sided embayment. Pleistocene beach ridges have been truncated by the river, and swales have been entrenched. Sites of radiocarbon samples are shown. (Published with permission of N.S.W. Department of Lands.) JOURNAL ROYAL SOCIETY N.S.W. THOM PLATE I JOURNAL ROY AL SOCIETY INGS AW. THOM PLATE II Sours ee JOURNAL ROYAL SOCIETY N.S.W. THOM PLATE a Journal and Proceedings, Royal Society of New South Wales, Vol. 98, pp. 37-83, 1965 The Stratigraphy of the Hervey Group in Central New South Wales J. R. CONOLLY School of Applied Geology, University of New South Wales Kensington, N.S.W. ABSTRACT—The outcrop distribution, structure, and stratigraphy of the sediments of the Hervey Group in Central New South Wales is outlined. These sediments were mainly deposited during the Upper Devonian although sedimentation probably started in the Middle Devonian and continued into the Lower Carboniferous. The Hervey Group is subdivided into three Sub-Groups called the Beargamil, Nangar and Cookamidgera Sub-Groups and the outcrop of these rocks is shown on seven geological maps. Generally the basal sediments of the Hervey Group are characterized by red arkosic or lithic sandstones, and red siltstones and mudstones. These red measures have been grouped into the Beargamil Sub-Group and generally unconformably overlie Silurian to Lower Devonian acid volcanics, Middle Devonian granites or older Silurian and Ordovician sediments. The Beargamil Sub-Group is overlain by a thick sequence of white quartzose sandstones, conglomerates, red siltstones and mudstones forming the Nangar Sub-Group. Jed quartzose siltstones are the most abundant rock type and are interbedded with red and white quartzose sandstones, pebbly sandstones and conglomerates in a cyclic pattern. Upper Devonian fish-plates and plants are commonly preserved throughout the Nangar Sub-Group. The Nangar Sub-Group reaches thicknesses of over 5,000 feet and is overlain by a thick sequence of red beds grouped into the Cookamidgera Sub-Group. These rocks mainly consist of red siltstones and red mudstones with minor amounts of red lithic and quartzose sandstones. During the upper Middle Devonian to lower Upper Devonian, arkosic and lithic red beds were deposited on an alluvial plain which was flanked to the north-west and east by a shallow marine shelf and to the south by a landmass. In the Upper Devonian the sea regressed to the north and east and most of central New South Wales was an extensive alluvial flood plain. Rivers flowing from the west and then southwards around a land barrier to the south deposited quartzose sediments, silts and muds in the flood plain of large rivers and in large inland lakes. This style of sedimentation probably continued into the Lower Carboniferous with extensive deposition of fine-grained red silts and muds. Introduction During the Palaeozoic, Eastern Australia was the site for extensive sedimentation and volcanic activity. Deposition was interrupted by several periods of folding and granite intrusion, welding the Palaeozoic rocks onto the continental block by the end of the Palaeozoic. The oldest sediments of the Palaeozoic in New South Wales belong to the Cambrian Period and sedimentation continued into the Upper Devonian in the central, western, and southern part of New South Wales, and into the Permian in the northern and eastern part of New South Wales. Hence the last period of sedimentation in the Palaeozoic of central western New South Wales occurred during the Upper Devonian. The Upper Devonian sediments of central western New South Wales are preserved in meridionally elongated outliers, normally lying on the eroded ‘surface of folded older Palaeozoic rocks. In general, detailed stratigraphy is unknown and the fossilrecord is poor. Although the sediments are relatively poor in fossils, a marine fauna is (common within the eastern area, while a fish fauna is characteristic of the western area. Lepidodendrid plants are scattered throughout all groups and in some areas, Archaeopterid and Rhacopterid plants may be representative of a Lower Carboniferous age (Conolly, 1964). Upper Devonian rocks outcrop throughout eastern, central, and western New South Wales (Figs. 1 and 2). The Upper Devonian rocks of the Lachlan Geosyncline have been described (Conolly, 1964) and three broad provinces delineated. The rocks of the Lambie and Catombal Groups and the Upper Devonian rocks of the Yalwal-Eden district form the eastern province. The Mulga Downs and Cocoparra Groups form the western province and the Hervey Group the central province (Fig. 2). In a preliminary report on the rocks of the Hervey Group, the author (Conolly, 1964) defined the Hervey group and suggested that it could be subdivided into three sequences which could be given Sub-Group status. These three Sub-Groups were not defined, since it was intended to define them and to discuss the stratigraphy in detail in this paper. 38 J. R. CONOLLY ' ' 1 | NORTHERN ' 1 TERRITORY 1! ! 1 ! ewer == ; ae i / 2 i NEW $0UTH Wwates Sa 1 i 7 a Lee ty J } ! ary i . 1 x Pa H g $ I Fic. 1 Locality map showing area included in ig. 2 Field investigations on the Upper Devonian sediments of central western New South Wales were started in March, 1958. From this time to November, 1959, the author studied the Upper Devonian sediments of the Catombal Group in the Wellington-Molong region (Conolly, 1960, 1963). From January, 1960, to February, 1962, field work was carried out on the other Upper Devonian sediments in central western New South Wales. Most of this latter period was spent mapping the Upper Devonian sediments of the Hervey Group which outcropped over a large area of central New South Wales (Figs. 2, 3). Previous Investigations Only three attempts have been made to form a concise account of the regional geology of the Condobolin-Peak Hill-Forbes district. In 1910, Andrews described the geology of the Forbes- Parkes goldfields and later in 1937, Raggatt published an account of the geology of the Condobolin-Trundle area. David and Browne (1950, pp. 249-250) described the Upper Devonian rocks from east and west of Forbes and Parkes, and gave the hitherto most complete account of the fauna and flora of these sediments. Other brief notes published on the geology of central New South Wales have been made by Wilkinson (1885) who described the shallowly- dipping Upper Devonian ranges to the east of Parkes, and Dun (1898) who described Upper Ordovician graptolites from Peak Hill and also described the fossil assemblages of the Silurian and Devonian which are listed in Andrews’ account of the Forbes-Parkes goldfield. An account of the regional geology of the Forbes-Narromine military four mile area has been prepared by the author from knowledge of previous work and his investigations of the geology of the Bogan Gate-Trundle district, and the Forbes district. cone: “1 elottenham | °Narromine | SYDNEY BASIN ®Naradhan nkin Springs Yalgogr in 8 § Se ee EY a Qe ro) 2 ZORRE xK oO [eo] 3 a oF = fe oO | “Griffith \Sacatetnon Mie a en | ‘5 a6 50 \ et miles rrandera | ° ° 14 151° m5" | 35°S i J oI Sea ol SSR 8 le 359 OUTCROP DISTRIBUTION OF UPPER DEVONIAN SEDIMENTS IN CENTRAL WESTERN NEW SOUTH WALES E=1 Lambie Group Hervey Group ZA Catombal Group [J Mulga Downs Group BS Cocoparra Group Fie. 2 SERATIGRAPHY* OF (HERVEY GROUP IN: CENTRAL N.S.W. 39 The Geological succession at Forbes is : quartzose greywackes with turbidite structures. Massive sandstones with fragmentary fossils, including Rhynchonella, Pterinaea, Pleurotomaria and Orthis (Andrews, 1910, p. 25). subgreywackes, limestones and conglomerates with Halysites australe, Tryplasma, Heliolites, Favosites, Spongo- Quartzose shales and laminated mudstones, often marly, grading into The Graptolites include species of Climacograptus. Top Upper Devonian Hervey Group ? Erosional gap Lower—? Middle Devonian 1,000’ + Silurian Interbedded shales, 2,500 + phyllum. Upper Ordovician 1,500’ + BASE This succession has been measured in the anticlinal structures preserved immediately to the west of Forbes and previously mentioned by Andrews (1910, p. 23). The succession near Forbes appears to be quite conformable, although the Upper Devonian sandstones of the Hervey Group probably unconformably overlie the older rocks. The sequence beneath the Upper Devonian represents a one-way trend from older deepwater to younger shallow-water marine shelf sediments in the Lower Palaeozoic. These sediments are often overlain by thick piles of acid volcanics, both to the east of Forbes in the Manildra district, and to the west in the Bogan Gate- Trundle district. In many localities acid lavas of this age unconformably underlie the Upper Devonian Hervey Group. To the east of the meridian of Parkes, the Lower Palaeozoic sequence thickens considerably and Steggles (1961) and Ringis (1962) have mapped areas to the north-east of the Hervey Syncline (Fig. 3) which show a thickness of over 25,000 feet of marine sediments, probably of Ordovician- Silurian age. A similar succession exists to the south of Mandagery railway station (Fig. 8), where there is a thick sequence of greywackes and shales. Hence there appears to be a shallowing of the sea to the west during the Lower Palaeo- zoic with shelf deposits being deposited in the Trundle-Forbes area and a deeper-water trough facies deposited to the east of Parkes, Forbes and Peak Hill. Large areas of granitic rocks outcrop in central New South Wales and include the Yeoval Granite (Fig. 6), the Eugowra Granite (Figs. 8, 11) and the Young Granite (Fig. 13), which probably all belong to the one massif and intrude the Lower Palaeozoic sequence including the Lower Devonian acid lavas. Both the granites and older stratified rocks are unconformably overlain by Upper Devonian sediments. The age of the granites is provisionally placed as Middle Devonian. Small isolated granite masses also outcrop in the Condobolin-Bogan Gate district (Figs. 15, 17, 19) and may also be of Middle Devonian age. Upper Devonian fish plates from the sediments of the Hervey Group have been described by Hills (1932, 1935) and include Bothriolepis, Phyllolepsis, Dipterus, Remingolepsis; from Gingham Gap in the Hervey Syncline ; and from Jemalong Gap west of Forbes, a very large dermal plate of Bothriolepis. Other recorded fossils (David and Browne, 1950, pp. 249-250) include Archaeocalamites and Lepidodendron australe at Jemalong Gap, Calamitoid remains in the Corradgery Range near Jemalong Gap, Lepidodendroid remains from the Hervey Syncline and further south at Canowindra where they were associated with Lingula gregaria, marine fossils from Grenfell, and in the Trundle, Bogan Gate, Condobolin district marine fossils, including Sfpirifer pittmani at Mineral Hill, north-west of Condobolin. Raggatt (1937) measured a section through the Devonian sediments in the Condobolin district and he also observed a similar sequence near Bogan Gate where he noted fossiliferous marine bands near the base. Raggatt also noted that the Devonian rested with marked unconformity on older metamorphics, rhyolites and fossiliferous limestones. Structural Setting of the Hervey Group The Hervey Group outcrops in three major synclinal belts which are elongated in a north- south direction. These belts include an eastern belt with many minor folds, a central belt called the Tullamore Syncline and a western belt called the Murda Syncline (Fig. 3). The eastern belt has a total outcrop length of 140 miles and a maximum width of 24 miles from east of Parkes to Manildra but near its northern and southern extremities, the belt is only four to seven miles wide. A similar large synclinal structure runs parallel to the eastern belt and at a distance of about 20 miles to the west of it. The northern half of this area is called the Tullamore Syncline 40 J. R. CONOLLY * Condobolin OUTCROP DISTRIBUTION OF THE HERVEY GROUP IN CENTRAL WESTERN N.SW. Inset agreas show localities of Maps. 0 & 16 32 et —— ret —— tot scale in miles Weddin Range Hervey Syncline ‘Sy Koorawat Syncline Young @ Be congou Syncline ® Cootamundra EG a3. which is a very open structure extending from north of Tullamore at least 80 miles southwards towards Cootamundra. It has an average width of 10 miles in an east-west direction and may extend southwards to the Congou Syncline four miles to the north of Cootamundra. A third synclinal structure occurs parallel to the Tullamore Syncline and at an average distance of 35 miles to the west of it. The structure has a thin southern nose to the north of Condobolin but broadens considerably to the north and has been called the Murda syncline. There is no apparent link between these three synclinal belts except south of Grenfell where the Wheoga and Weddin Ranges sweep in an easterly direction towards the south-western portion of the Hervey Group at Grenfell. In this area the outcrops of both belts are only separated by a distance of twelve miles. The Weddin Range probably represents a broad anticlinal bend towards the eastern belt from the Tullamore Syncline. These three broad synclinal structures are probably remnants of a large blanket of Upper Devonian sediment that was draped over the older Palaeozoic basement and has suffered broad warping and open folding. Extensive erosion has produced a flat plain where the three meridinal synclinal belts of Upper Devonian rocks outcrop above the older Palaeozoic base- ment rocks and Tertiary to Recent alluvial deposits. STRATIGRAPHY OF HERVEY GROUP IN CENTRAL N.S.W. Al TABLE 1 Sivatigraphy of the Hervey Group (Upper Devonian—Lower Carboniferous) in Central New South Wales Gooloo- Koora- Trundle- Hervey Parkes- gong- watha Weddin Tullamore Bogan Murda Syncline Manildra Grenfell Syncline Range Gate Syncline COOKAMIDGERA SUB- Burrill Undiffer- Not GROUP Fm. entiated exposed Upper red beds Eurow Undiffer- Koora- Undiffer- Undiffer- Belvedere Fm. entiated watha Fm. entiated entiated Fm. NANGAR SUB- Caloma Bumberry GROUP Shee Fm. Rhythmic — succes- Pipe Pipe Bumberry Bumberry Not sion of white Fm. Fm. Em. Fm exposed sandstones with Mandagery Mandagery Mandagery Mandagery Weddin Weddin Weddin Boona red sandstones So: 5:5: SyieH S23: SEO Seer oor Sos and red _- silt- Cloghnan Cloghnan stones Shale Shale Troffs Troffs Fm. Fm. BEARGAMIL SUB- Kadina Kadina Hunter GROUP Fm. Fm. Siltstone Basal red beds, lithic Clagger Peaks Bendick Bogan Not Bogan ? Con- sandstones, ar- Ss: S.S. with Fm. Gate exposed Gate dobolin koses Mogongong hen Sane Po Congl. Member Outline Stratigraphy of the Hervey Group The type section of the Hervey Group was defined by Conolly (1964). The type section was measured along Clagger Creek to the Caloma Trig, six miles north-east of Hervey Park at the northern end of the Hervey’s Range (Fig. 6). The section here is 5,250 feet thick and consists of the following subdivisions : Cookamidgera Sub-Group is not preserved in this area but occurs in the southern half of the Hervey’s Range which is downfaulted against the northern half (Fig. 6). The Hervey Group outcrops discontinuously over an area of over ten thousand square miles (Fig. 2). Variations in total thickness over this area are only apparent because of extensive Thickness Top in Feet Caloma Sandstone White orthoquartzites, forming rugged cliff outcrops 750’+ Nangar | Sine Formation Green and red shales and siltstones with occasional Sub-Group < white sandstone members ‘ 820° | Mandagery Sandstone White sandstones interbedded with red siltstones and occasional red sandstones .. tote 1,720’ Kadina Formation Red siltstones with red sandstone members LTO’ Beargamil Clagger Sandstone Thin conglomerates at the base going into massive red Sub-Group and green sandstones and siltstones 850’ TOTAL 5,250’ + BASE At this locality, the Hervey Group is separated erosion of the upper formations. Correlation from older Palaeozoic andesites to the west by a thin strip of boulder drift and alluvium. On the north-eastern side and in the southern section of the Hervey’s Range, the Upper Devonian overlies acid volcanics of probable Lower Devonian age with a slight unconformity. The Caloma Sandstone, Pipe Formation and Mandagery Sandstone belong to the Nangar Sub- Group and the Kadina Formation and Clagger Sandstone to the Beargamil Sub-Group. The becomes difficult because of the large erosional gaps and facies changes, resulting in the erection of numerous formational names which are shown on the correlation chart (Table 1) and on the correlation diagrams (Figs. 4 and 5). THE BEARGAMIL SUB-GROUP The type section was measured one half mile due east of Beargamil Dam on the western flank of the Bumberry Syncline (Fig. 8). In J. R. CONOLLY 42 ‘WJ 4Ipuag "EL 9U0}S}}IS Ja}UNH ZL Jaquay ‘]6uog Buocbucboey, ‘11 “S'S S02d OL ‘W4 DUIPDY “Z ‘S'S 4e6b0)9 | dNOY9- ENS IWVOYNVSd ‘wy Assaquing 1 ‘S'S DUO 'S ‘Wy adig 'y ‘S'S Kuabopuop '€ dNOY9- ANS YVINVN “W4 DYJDMDIOIY “P| P9zD1}UII9}J PUT) 6 ‘W4 MOINZ -g ‘U4 y!44Ng *g dNOyd - Ns VesSCINVHX005 dno“ ASAYSH QN3951 VyMO9NS eg SAMY Wd auijauhs Aa Asay ; 9U0}S }IS 3 3U0}SPUDS / auoyspuos A\qqag aUu0|Spu0S 2)0uS ‘au038}7tS ‘wesBbeip Ay1)e90) ay} uo UMOYS ase SUWN)OD painseaw yo Suol}Sod ayL MS'N ‘ANIMONAS VHLVMVNOOM FHL OL ANITONAS AFAMSH AHL WONS dNOY9 AZAYSH FHL 40 WVYOVIG NOILV1aYYOo GNV SNWN109 SIHdVYSILVYLS 43 STRATIGRAPHY OF HERVEY GROUP IN CENTRAL N‘5S.W. OONINYNW ® aurj2uhs BYyYEMEIOOH VHLVMVYOO™ dvH ALIWVI07 YOS SSW NI 37V9S SL OL S 0 S ooo? = ,} 37S NWN109 STRATIGRAPHIC COLUMNS AND El, eee CORRELATION DIAGRAM OF THE eal HERVEY GROUP FROM THE HERVEY SYNCLINE TO THE KOORAWATHA SB i SYNCLINE, NSW. 2 | Eiistone Sandstone 2] Pebbly Sondstone The positions of measured columns are shown on the locality diagram COLUMN SCALE {" = 2000' s © 5 x SCALE IN MILES FOR LOCALITY MAP | Hervey NANGAR SUB -GROUP LEGEND HERVEY GROUP COOKAMIDGERA SUB - GROUP 6. Burril Frm. 8. Eurow Fm 8. Undifferentiated 14. Koorawatha Fm, Syncline 3, Mandagery S.S. 4, Pipe Fm. 5 Caloma SS 7 Bumberry Fm. BEARGAMIL SUB -GROUP 1 Clogger S.S 2. Kadina Fm 10 Peaks S.S 11. Mogongong Congl Member 12 Hunter Siltstone 13. Bendick Fm. KOORAWATHA Koorawatha Syncline ATIONOD ‘a Lf ‘MW’S'N IVULNAD NI dNOWD ATANAH AO AHdVNOILVALS 44 J. R. CONOLLY z 4 (2) [00] {o) [a) Zz (o} O 45 STRATIGRAPHY OF HERVEY GROUP IN CENTRAL N.S.W. VISIN34N9 Le SagyYos Sl ¢g ‘SI dow A}1)090) Jo} SayiW ul a}0S ONOIWAM LS3M 6 OL g 0 S 0002 =, 93)09S uWn}09 ‘SS 2309 udbog ¢ dnojg-qns jiwobs08g "W4 S4jO4] OP ayoys ueuy6o)9 qr ‘S'S UIPPOM- F — ‘w4 unoqopuon | 9U0}S}IIS B aUOPSpUDS = ====| '§ § DUCCg 2 — dnoug-qng sobuon auoyspunos Ayqqad9 oe. 0 W4 asaparjag~é € auo}spuns oe Spaq pas pajyOIyUasajjipUug -g dnoig-qns osabpiwoy005 ; a OPS eee te, Miers) dnoig AasayH ON39931 ‘wes6eip Ay1je90) ay} UO UMOYS ae SUWUN}OD paunseaw jo suolysod ay) ‘weubeip siy} jo uoljsod usaysaM Y}NOS ay} ul doudyno you seop dnoig AaasayH aul ‘GN | M'S'N ‘V3uevV NITOSOGNOD -3S9NVY NIGGSM JHL NI dNOY¥9 ASAYSH FHL 40 WVYSVIG NOILV1SYYOS A GNV SNWN109 JIHdVYSILVYLS ——— ee = te \ / ' —— “1 sR May, e Is ) SYNCLINE / yr i s CONDOBOLIN STRATIGRAPHIC COLUMNS AND CORRELATION DIAGRAM OF THE HERVEY GROUP IN THE WEDDIN RANGE- CONDOBOLIN AREA, N.S.W. NB. The Hervey Group does not outcrop in the south western portion of this diagram. The positions of measured columns are shown on the locality diagram LEGEND Hervey Group siltstone, shale Cookamidgera Sub-Group 6 Undifferentiated red beds [5S] sandstone 3 2 Belvedere Fm pebbly sandstone Nongor Sub-Group \ 2 Boon $$ sondstone & siltstone \ 1. Condobolin Fm 0 y) uv 4 - Weddin S.S 4b- Cloghnan Shale 40- Trotts Fm. Beorgomil Sub-Group 5. Bogan Gote SS N Column scale > 2000 . 5 t) 5 10 15 ———— es WEST WYALONG Sole in miles for locality mop Fic. 5 FORBES a TF ATIONOD “uf ‘WSN TVMINGO NI dNOWD ATAMAH AO AHdVADILVALS cP 46 J. R. CONOLLY this locality two to three hundred feet of basal red conglomerates, red arkoses and lithic sand- stones rest with a marked angular unconformity on acid volcanics and tuffs of probable Lower Devonian age. The basal red beds and arkoses of this Sub- Group make one of the most distinctive features of the Hervey Group. Elsewhere to the east in both the Catombal Group and the Lambie Group, the basal beds are normally of marine origin with numerous fossiliferous bands containing brachio- ods. : To the south-west of the Hervey Group, the Cocoparra Group is marked by the presence of basal red measures, but they are characteristically conglomeratic, hence can be distinguished from the finer red beds of the Beargamil Sub-Group. To the west the Mulga Downs Group 1s generally similar to the Cocoparra Group and overlies the marine beds of the Ampitheatre Group (Rayner, 1962). THE NANGAR SUB-GROUP The type section of the Nangar Sub-Group was measured in the vicinity of the Nangar Trig. on the axis of the Nangar Anticline to the west of Manildra (Fig. 8). This Sub-Group generally comprises more than four fifths of the total thickness of the Hervey Group and consequently is the unit that is the most typical of Hervey Group sedimentation. It always begins with a massive orthoquartzite sandstone formation which lies above the upper red beds of the Beargamil Sub-Group. Following this, there is a rhythmic sequence of red and white formations. The sedimentation appears to be cyclic with the following characteristic cycler: Top Red shales and siltstones Red siltstones with red sandstones Red siltstones with red and_ white sandstones BASE White sandstones The thickness of such a cycle may be 100 feet or over a thousand feet. Formations within the Sub-Group may have several such cycles of sedimentation or may correspond to one major cycle: THE COOKAMIDGERA SUB-GROUP The type section was measured immediately east of the village of Cookamidgera in the centre of the Parkes Syncline, fifteen miles to the east of Parkes (Fig. 8). The horizons above the highest massive white sandstone in the Nangar Sub-Group consist of a thick sequence of red beds which have been called the Cookamidgera Sub-Group. Because of their fine-grained nature, they make poor outcrops and because of their position in the sequence, they frequently fail to outcrop. The upper red-bed sediments of the Upper Devonian have also been recognised in the Coco- parra, Catombal and Lambie Groups (Conolly, 1964). Upper red beds preserved in the centre of open synclines may only correspond to the red-measure phase within a typical Nangar Sub- Group cycle. However, when lithological cor- relation can be made on a local scale, red-measure rhythms of this type can be given Formation or Sub-Group status. DETAILED STRATIGRAPHY OF THE HERVEY GROUP Since the Hervey Group outcrops in isolated synclinal areas and correlation becomes difficult when erosional gaps separate different sequences, each area with its own local rock units will be described separately. In this way, the Hervey Group can be sub- divided into eight different areas of outcrop that correspond to natural structural features separated from one another by older Palaeozoic rocks or alluvium. Sometimes correlation can be made between areas but only a few formations persist over large distances. The stratigraphy of the Hervey Group in the eight areas is shown on Table 1, and the correlation diagrams (Figs. 4 and 5) show the areal relationships of the formations. There are seven geological maps showing the outcrop of the Hervey Group (Figs. 6, 8, 11, 13, 15, 17, 19), covering the areas shown on Fig. 3. The stratigraphy of the areas listed on Table 1 will be described in the following order : . Hervey Syncline (Fig. 6) Manildra-Gooloogong district (Fig. 8) . Gooloogong-Grenfell district (Fig. 11) . Koorawatha Syncline (Fig. 13) . Tullamore-Weddin Range district (Figs. 15, 17) 6. Murda Syncline (Fig. 19) The Weddin Range, Tullamore, Trundle- Bogan Gate districts listed on Table 1 are more conveniently described under the heading ‘“ Tullamore-Weddin Range district ”’. CUR Wb re The Hervey Syncline The Hervey Syncline is a long narrow synclinal structure elongated in a north-south direction, occurring several miles to the east of Peak Hill (Fig. 6). Detailed stratigraphy and structure are shown on the geological map of the Hervey Syncline (Fig. 6). STRATIGRAPHY OF HERVEY GROUP IN CENTRAL N.S.W. AG The geological map has been prepared from air photos and ground traverses on a planimetric base at a scale of 1:45,000. The Hervey Syncline forms a basin-shaped range with the inner depression of the basin coinciding with the synclinal axis. The outer sides are made up of rugged cliffs of sandstone which rise to a height of 1,800 feet above the flat alluvial plain to the west of Peak Hill. The highest point is the Trig-station at Caloma in the northern end of the range which is over 2,600 feet above sea level (Plate 1). The Hervey Syncline is essentially two large synclines belonging to the one synclinal structure which are faulted against one another by a steeply dipping normal fault with a downthrow side to the south east. Near Kadina Creek this fault has its maximum displacement, where older Palaeozoic formations rest against upper Hervey Group formations. Faulting also occurs on the north-western nose where several small cross faults allow for the accommodation of thick basal formations that dip more steeply under the upper formations (Fig. 6). The stratigraphy of the Hervey Group in the Hervey Syncline will be described by discussing each formation in the following order : BaAsE 1. Clagger Sandstone \ Beargamil Sub- 2. Kadina Formation Jf Group 3. Mandagery Sandstone 4. Pipe Formation Lcoeee Sub- 5. Caloma Sandstone J Group: Top 6. Burrill Formation Cookamidgera Sub-Group THE CLAGGER SANDSTONE The Clagger Sandstone is the basal formation of the Hervey Group in the Hervey Syncline. It can be defined as a sequence of basal sediments which consist of red sandstones and pebbly sandstones and a smaller percentage of red shales and siltstones. When the top of the formation is reached, finer red siltstones become the dominant sediment, the last thick (five to ten feet) red sandstone member being defined as the top horizon conformably underlying the fine red siltstones and shales of the Kadina Formation. Basal red shales and thin pebbly sandstones of the Clagger Sandstone unconformably overlie acid volcanics of probable Lower Devonian age in the northern section of the Hervey Syncline. The Clagger Sandstone thins considerably to the south and lenses out completely several miles to the south of Gingham Gap. The beds of the Clagger Sandstone are poorly preserved, but they form high strike ridges around the northern nose of the Hervey syncline near Clagger Creek where the type section was measured, as follows : Top Interbedded red sandstones, white sand- stones and red siltstones ; sone 200" Red sandstones more abundant than red siltstones with which they are inter- bedded ws Sn a vs 4407 Fine grained red conglomerate and coarse sandstone - ar 30’ BasE Red _ siltstones with minor sandstone and pebbly sandstone lenses .. 180’ TOTAL 850’ The most characteristic feature of the sedi- ments of the Clagger Sandstone is their red colour and poorly sorted nature. Sedimentary structures include current bedding which occurs in bands two inches to three feet thick, ripple marks of both wave and current types, and mud- cracks. Bedding tends to be lenticular and individual members cannot be traced for great distances. No fossils have been found or recorded from the Clagger Sandstone. This may be merely a function of poor conditions of preservation prevailing during’ deposition, particularly in an oxidising environment where carbonaceous remains are quite often destroyed. THE KADINA FORMATION The Kadina Formation overlies the Clagger Sandstone to the north of Gingham Gap but when the Clagger Sandstone lenses out to the south, it forms the basal formation of the Hervey Group (Fig. 6). It is defined as a thick sequence of fine-grained red sediments which are mostly red_ siltstones with minor shales and very few sandstone members which are also red in colour. The type section occurs in the vicinity of the Kadina Trig. station, distance four miles north of the southern tip of the Hervey Syncline, where the following sequence was measured : Top Red siltstones with minor fine-grained red sandstones ay 450° Red siltstones ; ee sg a 100" BasE Erosional gap, with traces of red silt- stone .. 2? 500’ TotaL THICKNESS approx. 1,050’ The Kadina Formation has a _ consistent thickness throughout most of the Hervey Syn- cline. In the north a thickness of 1,110 feet was measured along Clagger Creek. The Kadina Formation may be considerably thicker in the northern nose of the Hervey Syncline, two miles south of Gundong Creek; however, there is a lot of minor folding and faulting in this region making it impossible to calculate the thickness accurately. 48 J. R. CONOLLY Once again fossils have not been recorded or found in the Kadina Formation. The top of the Kadina Formation coincides with the base of the first massive white sandstone member of the Mandagery Sandstone which conformably over- lies it. Sedimentary structures include ripple marks, small scale current bedding, “ worm tracks ’’ and mudcracks. THE MANDAGERY SANDSTONE Mr. D. B. Walker (personal communication) first used the name Mandagery Sandstone for the Upper Devonian sediments that outcrop in the vicinity of Mandagery Station east of Parkes (Fig. 8). Although Walker’s facts were recorded on an unpublished geological map the term “Mandagery Sandstone’”’ has been frequently used by geologists when reference is made to the Upper Devonian sandstones that outcrop in the ranges to the west of Manildra. Since one of the most striking features of the Upper Devonian sediments of this region are cliff-forming sandstones it seems appropriate to place these sandstones into a formation called the SURATIGRAPHY OF HERVEY GROUP IN CENTRAL N.S.W. 49 Mandagery Sandstone which has a type section in the Mandagery district. This type section will be described in detail in the next section which discusses the geology of the Manildra- Gooloogong region. In the Hervey Syncline the Mandagery Sand- stone conformably overlies the Kadina Forma- tion and consists of fine-grained to coarse-grained white sandstones which are interbedded with red and green shales and siltstones. Red sandstones do occur but are not abundant. A section measured in the Gingham Gap area along the " [Dtb~] iv Dt Y] = “ w 2 ae Ww e De ne ae ; Bes c= Ww - Ww Es {U E OG 2PEw oc | WL iw 4) w iS 2 2 5 a fe) i ai Sy pps S52 2 € bed %*B 55 S Gwen sepia ie =o 5 02529 ue oa > - sg — = ie gees Oe ad — @ o 9 > sz vo a a On co S05 a2 ar me B/4 a > cee ag = Sane a > 2 > © > > > road to Baldry from Peak Hill on the eastern side of the Hervey Syncline has the following sequence : Top White sandstones with fine-grained silt- stone ae so 150’ White massive sandstone ae .. 100’ BasE_ Interbedded white sandstones and shales with some red sandstone 200’ TotTaL THICKNESS 450’ Near the Kadina Trig. station the Mandagery Sandstone consists of 200 feet of interbedded Greywackes, f.Og”] Pov] a) v ~ rm ) o = 5 ce ro) coe 2 S ce ve ° £ 2 0 = {= = S~ = rT) o x [00 wee Fete} ne ch ra) a vu ne A > a na Voo” fo 2 a = = SR wo on” =) 0) > ¢ = ell 3° o 2) a Ae by v a mas [} vo = u = = = 2) = tes a x g 2 re > 2 5 2 a. > a . = w 06 a - Oo = = Vs cs) a s = : 35 nw wo ° c ors ec YY x x c ) 2 4 Cs SS 3 1 Se ~ Oo ~ cn Cc — im aw =) 4 = sy oO = 9 a kt oS =O aoe ow: > CT) 4 c 0 UD co oO aA Dn na eas ee ee F500 8oOp se So o-9 = o>e ao] CFO SSD Ce 4+ v7o = aeo0 fe 82 oO fa) = OF Oe tein oO = ‘ GEOLOGICAL MAP SHOWING THE HERVEY GROUP IN THE HERVEY SYNCLINE 9 “ola LEGEND ~Tertiary- [[Atuvium To ie exr Recent [Boulder drift ra) uy DID “Upper [Cookamidsera [Burritt Fm Devonian= |Sub Group = |_ ¥ aL Carboni- [Cotoms ss ferous Nongor Pipe Fm 5; Hervey Sub Group LMandogery SS 5} Group Beorgomil Kadina Fm. SubGroup | Clagger 5S [Duce] qLower Devonian 2 Lower Devonian- 2 Ordovician Budgebegombil Tutt” Unditterentiated or] Lahyolites, Dacites Undifferentiated Slotes, Greywockes, O9¥] etc Fave] Mid Devonian. [reovat Gronite Gaologicol boundary Geological boundary position opproximate — —~ — Foult Foult position approximate Synclinol axis Anticlinol axis Dip ond strike (trom field observations) M2 Dip and strike (oir photo interpretation ) SCALE IN MILES GEOLOGICAL MAP SHOWING THE HERVEY GROUP IN THE HERVEY SYNCLINE BS Pee Seine: 5 BSS ea Sees BO co me eo, Fas aoe See eae “8 Syt z REEE ads » pS ata = 5 «CUB BU 2. Bay eles) ed ELI) SPS ate BBpe 326 i=] Bas 2,858 288'5 BE GgahEes ee OnF GEe eet a e wo WwW Boe SC®aPZ me Bio ie Chae Ais! Beuz ieee oa - BS Py Ss BRasoa &25 885285 Zz Si io YF, S38 4 Pe) SB, Rea a3 7 (op) Soo ar cs goS. 8 ae Bee ous ae BARB 8 7 $2 Res rtrtea =) 15 ~BaoSe ge Or yee Wy ie i v3 os An Ce 6 ay Sug She as Saas aea5 a BoTtoanan ° Ade :eoas Dac sae *9as.c PauUwMn sees ems} Be 5S Bp 2 Be Coss 8 ob Sok s Fae oS Bo Sy BeUo Simms of By 50 oR se Bio 22 6 SeEQ RR CSS. FERC eb a PRESB eee S 67 th oo a oa one ao pu Bee, SR SFR mo eae 2 SeR on Sa 5) Gage Usha ese 5 feO, S8n 2A os ors A pae “of ee Pund ga om ye E Eten SSoh segks mor S35 fies 532 Bae See ae So nS eo ona 2 puck Blas gee ey (3] agdg S82 23 S8 zie Eee feos Si eee Ssh FREIRES i= = ~s 1424 a ET BEEE Ss SELLE 28g Sp ° 7 Sheba R288 ASF 8 a2 oR BAB Bas Sreesas Ssemadaeaeey ScHESSR RARE ERSZHS 528.29 acre G < O02 Sp p STP S28 8 Sos Spe,aecsso age otbeaSeun beards S aE Pos os o8 mse8ase nak? BTHpg ee Sanz Boghaee S885 Bg oeB & oF GE. ofrebeak Retin” lee OR RRSfe ere ga eFou 6) Slal3 Sons EET 2 ba? AB 5a Ato oo p & 2 gS RAS ae Fee 6 7 O t eee ae gag BrETePS SaRs Big Bee a Bags ROSES! Eaa3a essa) iti) (uselerse FonoonsaA sooo eB haa? § teil! t=) Ww w ral 5 {43} 2 > oF FS aus ae oS (gis np Boe Sia! St S| a Pe Sot 2epak ct oD Zebee .. Bog ae Bee 5° oe ial weg? 8 fecfou ap 3 gee 2 od lee | es az np - gee s Go eh 4 fag & as we EF gee: 2 Sig pR § BRB S 2 = 7 aoe & fos o4 8 aas [Ep iar! REE EES yep as i ae. A oe = 3 me SH to e oe tat} & w Fs od 2 B ° Lal rem! 5 a8 eo a Fy = oe wo. i) ea Bf aE i ee. is) o g oF Eo ts 2% Be sl|8 se #8 ad e/= 88 oa 8F XTIONOO “Uf MLVALS © SN TVYINAD NI dNOWD ATANAH AO AHAVA 6F 50 J. R. CONOLLY BURRIL FM ?L.CARBONIFEROUS | CALOMA SS. - U. DEVONIAN PIPE FM. ACID VOLCANKS (L. DEVONIAN ) UNDIFFERENTIATED AAAS SEDS. (SIL- ORD.) A2 MANDAGERY S.S. KADINA FM. CLAGGER SS. Lay H a Scale in miles SECTIONS ACROSS THE HERVEY SYNCLINE BiG: white sandstones and white sediments overlain by 150 feet of massive sandstone that forms a prominent ridge line, that strikes northward towards Gingham Gap. The Mandagery Sandstone marks the beginning of the Nangar Sub-Group which is a rhythmic succession of white and red sediments. The rhythmic nature of the sequences within the Nangar Sub-Group makes many of the forma- tions within it hard to define. For instance, in the northern part of the Hervey Syncline the Mandagery Sandstone has many more beds of fine-grained sediments normally red in colour, interbedded among the more massive pale- coloured or white sandstones. The thickness in the Clagger Creek section (Flg. 6) is 1,720 feet, most of which is sandstone, but the sequence consists of at least twelve cycles of white sandstone separated by finer-grained green silt- stones and shales. The top of the Mandagery Sandstone is the last white sandstone member which conformably . Formation. od d underlies several hundred feet of fine-grained sandstones, shales and siltstones of the Pipe Impressions of fish plates and lepidodendrid plants have been found in the Mandagery Sandstone in the Clagger Creek section, but this formation is not as rich in fossils as the Caloma Sandstone some one thousand feet stratigraphically above it. Sedimentary structures include current bedding, ripple marks and occasionally small flow and load casts are preserved on the base of sandstone bands overlying finer sediments. THE PIPE FORMATION The Pipe Formation consists of fine-grained sediments that make poor outcrops and occurs conformably between two formations that contain a higher percentage of sandstone, the Mandagery Sandstone and the Caloma Sand- stone. The Pipe Formation can be easily traced on aerial photographs because it outcrops in valleys between the sandstone ridges of the Caloma and Mandagery Sandstone. STRATIGRAPHY OF HERVEY GROUP IN CENTRAL N.S.W. The formation consists of very fine-grained white sandstones with red and white siltstones and red and green or buff shales. The type section was measured in the vicinity of the Caloma Trig. station in the northern end of the Hervey Syncline about one mile to the west of the headwaters of Pipe Clay Creek which derives its name from the clays and silts of the Pipe Formation (Fig. 6). In this region the following section was measured : Top Fine-grained white sandstones and silt- stones with green shales : 200" Red and white siltstones with some fine- grained white sandstone .. 9350’ BasE Mainly very fine-grained sediment, red and white siltstones and some fine to medium-grained white sandstones towards the base ais .. 320’ ToTaL THICKNESS 820’ In the southern part of the Hervey Syncline a section has been measured where Burrill Creek crosses the western faulted limb of the Hervey Syncline. Here, there is a fairly large thickness of fine and medium-grained sandstone at the base of the formation making a subdued ridge line and the beds are very steeply dipping and locally overturned. Close to the Kadina Trig. station the Pipe Formation forms a prominent valley and is approximately 750’ thick. Most of the sediment consists of fine-grained red and white sandstones and coarse-grained red siltstones. Sedimentary structures include ripple marks and small-scale cross bedding. THE CALOMA SANDSTONE The Caloma Sandstone conformably overlies the Pipe Formation and is a massive sandstone formation consisting of medium to fine-grained white sandstones with many thin pebbly or conglomerate layers. It forms large cliffs capping the Hervey Syncline and making a very prominent ridge line throughout the Hervey Syncline (Plate 1). The type section was measured in the vicinity of the Caloma Trig. station in the northern end of the Hervey Range where the Caloma Sandstone has a thickness of at least 750’. In this locality the top of the formation is missing due to erosion, but the | i preserved thickness of the formation increases towards Gingham Gap. South of Gingham Gap, the Caloma Sandstone is conformably overlain by a sequence of red beds grouped into the Burrill Formation. _ Kadina Trig. station in the southern part of the In a section measured near d1 Hervey Syncline the Caloma Sandstone consists of 1,720 feet of white sandstones with several fish-plate horizons which occur at interavls throughout the succession. Hills (1932) has described fish plates that occur in the Caloma Sandstone in the Gingham Gap area. He described Phyllolepis sp., Remingolepis sp., Striacanthus sp., Bothniolepis sp., Antiarcht gen indet., Holoptychius sp., and Crossopterygii gen indet., and later in 1935 Hills described plates related to the genus Dipterus. Hills ascribes to this fauna an Upper Devonian age, comparable with that of similar faunas in Europe. The writer has also found many poorly preserved fish plates in the type area near Caloma Trig. and these are frequently associated with Lefidodendron australe. The fish plates generally occur in pebbly bands in medium-grained white sandstones. Quite often only one or two fish plate impressions will be found over a very large area and they are frequently poorly preserved. Current bedding is the dominant sedimentary structure in the Caloma Sandstone and units from two to three feet thick are quite abundant. THE BURRILL FORMATION The Burtill Formation is a red-bed sequence that conformably overlies the massive white sandstones of the Caloma Sandstone. It is not preserved to the north of Gingham Gap but in the southern part of the Hervey’s Range outcrops as a synclinal structure about four miles long and one mile across at its maximum width (Fig. 6). The beds of the Burrill Formation consist mainly of medium to coarse-grained red siltstones, but there are also many red sandstone members, particularly towards the base. The type section was measured across the western limb of the syncline in the region of the headwaters of Burrill Creek about one mile to the west of the Kadina Trig. station. Here, there was more than 1,000 feet of fine-grained red beds with 250 feet of these beds near the base consisting of many medium to fine-grained sandstone members. The formation is probably a lot thicker but erosion has removed the softer red beds leaving a valley which is the only land in the Hervey Syncline that has been cleared for cultivation. Poorly preserved fish-plates occur in fine-grained red sandstones near the base of the formation. They closely resemble some of the types associated with the Bothriolepis fauna in the Caloma Sandstone. 52 The Manildra-Gooloogong Region The Hervey Group in the Manildra-Gooloogong district outcrops from two miles west of Manildra westwards for twenty miles towards Parkes and southwards for thirty-two miles to Gooloogong on the Lachlan River. Detailed stratigraphy and structure are shown on the geological map (Fig. 8) and the section diagram (Fig. 9). The geological map has been prepared Geological boundary approx. Fault Dip and strike (air photo) Dip and strike (field) Overturned dip and strike Horizontal bedding ~ S a) uv c 2 °o 2 a cs) a ° ° a o Synclinal axis Anticlinal axis Du Co etal Fault position approximate DuB: baa Daas (eat ] [aa] i zs aD Ou | 2 | : 2 He £ 8 o -| aN x cPy 2 eo 2 Uv + = wv 3 ame MO Resang) Gee Ue ad we ra ae = é aL Cees Few = > Y c ca Ee pl ee io Ud) ig wn a ws 2 ay oo” 97e S$ o> un Su soa > 32S 2 a oo 5 2 @. (O. £€F OM ow eon w ro) Zz a z cee e A Oe] << 5 zw z 3G z Ww = iS) > oO Zoe ze 3 w Ow -> a°Q « ax US tii! s 2 ro) wo r M2 so a, ed . Ww ze CS &B Sia Zz. = f4 e¢f rf Yue ee ——— Ww OF Say Ou x z eo ao w a 2 =| = Ww Ww Bier es = fo) = z= ae De Fe DE ay wn = v v v v v Vood, v~W~\_SILURIAN QNoUr LV ae ae Ende Ke a Zz 2 © WwW a 1S) Zz jo) oO jo) jo) ) oO O © ' < a oO = z WwW > ao ee x lu 35 = <2) = = 2) x ep) oe < >» a < O je) oO a 12) lu 1o) | Si Ea \s = z £5) (ep Se Ore eee Rolin WwW 20 aon ae ooSe 325 > + @2 & © ME LS aata) Ei) eS: = 3 BE S ec Prclemiers ima: = = vo — rr 25.8 22 ee eee voease = S$ ° - o a Li 4 3 ag Din ve | oe oO 4 = 2 bd > oO Su => 2 Eo = BL os a 5 = (Say Sos edi Se 0 2 (=) o,. a eo 3 ae (Ss) Zz own Ww < z = z < | re) oO = fo) ma = > Ww > ©) lw > 2 w ray 9 ° ©. one iS dete o 6 o a ro) = oe ros wu w a oe et eS eer ene LW Ww ow (e) [=) 5 oa , ro) ° (&) lu ray wa xr SS = LS) > - Oo ~ = a SPRAPIGRAPHY OF HERVEY GROUP IN CENTRAL N-S.W. deposition by turbidity currents and are probably related to similar sediments now outcropping at Mandagery and south of Peak Hill. Overlying this group with a probable unconformity is a thick sequence of acid and intermediate volcanics and associated tuffaceous sediments and shales. 59 These are correlated with similar volcanics from the Cargo-Toogong area (Fig. 8) on lithological grounds and are of possible late Silurian to early Devonian age. The Hervey Group unconformably overlies these volcanics over a large area. They i) eo = c » ° a) a) Fic. 11 b8 are preserved as impressions in closely-fractured red siltstones alongside with numerous worm burrows. Mudcracks, worm tracks and burrows, ripple marks and small-scale current bedding are all common sedimentary structures. The Gooloogong-Grenfell Region The Hervey Group in the Gooloogong-Grenfell region extends southwards from the Lachlan River near Gooloogong about twenty to twenty- five miles towards the main western highway from Cowra to Grenfell (Fig. 11). The Upper Devonian sediments in this area outcrop in an east-west belt of anticlines and synclines which is an average of twenty miles wide. It is one of the largest single areas of outcrop of Upper Devonian sediments in New South Wales covering an area of approximately four hundred square miles. Once again, the Upper Devonian rocks form tugged ranges with strike ridges rising 1,500 to 2,000 feet above the alluvial plain of the Lachlan River. Detailed stratigraphy and structure are shown on the geological map (Fig. 11) and the section diagram (Fig. 12). The sediments of the Hervey Group outcrop in four main synclines and three anticlines. From the west these structures include the Red Cliff Syncline, Gooloogong Anticline, Sugarloaf Syncline, Kangarooby Anticline, Conimbla Syn- cline, Broula Anticline and the northern exten- sion of the Koorawatha Syncline. Between Manildra and Grenfell (Fig. 4) the Hervey Group outcrops in a folded synclinal depression which pitches to the south to the north of Gooloogong, and to the north to the south of Gooloogong forming a deep basin of Upper Devonian sediments in the Gooloogong region. Stevens (1950) mapped the far eastern boundary of the Upper Devonian sediments from west of Canowindra southwards along the Lachlan River towards Cowra. He noted that these sediments all dipped to the west and consisted of interbedded grits, quartzites and shales. Apart from this, no detailed investiga- tion has been made of the Upper Devonian sediments in the Gooloogong-Grenfell area. David and Browne (1950, p. 157) mention a belt of quartz-rich eaiments ene through Grenfell towards Parkes and Peak Hill of Possible Ordovician age. This group of sedi- ments is shown as undifferentiated sediments of Eewe Ordovician and Silurian age on the pea logical map (Fig. 11). They are quite highly ‘olded and schistose in many places in the area J. R. CONOLLY to the north and south of Grenfell and intruded by the Eugowra . d ate Grantee Sowra granite to the west y These sediments are characterised by sedi mentary structures such as flow casts sli and graded bedding suggesting fatty a = GRENFELL REGION tion oppreximote Grolegical beundery peniticn approximate Geological baundary Antictinal xis Fault Foult IN THE GOOLOOGONG - fa a 2 =) x a BgEw o s“ a > £ = w 3542 > rey ti a 4.5.8 Si w e os 3 Ww 2s = ae: - 2 8 5 4) es 2 2.9 feng = § 2 33 a Woe BS 3 B: 3a uw a : = ze - as S23 q sé 34 i 3 8 Piece 5, 33° (7) ae Bo: o Ww ere = pe z S Ol oan we 5 Fo] Wee f ¥e go § w JG 8 6 jromemems °o Sos.) Sees 2a ae STRATIGRAPHY OF HERVEY GROUP IN CENTRAL NS.W. by turbidity currents and are probably similar sediments now outcropping at nd south of Peak Hill. Overlying th a probable unconformity is a f acid and intermediate volcanics d tuffaceous sediments and shales. 59 These are correlated with similar volcanics from the Cargo-Toogong area (Fig. 8) on lithological grounds and are of possible late Silurian to early Devonian age. The Hervey Group unconformably overlies these volcanics over a large area. They Scale in miles Fic, 11 60 J. R. CONOLLY normally consist of quartz, felspar porphyries with a devitrified ground mass. Most are rhyolites or dacites but some intermediate and basaltic lavas occur in the axial region of the Gooloogong Anticline. The Eugowra Granite outcrops northward across the Lachlan River to Eugowra. Since it intrudes the Ordovician and Silurian sediments and the volcanics mentioned above and is unconformably overlain by Upper Devonian sediments, a Middle Devonian age is postulated for this batholith (Plate III, 1). The stratigraphy of the Hervey Group in the Gooloogong-Grenfell area is shown on Fig. 4. Six stratigraphic columns (columns K to P inclusive on Fig. 4) measured from ground traverses and air photos show variation in thickness for the formations of the Hervey Group. The Peaks Sandstone, Mogongong Con- glomerate Member and the Hunter Siltstone are all red bed formations belonging to the basal Beargamil Sub-Group which is_ considerably thicker in this area than in others. The rhythmic beds of the Nangar Sub-Group are represented by the Mandagery Sandstone and the Bumberry Formation which continue south- wards from the Manildra district. The upper red beds of the Cookamidgera Sub-Group have not been subdivided in this area, although they do outcrop in two areas just to the south of Gooloogong (Fig. 11). Although there is a far greater thickness of the Beargamil Sub-Group preserved with a thick basal conglomerate member developed in one area (the Mogongong Conglomerate Member) the stratigraphy of the Hervey Group is very similar to that of the Manildra-Gooloogong area, and can be summarised as follows: . Cookamidgera Sub-Group . Bumberry Formation .. . Mandagery Sandstone fNangar Sub-Group . Hunter Siltstone . Peaks Sandstone rh WH Ot b Beargamil Sub-Group THE PEAKS SANDSTONE The Peaks Sandstone is the basal formation of the Beargamil Sub-Group in the Gooloogong- Grenfell region. It consists of red sandstones and grits interbedded with red siltstones and shales. There are numerous pebbly bands amongst the sandstones and the formation has a thick conglomerate member, the Mogongong Conglomerate Member, developed in the southern part of the Sugarloaf Syncline (Fig. 11). The Peaks Sandstone unconformably overlies acid and intermediate volcanics in the type area at Peaks Creek in the eastern limb of the southern nose of the Red Cliff Syncline where the following sequence was measured : Top White and red coarse and medium-grained sandstones and red siltstone Pe LDOF Red siltstone he . at ft 30” Red coarse-grained sandstones and red siltstone and red shale ‘ 190’ BASE Red siltstone and red shale a oh 50’ TotaL THICKNESS 420’ The top of the Peaks Sandstone is defined as the last coarse sandstone member (five to ten feet thick) underlying the thick sequence of red siltstones of the Hunter Siltstone. The sandstone beds of the Peaks Sandstone are normally five to ten feet thick and pebbly layers are abundant. Whiter sandstones appear more frequently towards the top of the formation whereas the basal sandstones are mainly red in colour. The Peaks Sandstone everywhere rests on probable Lower Devonian acid or intermediate volcanics and their associated sediments, except four miles south-west of Gooloogong where they rest on the Eugowra Granite (Plate III, 1). In this locality the Peaks Sandstone consists of 350 feet of red grits, conglomerates and red and white coarse-grained sandstones. The Peaks Sandstone has a maximum recorded thickness of 1,500 feet in the Gooloogong Anticline. From this locality it thins rapidly to the east where only one or two hundred feet of sediment form the basal beds. Thick current-bedded units occur in the massive red and white sandstones and measure- ments made in the western area of outcrop indicate a palaeocurrent from the west. The Mogongong Conglomerate Member is a massive conglomerate member developed at the base of the Peaks Sandstone near Mogongong (Fig. 11). In the type section just north of the Cowra-Grenfell highway and three miles north of Mogongong the following sequence occurs : Coarse pebbly sandstones, thin con- glomerate beds and red siltstone BasE Massive red conglomerate 200° 120’ TotTaAL THICKNESS 320’ The Mogongong Conglomerate Member thins out gradually five miles to the north and is thinning slowly to the south but does not outcrop further south than Bungalong Creek because of the plunge of the Upper Devonian rocks in this area. The Mogongong Conglomerate Member generally consists of a thick massive conglomerate member which is up to 150 feet thick with poor and indistinct bedding, overlain by interbedded conglomerates and sandstones which are well bedded. The pebbles vary in STRATIGRAPHY OF HERVEY GROUP IN CENTRAL N.S.W. 61 size from one-half an inch to three inches in in diameter and consist mainly of fine-grained orthoquartzitic sandstones and siltstones, chert, vein quartz and acid volcanics. Generally, the percentage of pebbles to sandy matrix is high and the characteristic basal conglomerate consists of 50 to 80 percent pebbles and the remainder of sandy matrix. However, the percentage of pebbles decreases with distance from the basal layers, and thin pebbly sand- stones are the dominant coarse lithology in the topmost beds. THE HUNTER SILTSTONE The Hunter Siltstone is a thick sequence of red siltstones and shales and a lesser proportion of fine-grained red sandstones conformably over- lying the Peaks Sandstone and underlying the Mandagery Sandstone. It forms prominent valleys between the strike ridges of the Mandagery and Peaks Sandstones. The type section was measured on the eastern limb of the Gooloogong Anticline along the Hunter Gully Creek where a thickness of one thousand feet of ted siltstone with occasional fine-grained red sandstone and shale members is calculated from width of outcrop and average dip. Un- fortunately, the fine-grained sediments of the Hunter Siltstone do not form continuous out- crops and hence it is impossible to find a completely preserved section. The Hunter Siltstone is a persistent formation and has estimated thicknesses that vary from 500 to 1,600 feet (Fig. 4). The maximum estimated thickness of 1,600 feet occurs on the eastern side of the region near the Lachlan River (column K, Fig. 4). Sedimentary struc- tures include worm tracks and trails, mud- cracks, ripple marks and small-scale current bedding in beds half an inch to one foot thick. THE MANDAGERY SANDSTONE The Mandagery Sandstone conformably over- ies the Hunter Siltstone of the Beargamil Sub-Group in a similar fashion to the way it overlies the fine-grained red sediments of the Kadina Formation in the Manildra-Gooloogong region. The formation can be traced along the strike along the eastern side of the Manildra region across the Lachlan River down the eastern side of the Grenfell-Gooloogong region. Once again, the Mandagery Sandstone is the first thick white sandstone formation overlying the red beds of the Beargamil Sub-Group. In the Grenfell-Gooloogong region the Man- _ dagery Sandstone is five hundred feet thick on the north-eastern margin and maintains a thickness between 500 and 1,000 feet thick southwards towards Cowra (Fig. 4). It mainly consists of fine-grained sandstones with many white siltstones and some red siltstones. Five miles west of Cowra, where the Grenfell-Cowra highway crosses the most eastern strike ridge of KOORAWATHA SYNCLINE ia Scale in miles KOORAWATHA | SYNCLINE VOLCANICS YOUNG GRANITE ? L. DEVONIAN M. DEVONIAN 1 BROULA ian ) BROULA ANTICUINE CONIMBLA SYNCLINE g : HUNTER SILTSTONE CONIMBLA SYNCLINE SUGARLOAF SYNCLINE SECTIONS ACROSS THE GOOLOOGONG GOOLOOGONG ANTICLINE GRoPp =F VV. COOKAMIDGERA SUB SUGARLOAF SYNCLINE MANDAGERY SS é Se a (oe uJ ae) Da =) a RED CLIFF SYNCLINE A ? L.CARBONIFEROUS - U. DEVONIAN HERVEY GROUP - GRENFELL REGION Fic. 12 62 Mandagery Sandstone, fish plates, referable to the genus Bothnolepis, are found together with Lepidodendrid and Cordaitid plant remains. The Mandagery Sandstone thickens to 1,200 feet in the Gooloogong Anticline where it forms prominent ridge lines and steep dip slopes with screes. Current bedding measurements in the Man- dagery Sandstone indicate a _ palaeocurrent direction from the north-west. Ripple marks and small scale current bedding are common in smaller beds of fine sand or coarse silt grain size. THE BUMBERRY FORMATION The Bumberry Formation continues southward from the Manildra district to the Gooloogong- ; oy POSTULATED AXIS OF THE KOORAWATHA SYNCL INE RK CONOELY: Grenfell area. Once again this formation con- sists of a thick rhythmic succession of red and white beds. A section measured on the eastern limb of the Kangarooby Anticline along the back road from Gooloogong to Cowra consists of 3,000 feet of interbedded white sandstones and white siltstones with red sandstones and siltstones. However, there appears to be a far greater thickness of white sandstones than in the equivalent Bumberry Formation of the Manildra- Gooloogong region. The Bumberry Formation is 3,200 feet thick to the north-east of the Kangarooby Anticline, but elsewhere erosion has removed most of its upper members (Fig. 4). White quartzite and sandstone ridges occur sporadically through a 1Cecnn --DuBa —| YY Sl % Fm. umberry andagery esp Nongor Sub-Group ? L. CARBONIF EROUS le i | STRATIGRAPHY OF HERVEY GROUP IN CENTRAL N.S.W. sequence which consists mainly of fine-grained sandstones and coarse siltstones. Ripple marks and current bedding are the most frequent sedi- mentary structures. Current bedding measure- ments show that palaeocurrents came from the north-west and north. Traces of fish plates and Lepidodendrid plant remains have been found in some medium to coarse-grained sandstones, but all were too poorly preserved for identification. THE COOKAMIDGERA SUB-GROUP The red beds of the Cookamidgera Sub-Group conformably overlie the Nangar Sub-Group and outcrop in only two localities, firstly within the northern extension of the Conimbla Syncline and oH Hee endick Fm. ed ond interme- diate lavas [Young granite eargamil Sub-Group Geological boundary position approximate Geological boundary Fault position approximate Anticlinal axis Synclinal axis {THE HERVEY GROUP 63 secondly on the flank of the Broula Anticline (Fig. 11). In these localities 500 to 600 feet of red siltstones and shales outcrop in valleys. Low-lying strike ridges of fine-grained red and white sandstone members are the only beds that make good outcrops. Most of the succession consists of fine red sediments but there are several thin lenticular members of white sand- stone. Sedimentary structures include ripple marks and small-scale current bedding. The Koorawatha Syncline The Hervey Group in the Koorawatha Syncline extends from west of Cowra southwards to the east of Young (Fig. 4). The sediments oct 61 BiG. 13 GEOLOGICAL MAP SHOWING THE HERVEY GROUP IN THE KOORAWATHA SYNCLINE “ail itn ail SE ln a SE A ly eS 62 J Mandagery Sandstone, fish plates, referable to the genus Bothriolepis, are found together with Lepidodendrid and Cordaitid plant remains. The Mandagery Sandstone thickens to 1,200 feet in the Gooloogong Anticline where it forms prominent ridge lines and steep dip slopes with screes. Current bedding measurements in the Man- dagery Sandstone indicate a palaeocurrent direction from the north-west. Ripple marks and small scale current bedding are common in smaller beds of fine sand or coarse silt grain size. Tue BumMBERRY FORMATION The Bumberry Formation continues southward from the Manildra district to the Gooloogong- . R. CONOLLY Grenfell area. Once again this formati sists of a thick rhythmic succesgi ON con. white beds. A section measured ae Hee 2 em limb of the Kangarooby Anticlin toad from Goclengodeite Cowra ae i feet of interbedded white sandstones al aa siltstones with red sandstones and allt However, there appears to be a far a thickness of white sandstones than ad equivalent Bumberry Formation of the Meda Gooloogong region. : The Bumberry Formation is 3,20 ick to the north-east of the Kangeeai ee but elsewhere erosion has removed most of ik upper members (Fig. 4). White quartzite ani sandstone ridges occur sporadically through « STRATIGRAPHY OF HERVEY which consists mainly of fine-grained es and coarse siltstones. Ripple marks and current bedding are the most frequent sedi- mentary structures. Current bedding measure- ments show that palaeocurrents came from the north-west and north. i ; Traces of fish plates and Lepidodendrid plant remains have been found in some medium to coarse-grained sandstones, but all were too poorly preserved for identification. cequence sandston' Tur COOKAMIDGERA SUB-GROUP The red beds of the Cookamidgera Sub-Group conformably overlie the Nangar Sub-Group and outcrop in only two localities, firstly within the northern extension of the Conimbla Syncline and GROUP IN CENTRAL N.S.W, 63 secondly on the flank of the Broula icli (Fig. 11). In these localities 500 to 600 fest ted siltstones and shales outcrop in valleys Low-lying strike ridges of fine-grained red ai white sandstone members are the only beds that make good outcrops. Most of the succession consists of fine red sediments but there are several thin lenticular members of white sand- stone. Sedimentary structures include ri and small-scale current bedding. er The Koorawatha Syncline The Hervey Group in the Koorawatha Syncline extends from west of Cowra southwards to the east of Young (Fig. 4). The sediments Fic. 13 we z = Oo z > wo < = ES = we ° ° x Ww = = z a 2 o a ° > a & Ww =x w x = ° 5 = wo < z 3) oO ° = Oo Ww oO 64 J. R. CONOLLY KOORAWATHA SYNCLINE ksi s CREEK eer TRIG HERVEY GROUP KOORAWATHA FM ? L. CARBONIFEROUS - U DEVONIAN BUMBERRY FM MANDAGERY SS 0 BENDICK FM SECTIONS A BLACK RANGE ? | DEVONIAN KOORAWAT HA CALABASH CREEK SYNCLINE | ? M. DEVONIAN VOLCANICS 1 Scale in miles OSS THE KOORAWATHA SYNCLINE Fie. 14 in this area outcrop in a large long synclinal structure which originates to the north in the Gooloogong-Grenfell area near the headwaters of Koorawatha Creek and pitches very gently southwards, the axis following Koorawatha Creek and passing through the town of Koora- watha (Fig. 13). The total length of the structure from northern to southern nose is 50 miles and it has an average width of 8 miles. The area shown on Fig. 13 and described in this section is the southernmost 36 miles of the Koorawatha Syncline measured along the strike. The Mandagery Sandstone mapped further north in the Manildra and the Gooloogong districts can be traced along the strike into the Koorawatha Syncline. It forms an excellent marker horizon, making a prominent ridge feature just above the basal red beds of the Beargamil Sub-Group. The topography is similar to other areas of Upper Devonian further north only the relief between the Hervey Group and older rocks is generally not nearly so great. The central portion of the Koorawatha Syncline is marked by very few good outcrops and mainly consists of poorly-exposed red beds. The geological map of the Koorawatha Syncline (Fig. 13) was prepared on an air photo base on a scale of 1: 45,000 from ground traverses and air photo interpretation. Strati- graphic columns from the Koorawatha Syncline are shown on Fig. 4 and geological sections on Fig. 14. The northern nose of the Koorawatha Syncline has already been discussed, in the previous section on the Gooloogong-Grenfell region. The southern and main portion of the syncline is a wide structure with minor folding and faulting along the limbs (Fig. 13, 14). Minor folds on the limb of the main structure occur three miles to the south-east of Koorawatha, four miles to the east of Bendick Murrell, five miles to the south-west of Murringo, and in the upper red beds in the synclinal axial region near Bendick Murrell. Many of these open structures are faulted, and to the south of Murringo, the eastern limb of the Koorawatha Syncline has been overturned and faulted against older acid and intermediate volcanics. In the vicinity of the Marina Trig. minor anti- clines and synclines occur on the south-western limb of the Koorawatha Syncline. Two of these minor structures are faulted with the eastern limb moving to the north. Faulting also brings the Young Granite against the Upper Devonian in this area with overturning of the western limb of the syncline near Wambanumba Trig. North of Portar’s Quarry, near Wambanumba Trig. on the western limb of the Koorawatha Syncline, there is a physiographically depressed area of Young Granite and alluvium and the lower beds of the Hervey Group do not outcrop. It is possible that many of these lower beds have been faulted against the Young Granite in this area. Similar relationships may exist STRATIGRAPHY OF HERVEY GROUP IN CENTRAL N.S.W. 65 further north near Koorawatha where faulting separates Hervey Group sediments from older lavas and granite. Only two rock groups outcrop unconformably or faulted against the Hervey Group sediments of the Koorawatha Syncline. They are the Young Granite and a thick sequence of acid and intermediate lavas. N. C. Stevens continued his mapping (Stevens, 1950, 1951) southwards, to the east of the Koorawatha Syncline, but this work has not been published and Stevens only prepared draft maps of the geology to the east of the Koorawatha Syncline. Since this time an unpublished geological map has been produced by Mr. D. Wynn of the New South Wales Geological Survey, showing the regional geology of the Young district. No other detailed geology has been carried out or published in this area. The granite, called the Young Granite, that underlies and is faulted against the Hervey Group is probably a southern extension of the Eugowra Granite and may be of much the same age. However, the large group of acid and intermediate volcanics that underlie the Hervey Group and which have been intruded by the Young Granite are essentially more basic than the volcanics of the Manildra-Grenfell area. Their age is tentatively ascribed to the Lower Devonian or Upper Silurian. STRATIGRAPHY The stratigraphy of the Hervey Group in the Koorawatha Syncline is illustrated in three columns (columns Q to S) on Fig. 14. The Beargamil Sub-Group is thin, represented only by the Bendick Formation. The Nangar Sub- Group is represented by the Mandagery Sand- stone and the Bumberry Formation which continue southward from the Gooloogong area. Overlying the Bumberry Formation is a thick succession of red measures which has been called the Koorawatha Formation and tenta- tively placed in the Cookamidgera Sub-Group. The Hervey Group reaches a maximum thickness of nearly 4,000 feet near Bendick Murrell, which is considerably less than the 9,000 feet preserved in the Manildra district. How- ever, it is thought that quite a large thickness may be missing due to erosion. THE BENDICK FORMATION The Bendick Formation is the basal formation of the Hervey Group in the Koorawatha Syncline and the only representative of the basal _ ted beds of the Beargamil Sub-Group. It mainly consists of red shales and siltstones, but fine- 19 grained red sandstone members and _ poorly- sorted conglomerates occur in some areas. The type section was taken three miles south of the Bendick Trig. on the eastern limb of the Koora- watha Syncline (Fig. 13). Here the basal red beds unconformably overlie the Young Granite and the following section was measured : Top Red fine-grained sandstone and red silt- stones with some white sandstone .. 60’ Red siltstone, red conglomerate and coarse-grained sandstone ae ie 50’ BasE_ Red siltstones and red shales .. 2% 70’ 180’ Overlying the upper red beds of this formation is the basal coarse-grained white sandstone and pebbly sandstone of the Mandagery Sandstone. The Bendick Formation is generally quite thin and thicknesses between 100 and 300 feet are common throughout the area. A thin bed of red conglomerate preserved to the north-east of Koorawatha contains many limestone fragments and is cemented by hema- tite. Red grits are common near the base of the formation but conglomerates similar to one described above are rare. Traces of poorly preserved fish plates were found in red sandstones that underlie the massive white sandstones of the Mandagery Sandstone. No other fossils have been found in the Bendick Formation. Sedimentary structures include ripple marks, current bedding, and worm burrows. ToTAL THICKNESS THE MANDAGERY SANDSTONE The Mandagery Sandstone has been mapped from the Gooloogong area southwards along the eastern limb of the Koorawatha Syncline. It forms the first white sandstone formation above the red beds of the Bendick Formation in the Koorawatha Syncline. The Mandagery Sandstone is 400 to 500 feet thick north of Koorawatha and_ thickens gradually southwards till it is 800 feet thick near Bendick Murrell (Fig. 4). It thickens still more to the south and is 1,600 feet thick (column Q, Fig. 4) in a section across the Black Range in the southern nose of the syncline. The basal beds of the Mandagery Sandstone in the Koora- watha Syncline are alwasy very coarse grained with the development of pebbly sandstones and quartz-pebble conglomerates. Measurements of current bedding in these coarse-grained sandstones indicate a _ palaeo- current direction from the north-east near Koorawatha and from the north and east further south towards Bendick Murrell. Near Marina Trig. palaeocurrent directions swing slowly from ion ai endl 66 J. R. CONOLLY : AG GEOLOGICAL MAP SHOWING THE HERVEY GROUP IN THE TRUNDLE - BOGAN GATE _ DISTRICT \ \ \ TRUNDLE TUL LAMORE SYNCLI NE ‘ EAST COOKEYS PLAINS v v STATE FOREST v v YARRABANDAI Sa 4 NK (AE7 LEGEND ee See TERTIARY - RECENT [Altuvium, gravels Geological boundary —_—— ? L.CARBONIFEROUS - Cookamidgera Sub - Group [Undifferentiated Geological boundary position approximate —_ — — . DEVO : ——— U.DE Me Nangar Sub - Group Weddin S S Synclinal axis ——_xi—. GROUP Cleghnany Shale Dip and strike (from field observation ) ee Troffs Fm. Beargamil Sub - Group [Bogan Gate SS. Dip and strike (air photo interpretation ) 7 MIDDLE DEVONIAN [ Ganantagi Granite Das*] ? LOWER DEVONIAN [Acid volcanics [Dy] L. DEVONIAN - SILURIAN [Shole. sandstone, limestone [5 =] 0 1 2 3 : 5 6 ? LOWER SILURIAN Conglomerate. grit, Scale in miles sandstone Fic: 1d STRATIGRAPHY OF HERVEY GROUP IN CENTRAL N.S.W. 67 north-east towards the north-west in the southern parts of the Koorawatha Syncline. The coarse sandstones and conglomerates at the base of the Mandagery Sandstone are normally 35 to 50 feet thick. Overlying these sediments there is a thick sequence of fine and medium-grained sandstones. South of the Marina Trig. along the western limb of the Koorawatha Syncline there are two ridges of coarse sandstone in the Mandagery Sandstone separated by a thick sequence of fine-grained white sandstones and white and red siltstones. Stems of Lefidodendron have been found in the Mandagery Sandstone at Portar’s Quarry near the main road to Young on the western limb of the Koorawatha Syncline. Poor traces of fish plates were also found along the strike ridge near Portar’s Quarry. THE BUMBERRY FORMATION The Bumberry Formation overlies the Man- dagery Sandstone and consists of interbedded white sandstones, red siltstones, and shales. A section measured where Bang Bang Creek cuts through the eastern limb of the Koorawatha Syncline just to the east of Koorawatha, showed the following sequence : Top White sandstones and red siltstone 120’ Red siltstone and shale .. de aaa 50’ White sandstones and red siltstone .. 260’ White sandstone .. ee ae ene 30’ BasE Red siltstones with some white sandstone members ae a ae 100’ ToTaL THICKNESS 560’ The formation essentially consists of cycles of white sandstone that grade into red siltstones and shales, typical of the Nangar Sub-Group. The Bumberry Formation thickens to the south Where it is approximately 1,400 feet thick (column Q, Fig. 4). Sedimentary structures include current bed- ding, ripple marks, and mudcracks. Current bedding measurements in several localities indicated a palaeocurrent direction from the north and north-east. The Bumberry Forma- tion is conformably overlain by the Koorawatha Formation. THE KOORAWATHA FORMATION The base of this formation is defined as the first thick (300 ft.) red siltstone or shale member after the highest massive white sandstone member of the Bumberry Formation. The formation consists almost entirely of red beds and hence it is believed to represent the Cooka- midgera Sub-Group in the Koorawatha Syncline. Generally outcrops are poor, but good exposures occur in the vicinity of Bendick Murrell where medium-grained red sandstones of the Koorawatha Formation are folded into a series of open synclines and anticlines (Fig. 13). It is hard to find exposures of the Koorawatha Formation that would contribute to the compila- tion of a complete section, since the red beds are easily eroded and make poor outcrops. How- ever, an estimate of the exposed thickness in the Koorawatha district is over 1,000 feet of red beds and this has been chosen as the type area. No fossils have been found in this formation, but sedimentary structures such as ripple marks and small-scale current bedding are abundant. The Tullamore-Weddin Range District The sediments of the Hervey Group outcrop in a large synclinal structure called the Tulla- more Syncline in the Tullamore-Bogan Gate district. South of Bogan Gate on the eastern limb of this syncline, strike ridges of Upper Devonian sandstone extend southwards and form the Jemalong and Corradgery Ranges. These ranges extend twelve miles south of the Lachlan River, beyond which there is no further outcrop except to the south-west where the Wheoga and Weddin Ranges outcrop (Fig. 3). The outcrop distribution and_ stratigraphic columns measured of the Hervey Group from this area are illustrated on Fig. 5. The total length of outcrop of the sediments of the Hervey Group from the northern end of the Tullamore district, south to the Weddin Range is 110 miles. The area is generally very flat and the strike ridges of the Hervey Group rarely rise more than five hundred feet above older Palaeozoic rocks and more recent alluvium. The Weddin and Wheoga Ranges have the greatest relief, rising to heights of 1,000 to 1,500 feet above the surrounding plain. Geological maps of the Bogan Gate-Trundle district (Fig. 15) and the Tullamore district (Fig. 17) were prepared from air photos and ground traverses. Separate maps of the Weddin and Wheoga Ranges were not prepared, for they are just simple strike ridges that dip to the south and west respectively. Fig. 5 illustrates the outcrop of the Hervey Group from the Weddin Range to the Tullamore district. The Tullamore Syncline is the dominant structure of the area and only the Wheoga and Weddin Ranges outcrop away from it. These two ranges are strike ridges striking in the same direction as the eastern limb of the Tullamore Syncline but offset about twelve miles 68 J. R. CONOLLY TULLAMORE SYNCLINE Vv a a fe } a | HERVEY GROUP COOKAMIDGERA SUB -GROUP | ? L.CARBONIFEROUS - U, DEVONIAN WEDDIN S.S CLOGHNAN SHALE ?L. DEVONIAN TROFFS FM BOGAN GATE SS L. DEVONIAN - SILURIAN TULLAMORE SYNCLINE GUNNINGBLAND CREEK WARDS LOOKOUT SHALES, SANDSTONES, | LIMESTONES VOLCANICS 1 2 3 Scale in miles SECTIONS ACROSS THE TULLAMORE SYNCLINE IN THE BOGAN GATE DISTRICT Fre. 16 to the east of the eastern limb of the Tullamore Syncline and probably represent the only out- cropping remnants of another synclinal structure. The Weddin Range represents the partly preserved northern side of a broad shallow basin which strikes east-west at its southern extremity, and north-south at its northern extremity. The range is 13 miles long, along the strike, and dip slopes of 5 to 20 degrees dip gradually to the south from high cliffs on the northern side, extending the outcrop of the range to an average distance of 5 miles in the direction of the dip. The Wheoga Range is a strike ridge that is an erosion remnant of the northern extension of the Weddin Range. It dips to the west at angles of 30 to 40 degrees. Geological maps (Figs. 15, 17) and section diagrams (Figs. 16, 18) show the structure of the Tullamore Syncline, which is an extremely large syncline with a total outcrop length of at least 80 miles, and an average width of 12 miles. Both limbs of the syncline pinch together near Bogan Gate where they are only one mile apart. North of Trundle, near the Troffs (Map 17), there is some minor folding on the western limb of the syncline producing a synclinal structure that pitches at a low angle to the north. REGIONAL GEOLOGY Detailed investigations of the geology of the Tullamore-Weddin Range district include those by Raggatt (1937) and Andrews (1910). Raggatt (1937) made a regional geological reconnaissance of the Condobolin-Trundle district dubdividing the Palaeozoic succession in the following way : Devonian Quartz sandstone 2,000’ Fine-grained sand- stone, shale, lime- stone a Sandstone and con- glomerate Claystone, sand- stone, limestones, rhyolites, andes- ites. Slates, phyllites, some fossiliferous limestone, rhyo- lite. 700’ 2,000’ Silurian Ootha Series Silurian Cobar Series Because of poor outcrops and _ insufficient fossil evidence it is difficult to find the relation- ships between individual units of the Silurian and Devonian sequence. Apart from the distinctive Upper Devonian sediments and granitic outcrops it is possible to subdivide the sequence into a Devonian-Silurian sequence of sedimentary rocks which have been openly folded and are characterised by shallow or moderate dips. These rocks are, characteristically, sandstones, siltstones, shales, limestones and marls. Marine fossils of both Silurian and Devonian age have been described (Raggatt, 1937) from these sediments. These sediments are frequently overlain by a sequence of acid and intermediate volcanics. On the geological maps (Figs. 15, 17) these two units, that is, the sedimentary sequence and SPRATIGRAPHY OF HERVEY: GROUP IN CENTRAL N-s.W. 69 GEOLOGICAL MAP SHOWING THE HERVEY GROUP IN THE TULLAMORE DISTRICT ane j : LEGEND TERTIARY -RECENT [Attuvium, gravels Geological boundary a ? L.CARBONIFEROUS - Cookamidgera Sub-Group [Undifterentiated Geological boundary position approximate —_— —— ee DevOrmaN Nangar Sub-Group Weddin SS. with pebbly [ Foult a HERVEY s.s. horizon petaesa9 ; GROUP ee Shale Fault position approximate — = Troffs Fm. Synclinal axis ——s 2M. DEVONIAN [Gobondery Granite Anticlinal axis ae ? L. DEVONIAN [Acid volcanics Dip and strike (from field observation) po 2M, DEVONIAN - SILURIAN [Shale. sandstone, limestone Dip and strike (air photo interpretation) — PRE - SILURIAN [States. phyllites, schists -o—~] Fig: 17 70 J. R. CONOLLY the volcanic sequence, have been differentiated. It is possible that part of the volcanic sequence is actually interbedded with the uppermost beds of the sedimentary sequence but more detailed mapping is required before this can be estab- lished. Both sequences probably belong to the ““ Qotha Series ”’ as described by Raggatt (1937). Underlying these rocks is a much older regionally metamorphosed sequence of quartz- mica schists, phyllites and slates, which is probably the equivalent of the Cobar Series as originally described by Raggatt (1937). Recent work in the Cobar district by Rayner (1962) has shown that a similar group of rocks outcrop in the Cobar district. Rayner has demonstrated that they are probably Ordovician in age and are separated from the overlying Devonian- Silurian sequence by an unconformity. The deposition during the Silurian and Lower and Middle Devonian in the Tullamore-Bogan Gate district was essentially a shallow-water marine type with a high percentage of well sorted quartz-rich sandstones and calcarenites. This is in direct contrast to the somewhat deeper water sedimentation that was presumed to have taken place to the east of Forbes and Peak Hill. The Silurian and early Devonian sequences in the Bogan Gate and Forbes district are intruded by granites, but the Upper Devonian is not intruded by granite. Hence the tentative age of the granite is considered to be Middle Devonian. The Silurian and Devonian sequence under- lying the Upper Devonian in the Tullamore Syncline is only very gently folded in large open folds similar to the folding style of the Upper Devonian. Yet, it appears that acid volcanism and granite intrusion took place after most of the Silurian-Devonian succession was deposited. In general, granites of this age are very rare in the Forbes-Bogan Gate district, and are normally only small stocks that have not metamorphosed or affected their intruded sediments to any great extent. The Gobondery Granite that outcrops several miles to the west of The Troffs (Fig. 17), on the other hand, is a large granite massif which intruded the Silurian-Devonian sediments with significant contact metamorphism (Raggatt, 1937). The surface on to which the Upper Devonian was deposited in the Tullamore-Bogan Gate- Forbes district is thought to have consisted of an undulating plain of sub-horizontal Silurian and Devonian sediments which were covered with acid volcanic flows in some areas. STRATIGRAPHY OF THE HERVEY GROUP The stratigraphy of the Hervey Group in the Tullamore-Weddin Range region is illustrated on Fig. 5. Eight stratigraphic columns (columns E to C, Fig. 5) show variations in stratigraphy. The Upper Devonian rocks of the Hervey Group make a distinct unit, and can be sub- divided as follows : Top Cookamidgera Undifferentiated red beds Sub-Group ( Weddin Sandstone Nangar Sub- Cloghnan Shale Group Troffs Formation BasE Beargamil Sub- Bogan Gate Sandstone. Group All these formations outcrop in the Tullamore and Trundle-Bogan Gate districts (Figs 15, 17). Strike ridges of the massive sandstones of the Weddin Sandstone continue southwards to the Weddin Range where this formation has its type section. The basal red beds of the Beargamil Sub- Group are represented by the Bogan Gate Sandstone which is well developed in the Bogan Gate district. North of Bogan Gate, basal red beds are rare or missing for the first time in the Hervey Group. Instead, marine sandstones and calcarenites of the Troffs Formation pass gradually into the basal fish plate-bearing sandstones of the Weddin Sandstone. The Nangar Sub-Group can be divided into three formations called the Troffs Formation, the Cloughnan Shale and the Weddin Sandstone. The Troffs Formation consists of interbedded quartzose sandstones, siltstones and shales, and is best developed near The Troffs, north of Trundle (Fig. 17). The Cloghnan Shale consists mainly of siltstone and shale and overlies the Troffs Formation. It is also best developed to the north of Trundle in the vicinity of Cloghnan (Fig. 17). The Weddin Sandstone makes out- crops as high sandstone ridges from the Weddin Range to Tullamore in the north. It overlies — the Cloghnan Shale in the Bogan Gate-Tullamore district but rests directly on the red beds of the Beargamil Sub-Group in the Weddin Range. A red bed succession occurring above the Weddin Sandstone has been correlated with the Cookamidgera Sub-Group. Poor exposures make it impossible to subdivide this Sub-Group in the Tullamore-Weddin Range area. THE BoGAN GATE SANDSTONE The Bogan Gate Sandstone is the only named formation in the Beargamil Sub-Group in the Tullamore-Weddin Range area. In the type area at Bogan Gate, it consists of a succession STRATIGRAPHY OF HERVEY GROUP IN CENTRAL N.5.W. i1 TULLAMORE SYNCLINE eas CREEK BENALONG CLOGHNAN HERVEY GROUP = [ COOKAMIDGERA SUB -GROUP | ?L. CARBONIFEROUS | WEDDIN S.S. ~ U- DEVONIAN | CLOGHNAN SHALE TROFFS FM. 0 SECTIONS ACROSS THE TULLAMORE SYNCLINE Fic. of coarse-grained red sandstones, and inter- bedded red siltstones. To the south, in the Weddin Range, it mainly consists of fine-grained red sandstones and siltstones. To the north of Trundle, the Bogan Gate Sandstone is missing from the succession. The type section was measured 12 miles north- east of Bogan Gate on the eastern limb of the Tullamore Syncline (column F, Fig. 5). In this locality the Bogan Gate Sandstone dips at angles of 20 to 30 degrees under the strike ridges of the Troffs Formation. The following succession was measured in the type section : Top Red shales and siltstones : 110’ Coarse-grained red sandstone, red silt- stone ee ; 300’ Red shales and siltstones. : 100’ Base Coarse-grained red sandstones, minor fine red sandstone and siltstone Me 400’ TotaL THICKNESS 910’ The Bogan Gate Sandstone reaches its maximum thickness in this area. Southwards along the eastern limb of the Tullamore Syncline the basal red beds do not outcrop very well. Most of them have been removed by erosion and covered with alluvium. In the Weddin Range, the Bogan Gate Sandstone is 800 feet thick and unconformably overlies older Palaeozoic quartz sandstones and siltstones that strike at right angles to the Hervey Group and dip at angles of 80 degrees to the west. Small lenses or reworked limestones occur in the Bogan Gate Sandstone in this locality. These rocks are PRE - SILURIAN TULLAMORE SYNCLINE Vv? 7M. DEVONIAN -SLURIAN SHALE, LIMESTONE,SANDSTONE [“—] ? L. DEVONIAN VOLCANICS RN SLATES, PHYLLITES 1 72 3 Nios Pcs il Scale in miles H IN THE TULLAMORE DISTRICT 18 called calclithites and consist of many limestone fragments derived from older limestones from the basement rocks. Three miles to the north of Bogan Gate, the Bogan Gate Sandstone is only two to three hundred feet thick and rests with a slight unconformity on the acid lavas of probable Lower Devonian age. Five miles to the north of Bogan Gate on the western limb of the Tullamore Syncline, the Bogan Gate Sandstone is only 100 feet thick. No fossils have been found in the Bogan Gate Sandstone but sedimentary structures such as current bedding, ripple marks, and worm tracks and burrows are common. THE NANGAR SUB-GROUP The Nangar Sub-Group in the Tullamore- Weddin Range district can be subdivided into three formations, the Weddin sandstone, the Troffs Formation, and the Cloghnan Shale. The Troffs Formation forms the basal forma- tion of the Hervey Group in the Tullamore region. Relationships between the basal beds of the Troffs formation and older Palaeozoic rocks are hard to assess because of lack of good contacts in the field. North of The Troffs where the type section was measured, quartzose sand- stones and calcarenites rich in shallow-water marine fossils, appear to be conformable with the lowermost quartzose sandstones of the Troffs Formation. Both sequences strike and dip at the same attitude, but there is an erosional gap that probably represents 500 feet of sediment 72 J. R. CONOLLY between the two sequences. The Troffs Forma- tion is defined as the basal sandstone and shale formation of the Nangar Sub-Group in the Bogan Gate-Tullamore district. It consists mainly of fine-grained sandstones which do not make strike ridges as large as those of the Weddin Sandstone. It is conformably overlain by a shale formation which is called the Cloghnan Shale. The type section measured two miles to the north-east of the Troffs railway siding was as follows : Top Fine-grained white sandstones and silt- stones 7 200! Erosion gap—probably fine sediments ? 300 Coarse-grained white sandstones, and flaggy white sandstones : 60’ Fine-grained white sandstones, with red siltstones. s HLDO" Erosion gap, ‘traces of fine- -grained sand- stone sf 100’ Coarse-grained white sandstone, traces of brachiopods ate Ree yg lg BasE Erosion gap . ? 400’ TotTaL THICKNESS .. 1,340’ The Troffs Formation thins towards Bogan Gate. On the eastern limb of the Tullamore Syncline, north of Bogan Gate it is approximately 1,000 feet thick and on the western limb of the Tullamore Syncline to the west and north-west of Bogan Gate where it is 800 feet thick. To the south the Troffs Formation appears to thicken, however field relations are not clear in this area and it is possible that some of the sediments shown as the Troffs Formation may be intolded older Devonian basement sediments. The Troffs Formation thickens slightly towards the north and a thickness of 1,500 feet was measured near “ Aurora Park ’’ homestead east of Tullamore (column E, Fig. 5). Traces of fish plates were found in upper sandstones of the Troffs Formation, four miles to the north-west of Bogan Gate and traces of brachiopods are commonly found in the basal sandstones in the Trundle district. Current bedding and current ripple marks are abundant and load casts are preserved on the lower faces of some sandstones. The Cloghnan Shale: This formation con- formably overlies the Troffs Formation. It is defined as a thick shale and siltstone sequence that lies between the lower sandstones of the Weddin Sandstone and the upper sandstones of the Troffs Formation. It makes very poor outcrops and is a very mappable formation in the Tullamore region where it makes a well marked valley between strike ridges of the Weddin Sandstone and the Troffs Formation. Because of its less resistant nature, it was impossible to find a complete succession to measure. The type area was taken in the vicinity of Cloghnan station about six miles north-east of The Troffs (Fig. 17). In this vicinity the Cloghnan Shale is approximately 600 feet thick and consists of very fine-grained sandstones, coarse siltstones and shales that vary in colour from green to red. The Cloghnan Shale thickens considerably to the north and is over 2,000 feet thick near the “‘ Aurora Park ”’ station homestead (column E, Fig. 5). The Cloghnan Shale thins towards the south and thicknesses between 200 to 400 feet are common in the Bogan Gate district. No fossils have been found in this formation. Ripple marks and small-scale current bedding are the most common sedimentary structures and generally occur in coarse siltstones. THE WEDDIN SANDSTONE The Nangar Sub-Group cannot be subdivided into individual formations in the Weddin Range area where the Weddin Sandstone forms rugged © sandstone cliffs 800 feet high. The following sequence was measured as the type section of the Weddin Sandstone, near Black Spring Mountain in the Weddin Range: Top Fine and medium-grained white and buff sandstones with inter-bedded grees and white siltstones 4.00’ Medium white sandstones, coarse sand- stones interbedded with several 10’ to 20’ thick conglomerate layers 650’ Base White and red sandstones, conglomerate, but many fine red and white sand- stones and siltstones Rt : 450’ ToTAL THICKNESS :, L,5064 The Weddin Sandstone thins slowly to the north, and is probably only 1,000 feet thick in the Wheoga Range although the upper parts of the sequence have been removed by erosion. Better outcrops occur in the ranges near Bogan Gate and east of Tullamore where the Weddin Sandstone forms prominent strike ridges. The Weddin Sandstone makes large strike ridge outcrops in the Tullamore-Bogan Gate region. A section measured two miles north of Bogan Gate is 900 feet thick, consisting of medium to coarse-grained white sandstones with occasional pebbly and conglomerate layers. In the Tullamore region the Weddin Sandstone thickens considerably and is probably just over 2,000 feet thick in most sections (Fig. 5), although the upper parts of the outcrops are frequently removed by erosion. A conglomerate horizon is + Ay Sey STRATIGRAPHY OF HERVEY GROUP IN CENTRAL N.S.W. 73 present about 400 feet above the base of the formation and makes a good marker bed for mapping. This conglomerate is 10 to 50 feet thick and consists of pebbles of vein quartz, chert, and acid volcanic rocks. The pebbles range in size from quarter to one inch in diameter and are very well rounded. Fish plates are found in this formation. Although no excellent specimens have been found, impressions of individual plates are fairly abundant and similar to types described by Hills (1932, 1935) from the Hervey’s Range. Current bedding measurements in _ coarse- grained sandstones of the Weddin Sandstone show a palaeocurrent from the west, north-west and north in the Bogan Gate-Tullamore district although palaeocurrents consistently come from the north in the Weddin Range area. THE COOKAMIDGERA SUB-GROUP Thick red measures that conformably overlie the white sandstones of the Weddin Sandstone have been correlated with the Cookamidgera Sub- Group. These red beds are characterised by very poor exposures and in most localities occur underneath alluvium-filled valleys in the syn- clinal axis of the Tullamore Syncline. The thickness of these beds is estimated to be between 1,500 and 2,500 feet. Jed siltstones are the most abundant sediment, and ripple marks, the characteristic sedimentary structure. No fossils have been found in these beds. The Murda Syncline The most western outcrop of Hervey Group sediments occurs in a large synclinal structure, called the Murda Syncline, that outcrops to the north of Condobolin. Outcrop distribution and stratigraphical columns measured from this area are shown on Fig. 5. The Murda Syncline is named after Murda Murda Creek that flows through the syncline throughout most of its length (Fig. 19). The geology of the Murda Syncline is shown on the geological map (Fig. 19) which has been prepared using air photos and field traverses. Once again, strike ridges of Upper Devonian sandstones make the most marked relief-forming features in an area of flat plains or slightly undulating country which is mainly formed of alluvium and poor outcrops of older Palaeozoic rocks. The relief caused by the strike ridges of the sediments of the Hervey Group is generally small, but some hard sand- Stone ridges such as the ridge that forms the Boona Mountain rise 500 to 600 feet above the surrounding plain (Fig. 19). Geological sections across the Murda Syncline are shown on Fig. 20. The Murda Syncline is a broad open synclinal structure with minor folding on the northern limbs. The Murda Syncline shown on the geological map (Fig. 19) is 36 miles long, measured along the strike, and between 5 and 14 miles wide across the strike. The Murda Syncline extends several miles to the north and north-west of the area shown on Fig. 19. In general, the eastern limb of the syncline dips westward at angles of 30 and 20 degrees, while the western limb 1s somewhat steeper and dips at angles of 40 to 60 degrees to the east. Erosion has removed large areas of outcropping rock particularly around Murda Murda Creek in the southern part of the syncline. Dips in the centre of the syncline are low and average between 5 and 15 degrees. Minor folding and faulting is common in the area between Campbells Tank and most northern extensions of the syncline. Faulting in the region of Boona Gap has brought older limestones of probable Silurian age against Upper Devonian sandstones. Large strike faults also occur in regions of tight folding south of Watson’s Gap and also in the region of the southern nose of the Murda Syncline. Raggatt (1937) made a regional investigation of the Condobolin-Trundle sistrict that has already been briefly discussed. Raggatt, in an unpublished report (1936), named the quartzites and sandstones of the Upper Devonian, the Boona beds. This name has been retained for the hard sandstones, now called the Boona Sandstone, that make strike ridges of the Boona Mountain. (Note: there is a formal description of a Boonah Sandstone formation in the Victorian Tertiary sequence (Raggatt and Crespin, Proc. TOV OOCy 6) 1.5 40 (2 (ll) A115) In most localities, the sediments of the Hervey Group rest unconformably on older regionally metamorphosed slates, phyllites and schists of probable Silurian or Ordovician age. To the north-west of the Murda Syncline outcrops the Wilmatha Granite which has been given a late Silurian age by Raggatt (1937). More recent alluvium and gravels have been subdivided into two groups by Raggatt (1937). The first is the Pleistocene and Recent alluvium of the Lachlan River and the second the Tertiary alluvial deposits and gold-bearing leads that were previously described by Morrison (1927) from the Fifield area to the east of the Wilmatha Syncline. STRATIGRAPHY The stratigraphy of the Hervey Group in the Murda Syncline is illustrated on Fig. 5 in three 74 J.‘R.. CONOLLY stratigraphical columns. The basal red beds of the Beargamil Sub-Group that are characteristic features of the Hervey Group elsewhere in central New South Wales do not outcrop in the Murda Syncline. Instead, there is a formation of poorly-sorted sandstones, thin conglomerates, and shales with poorly preserved marine fossils, which are herein grouped into the Condobolin Formation. Above the Condobolin Formation are the white sandstones and interbedded red and white siltstones of the Boona Sandstone which can be correlated with the Nangar Sub- Group. The uppermost formation is a red bed sequence called the Belvedere Formation, which is probably an equivalent of the upper red beds of the Cookamidgera Sub-Group. Hence, although the base of the sequence is a marine, not an arkosic sequence, the formations TO ALBERT 20 MILES os STATE FOREST POSTULATED THE HERVEY GROUP IN THE MURDA_ SYNCLINE AXIS OF THE MURDA SYNCLINE GEOLOGICAL MAP .SHOWING eS —~__ DuBe a NY ATSONS \\oaP conformably overlying the basal sequence correlate with the typical Hervey Group succession. Traces of Lepidodendrid plant and fish plate remains have been found in the Boona Sandstone. Poorly preserved pelecypods, corals, and brachio- pods in the Condobolin Formation are probably indicative of an older age than Upper Devonian, and may be correlated with the “‘ Ampitheatre Stage ’’ (Lower to Middle Devonian) in the Cobar region to the west of Condobolin (Mulholland, 1940). THE CONDOBOLIN FORMATION The Condobolin Formation is the basal formation of the Devonian sequence in the Murda Syncline. Raggatt (1937) subdivided the 4 Ye Ww PINE PARK “ STRATIGRAPHY OF HERVEY GROUP IN CENTRAL N.S.W. 15 Devonian sequence in the Condobolin district into four units. The upper unit is defined as the Boona Sandstone in this report and the lower three units are grouped into the Condobolin Formation. The Condobolin Formation consists of inter- bedded shales, siltstones, sandstones and con- glomerates. In some localities conglomerate beds are abundant towards the base of the formation, particularly to the west of Wilmatha Hill where the Condobolin Formation forms outcrops in a synclinal structure away from and to the west of the main Murda Syncline (Fig. 19). In other localities, however, and particularly in the southern regions of the Murda Syncline conglomerate beds occur sporadically throughout the sequence and do not form distinct basal horizons. (ss) Belvedere Fm. Boana S.S. CondoboLin Fm. Slates, phyllites, Mica schists. Hervey Group uw E >. a 3 < i re o 15) oe a 1 c s = E Middle Devonian [Wilmatha Granite [FDa+7] 7 L. Carboniferous - ? M. Devonian ? Silurian ? Ordovician CAMPBELLS]: | TANK [oo The Condobolin Formation forms a sequence which is generally much softer than the Boona Sandstone and is poorly exposed. The type section was measured approximately six miles north of Condobolin on the eastern limb of the Murda Syncline. Here outcrops are bad, but the following subdivisions were esti- mated : Top Green and red shales, red siltstone, some thin sandstone members ‘ 300° Conglomerate beds with pebbles of vein quartz and chert, quartz-rich but poorly-sorted sandstones, interbedded shales and siltstones ie .. 400’ Poor exposures, siltstones and shales the dominant lithology, some thin con- glomerate and sandstone beds 300° BASE . 1,000’ —_|}-— ye pa E Geological boundary Geological boundary position approximate Dip and strike @ir photo interpretation) Dip strike (from field observation) Fault position approximate Synclinal axis Anticlinal axis Fic. 19 TO CONDOBOLIN 4 MILES — dana, a ae ; 74 J. R. CONOLLY stratigraphical columns. The basal red beds of the Beargamil Sub-Group that are characteristic features of the Hervey Group elsewhere in central New South Wales do not outcrop in the Murda Syncline. Instead, there is a formation of poorly-sorted sandstones, thin conglomerates, and shales with poorly preserved marine fossils, which are herein grouped into the Condobolin Formation. Above the Condobolin Formation are the white sandstones and interbedded red and white siltstones of the Boona Sandstone which can be correlated with the Nangar Sub- Group. The uppermost formation is a red bed sequence called the Belvedere Formation, which is probably an equivalent of the upper red beds of the Cookamidgera Sub-Group. Hence, although the base of the sequence is a marine, not an arkosic sequence, the formations conformably overlying the basal sequence correlate with the typical Hervey Group succession. Traces of Lepidodendrid plant and fish plate remains have been found in the Boona Sandstone. Poorly preserved pelecypods, corals, and brachio- pods in the Condobolin Formation are probably indicative of an older age than Upper Devonian, and may be correlated with the ‘‘ Ampitheatre Stage ” (Lower to Middle Devonian) in the Cobar region to the west of Condobolin (Mulholland, 1940). THE CONDOBOLIN FORMATION The Condobolin Formation is the basil formation of the Devonian sequence in the Murda Syncline. Raggatt (1937) subdivided the IN THE MURDA SYNCLINE THE HERVEY GROUP BULBODNEY GEOLOGICAL MAP SHOWING | VEDERE [ee STRATIGRAPHY OF HERVEY GROUP IN CENTRAL N.S.W. 75 Devonian sequence in the Condobolin district into four units. The upper unit is defined as the Boona Sandstone in this report and the lower three units are grouped into the Condobolin Formation. The Condobolin Formation consists of inter- bedded shales, siltstones, sandstones and con- glomerates. In some localities conglomerate beds are abundant towards the base of the formation, particularly to the west of Wilmatha Hill where the Condobolin Formation forms outcrops in a synclinal structure away from and tothe west of the main Murda Syncline (Fig. 19). In other localities, however, and particularly in the southern regions of the Murda Syncline conglomerate beds occur sporadically throughout the sequence and do not form distinct basal horizons. The Condobolin Formation forms a sequence which is generally much softer than the Boona Sandstone and is poorly exposed. The type section was measured approximately six miles north of Condobolin on the eastern limb of the Murda Syncline. Here outcrops are bad, but the following subdivisions were esti- mated : Top Green and red shales, red siltstone, some thin sandstone members ate Conglomerate beds with pebbles of vein quartz and chert, quartz-rich but poorly-sorted sandstones, interbedded shales and siltstones om Ss Poor exposures, siltstones and shales the dominant lithology, some thin con- glomerate and sandstone beds 300° 400° 300° BasE - 1,000° AA G bes Uf ‘s ii red —— —— p = ae ie : ' zi f 8 mae if san8; iO epee a eR ESEZ Ss 1 1 z 2 Fic. 19 TO CONDOGOLO 4 MILES 76 J. R. CONOLLY WATSONS GAP a ah MOUNTAIN MURDA SYNCLINE MURDA SYNCLINE MURDA CK HERVEY GROUP BELVEDERE FM. 7 L.CARBONIFEROUS - 2 M. DEVONIAN BOONA S.S CONDOBOLIN FM 0 “n i M. DEVONIAN ? SIL.-?0RD WILMATHA GRANITE SLATES, PHYLLITES, MICA SCHISTS 1 2 3 Scale in miles SECTIONS ACROSS THE MURDA SYNCLINE Fie. 20 Rapid changes in thickness are characteristic of the Condobolin Formation and along the eastern limb of the Murda Syncline the thickness of the Condobolin Formation varies from 200 feet to 1,500 feet. The boundary of the Condobolin Formation with older Palaeozoic basement rocks can be easily seen due to differences in vegetation on air photos. Estimates of the thickness of the Condobolin Formation show that it varies considerably in thickness and _ facies. The Condobolin Formation has a thickness of over 2,000 feet in the Yarra Yarra Creek area 6 miles to the north-west of Wilmatha Hill. In this locality, thin limestone beds occur interbedded in a sequence which consists of shales, sandstones and conglomerates. Species of brachiopods probably belonging to the genus Sfzmnella are abundant throughout the limestone and may be indicative of a Middle Devonian age. The faunas described from the lower units of the Devonian in the Condobolin district by W. S. Dun have been ascribed to the top of the Middle Devonian or to the base of the Upper Devonian Dyy Dr Fo We ‘Booker (in Rageatt alsa) However, since the sediments of the Condobolin Formation are conformable with the overlying Upper Devonian Sandstones of the Boona Sandstone they have been included in the Hervey Group. THE BoonAa SANDSTONE The Boona Sandstone is a sandstone formation conformably overlying the Condobolin Forma- tion. The entire Upper Devonian sequence including the Boona Sandstone and the overlying red beds of the Belvedere Formation was originally called the Boona Beds in an un- published report by Raggatt (1936). The name Boona Sandstone has now been restricted to the sandstone formation that makes the strike ridges of the Boona Mountain on the western limb of the Wilmatha Syncline. In this locality the Boona Sandstone consists of 1,500 feet of interbedded white sandstone, white grits, and thin red sandstone and red silt stone members. Along the eastern limb of the Wilmatha Syncline the Boona Sandstone thickens 1,000 feet in the south to 1,750 feet in the north (columns C to A,-Fig.-5)>~ Curreng bedding measurements in the eastern limb show palaeocurrents from the north-west and south- west. The only fossils found were poorly preserved traces of Lepidodendrid plants and fish plates and probably indicative of an Upper Devonian age. THE BELVEDERE FORMATION The Belvedere Formation conformably over- lies the Boona Sandstone. It consists of a thick sequence of red beds which normally form poor outcrops, but which form reasonably good outcrops near the “‘ Belvedere ”’ station property, about 25 miles north of Condobolin (Fig. 19). In the type area, on the “ Belvedere ”’ station property, the red sandstones of the Belvedere Formation make a large basin structure in the axial region of the Murda Syncline. Dips are shallow within this structure and minor folding may be present of the outer edges of it. Between the upper red sandstones of the Belvedere Formation which make the outcrops near ‘““ Belvedere’ homestead and the sandstones of the Boona Sandstone, there is a large poorly outcropping area of red shales and siltstones STRATIGRAPHY OF HERVEY GROUP IN CENTRAL N.S.W. 17 These finer red sediments form the lowermost sequence of the Belvedere Formation. Their thickness is estimated at 400 to 600 feet. The upper sequence of sandstones is 500 feet thick near Belvedere, making the total estimated thickness in the type area of at least 1,100 feet. The upper sandstones are also well preserved in strike ridges along the western side of Murda Murda Creek as it flows southwards towards Condobolin. Estimated thickness of the Belvedere Formation in other areas of the Wilmatha Syncline vary from 600 to 1,100 feet. Traces of fish plates have been found in the Belvedere Formation in the type area and sedimentary structures such as ripple marks and current bedding are common. CORRELATION AND STRATIGRAPHIC SUMMARY OF THE HERVEY GROUP It has been shown that the Hervey Group characteristically consists of three main litho- logical sequences which have been grouped into three Sub-Groups, the Beargamil, Nangar and Cookamidgera Sub-Groups. Figures 4 and 5 show the correlation of these Sub-groups from one measured column to another. Except in the Murda Syncline and in the Tullamore district, the basal sequence of the Hervey Group consists of red measures. These red measures vary considerably in mineralogical and fragmental rock content (Conolly, 1962) but all are indicative of an arkosic type of sedimentation. The basal red-bed formations of the Beargamil Sub-Group can be correlated with one another because of their position in the sequence and their similar types of lithology. The overlying sediments have an Upper Devonian age, hence it seems a permissible assumption that these red beds are the basal formations of an Upper Devonian sequence. The Nangar Sub-Group consists of a sequence of formations which are either dominantly sandstone, or red siltstones, or a succession of both of these lithologies. Rapid changes in thickness and lithology in this Sub-Group not only make correlation difficult, but also make the definition of actual formation boundaries difficult. Hence, it has been necessary to define the upper and lower surface of formations in a arbitrary manner. For instance, the Mandagery Sandstone is the basal formation of the Nangar Sub-Group and its lower boundary is defined as the first thick massive white sandstone above the red beds of the underlying Beargamil Sub-Group. The upper boundary of the Mandagery Sandstone is also an arbitrary one and coincides with the last massive white sandstone bed underlying a thick sequence of red siltstones or finer-grained sediments. The entire succes- sion of the Nangar Sub-Group is essentially similar and consists of repetitions of the cycle, white quartzose sandstones, red and white sandstones with some red siltstones, and then red siltstones. When the first member of this cycle, that is, the quartzose sandstone member, is developed as a mappable sequence it has been given a formation name. Similarly the red siltstones of the upper cycle also frequently form a mappable formation. It is in this manner that the Nangar Sub-Group has been subdivided. Hence, in the eastern area of outcrop shown on Fig. 4 the basal formation of the Nangar Sub-Group is a quartzose sandstone formation called the Mandagery Sandstone. In the western area of outcrop shown on Fig. 5, the Weddin Sandstone and the Boona Sandstone are equivalent sandstone formations to the Mandagery Sandstone but do not always occur immediately above basal red beds. Since the Mandagery, Boona, and Weddin Sandstones are similar in lithology, normally overlie basal formations of the Hervey Group, and all contain traces of a Bothriolepid fish- plate assemblage, it seems feasible to make a tentative correlation of these three formations with one another. Correlation of formations above the Mandagery Sandstone in the eastern area of outcrop in the Nangar Sub-Group is not so easy. It is normal to find a rhythmic succession of red and white measures after the first white sandstone formation of the Nangar Sub-Group. Some of these red or white sequences may be regarded as lithological units and are given formation names, while in other areas several such units are grouped together into one formation. For instance, in the Manildra- Gocloogong region, the first thick red siltstone and fine-grained red sandstone formation is called the Pipe Formation. This formation contains many thin beds of white sandstone and red siltstone. On the other hand, further south in the Gooloogong-Grenfell region, the formation that has an identical position in the sequence as the Pipe Formation, the Hunter Siltstone, consists almost entirely of red silt- stones. Hence if these two formations have been laid down at similar times then there is a distinct facies change between the two areas. Although sequences similar to those of the Pipe Formation and Hunter Siltstone are fairly consistent over a small area (10 to 20 miles), they are inconsistent over larger areas, making 78 J. R. CONOLLY it impossible to make positive correlations in the upper horizons of the Nangar Sub-Group on lithological grounds. Fossils are also of not much help in the upper formation of the Nangar Sub-Group. Many of these formations have a Lepidodendrid assemblage but the Bothriolepid assem lage is not so abundant. In the western area of outcrop shown on Fig. 5, the Weddin Sandstone has _ been tentatively correlated with the Boona Sand- stone. Underlying both of these formations in the Condobolin and Bogan Gate-Tullamore districts is a sequence of interbedded sand- stones, siltstones and sometimes thin beds of conglomerate in which traces of marine fossils are common and which may be indicative of a Middle Devonian or lower Upper Devonian age. It seems feasible to correlate these sequences, namely the Condobolin Formation, in the Condobolin district, and the Troffs Formation in the Bogan Gate-Tullamore district with one another. The upper red measures of the Hervey Group which have been called the Cookamidgera Sub-Group have been preserved in many areas. Several problems arise in the correlation of this Sub-Group. It seems that the rhythmic red and white sedimentation typical of the Nangar Sut-Group always terminates with a terresttial sequence of red beds which has been called the Cookamidgera Sub-Group. However, these uppermost red bed sequences may only corres- pond to thick red bed cycles of the Nangar Sub-Group... As most, lof “these beds sare extremely thick, much thicker than any of the red bed sequences that occur interbedded in the Nangar Sub-Group, it seems more reasonable to put the upper red’ bed sequences sof. the Hervey Group into a separate Sub-Group. Figures 4 and 5 show that the measurable thickness of the Hervey Group varies consider- ably. The largest thickness occurs in the Parkes Syncline, where there is over 9,000 feet preserved, and the maximum recorded thickness in most other areas varies between 4,000 and 8,000 feet. The variation in thickness and lithology is best studied at the level of Sub- Groups and formations which can be correlated from one area to another. THE BEARGAMIL SUB-GROUP Figure 21 is an isopach map of the Beargamil Sub-Group in central New South Wales. Although readings of thickness were not avail- able in some areas because of lack of outcrop, the isopach map clearly indicates that the Beargamil Sub-Group was not deposited any Tullamore fs? o ( Bogan “xe ® / Monildra / [ ® \\ sandstones 4 dbundant \N \ conglomerates abundant scale in miles (SOPACH MAP OF THE BEARGAMIL SUB - GROUP IN CENTRAL NEW SOUTH WALES (isopachs in hundreds of feet) Ere? 2! further west of the Tullamore-Bogan Gate region, and probably not further east than Manildra and not much further south than Young. To the north-east of Peak Hill there is a great thickness of basal red beds which is thickening steadily to the north. Other areas where a large thickness of sediment was deposited occur just to the east of Grenfell and just to the east of Bogan Gate. The areas of greatest thickness are also the areas with the coarsest sediments. From an inspection of the isopach map, it can be easily seen that the coarsest and thickest basal red bed sequences were laid down along a line that runs from near Grenfell north and _ slightly west towards Bogan Gate and then north and slightly east towards Peak Hill. The sequence thins steadily from these areas towards the south, west and south-east, but fluctuations. in thickness are present in the north-east. The Beargamil Sub-Group was deposited in a STRATIGRAPHY OF HERVEY GROUP IN CENTRAL N.5.W. trough-like area closed at its eastern, southern and western ends. The thickest accumulation of sediment took place along the central portion of this area with the deposition of conglomerates and coarse sandstones, as well as finer-grained sediments. THE NANGAR SUB-GROUP Problems of correlation make it difficult to reconstruct changes in lithology and thickness over any great lateral extent. The oaly sequence of beds that can be correlated through- out the area of deposition is the sequence of white orthoquartzites containing Bothrioleprs that occurs immediately above the Beargamil Sub-Group, in the east and ove:lying marine formations in the west. Figure 22 is an isopach map of this series of sandstone formations, namely the Mandagery, Weddin and Boona Sandstones. The thickest accumulations of sediment took place to the north of Tullamore and in a separate basin to the north-east of Forbes. The sedi- ments thin steadily to the east, indicating that a zero isopach could probably be found in that direction. The sediments also thicken steadily to the north in the Tullamore-Condobolin region. A ridge structure is present between Peak Hill and Forbes, where very little sediment was deposited. This ridge may probably correspond to an area in which siltstone sedimentation was greater than the sandstone sedimentation that makes this cycle. One of the most important features shown by this isopach map is the non-appearance oi any zero isopach line. In particular, the only trend that indicates the presence of such a line would be to the east. To the west, south, and north, however, deposition must have continued for some distance out of the area shown on Fig. 22. Figure 22 also shows the presence of a basal conglomerate facies along the south, south-western and western portions of the atea, and an area to the west and south of Grenfell where conglomerates were abundant. Finer- grained sandstones occur more frequently to the north-east. Hence, there is a facies change from fine-grained sandstone and siltstone in the north-east to sequences with abundant conglomerates in the west and south. Figure 23 is a palaeocurrent diagram showing the palaeocurrent directions for the Nangar Sub-Group sediments. The directions shown on this diagram were obtained from many hundreds of current bedding readings. Twenty to thirty readings were taken in each locality before the palaeocurrent direction was 79 calculated. Generally, palaeocurrents came from the west and as they approached the eastern area of deposition, swung southwards towards Young. South-east of Peak Hill there are some readings that indicate a local palaeo- current from the south-east. The thinning of the first orthoquartzite formation to the east and the abrupt swing in palaeocurrent direction when it reaches the east indicates that there may have been some barrier or high area to the east impeding deposition. Currents were probably strongest in the south near Young and along the western margin of the area shown on Fig. 23, where the conglomerate facies (mentioned above) was deposited. The sediments of the Nangar Sub-Group above the first otrhoquartzite cycle attain large thicknesses wherever they are preserved. There are not enough data available to enable the construction of an isopach map, but some general conclusions can be made by studying the changes in thicknesses and lithology as shown on the correlation diagrams (Figs. 4 and 5). Whereas the lower orthoquartzite cycle in the Nangar Sub-Group thinned to the east, the upper formations thicken. Coarse sand- stones and conglomerates are also present in the upper formations in the eastern area, but have not been found in any other areas. It seems that the sediments of the upper Nangar Sub-Group are essentially a sequence of cycles of red and white beds which thicken, and transgress the thin basal orthoquartzites to the east, but which thin to the west. THE COOKAMIDGERA SUB-GROUP The last phase of sedimentation that is preserved is a red-bed sequence consisting of red fine-grained sandstones, red siltstones, and red mudstones. This sequence, called the Cookamidgera Sub-Group, represents a thick sequence of red measures overlying the Nangar Sub-Group. Variation in thickness and lithology cannot be estimated, since erosion has removed most of the outcrops. Sedimentation The palaeogeography and sedimentation of the Upper Devonian rocks of the Lachlan Geosyncline have been reviewed by the author (Conolly, 1964). In this review petrological results were used as an aid to correlatioa and to the interpretation of provenance. The sedimentation of the Hervey Group was described for three time periods. flow direction Q from field Wi measurements ——) Interpreted main palaeocurrent direction Outcrop of the Harvey Group 0 ™N scale PALAEOCURRENT DIRECTIONS SUB - SROUP IN CENTRAL NEW SOUTH bedding calculated from current A Grenfell ) r \ 1 32 in miles vou? IN THE NANGAR WALES medsurements Fic. 23 an area confined by the isopachs shown on Fig. 21. The thickest accumulation of sediment took place in a trough-like area in the Grenfell district, where conglomerates are a characteristic feature of the basal sequence. Most of the deposits thickened or thinned into local basement highs and wedge-shaped deposits were commonly formed. The sediment was carried into the area by a large stream system which probably fed from a southern land mass and the sediments were deposited on an alluvial plain. The sea flanked this land area to the east near Wellington (Conolly, 1963), and to the north-west in the Tullamore-Condobolin district. In these areas, sandstones, shales, siltstones and con- glomerates were deposited in environments which probably fluctuated from estuarine to marine shelf. F 2. UPPER DEVONIAN TO LOWER CARBONIFEROUS The remainder of the sediments of the Hervey Group overlying the basal formations was very probably deposited throughout the Upper Devonian and into the Lower Carboniferous. The nature of the sedimentary structures such as current bedding, the cyclic mode of deposition, the abundance of plant and fish remains clearly suggest that the rocks were deposited in a terrestrial environment. The palaeocurrent directions shown on Fig. 23 suggest that the rivers carrying the sediments flowed from the west near Condobolin and Tulla- more and then flowed southwards in the Parkes or eastern area of deposition. It appears that the rivers may have flowed around a land barrier which existed south of Condobolin. 82 J..R. CONOLLY Deposition of the cycle, coarse sandstone, followed by sandstones and siltstones, and then by siltstones and mudstones, is_ probably typical of the cycles deposited by a large meandering river. The coarse deposits are deposited in the areas of the strongest currents. As the banks of the river are cut away, then the location of the strongest currents and hence the location of the deposition of the coarse sediments move. The coarse deposits are eventually covered by the fine-grained sands and silts of the point-bar deposits and then these in turn by the silts and muds of the flood plain. Rapid changes in thickness and lithology so prevalent in the Nangar Sub-Group are a characteristic feature of these deposits. Apart from normal river and flood-plain sediments, silts and muds were probably also deposited in large inland lakes or swamps. Acknowledgements This investigation was made while the author held a senior demonstrationship in geology in the School of Mining Engineering and Applied Geology, University of New South Wales. He is grateful for the assistance that the teaching and technical staff of this department afforded him during this period. References ANDREWS, E. C., 1910. The Forbes-Parkes Goldfield. Dept. Mines, N.S.W., Min. Resources No. 138. CoNnoL_Ly, J. R., 1960. Sedimentation in the Catombal Range, Wellington. Unpub. M.Sc. Thesis, Univ. N.S.W. ConoLty, J. R., 1962. Stratigraphic, sedimentary and palaeogeographic studies in the Upper Devonian rocks of central western New South Wales. Unpub. Ph.D. Thesis, Univ. N.S.W. Cono_Liy, J. R., 1963. Upper Devonian stratigraphy and sedimentation in the Wellington-Molong region, N.S:W. J. -Prac. Roy. Soc:, N.S:W., 96, 73° CONOLLY, J. R., 1964. The Upper Devonian rocks of the Lachlan Geosyncline, in “ The Geology of New South Wales’’. J. Geol. Soc. Aust. (in press). Davin, T. W. E., AND BROWNE, W. R., 1950. The Geology of the Commonwealth of Australia. E. Arnold & Co., London, 3 Vols. Dun, W. S., 1898. The occurrence of graptolites in the Peak Hill district. Rec. Geol. Surv. N.S.W.., 5, 83. Hamitton, L., 1961. Beargamil, Parkes. N.S.W. Hits, E. S., 1932. Upper Devonian fish from N.S.W. Quart. J. Geol. Soc. London, 88, 850-858. HILts, E. S., 1935. Records and description of some Australian Devonian fish. Proc. Roy. Soc. Vic., 48, 161-171. Morrison, M., 1927. Fifield test bores. Dept. Mines, N.S.W., 1138. MULHOLLAND, C. St. J., 1940. Geology and under- ground sources of the East Darling district. Min. Res. Mines Dept. N.S.W. No. 39. RaGGatTt, H. G., 1936. Geology and mineral resources of the Cundobolin-Trundle district. Unpub. Rept. Dept. Mines, N.S.W. RaGeatt, H. G., 1937. Geological survey of the Condobolin-Trundle district. Ann. Rept. Dept. Mines, N.S.W. (for 1936), 92-95. RAYNER, E. O., 1962. Mineralogy and genesis of the iron-rich copper ores of the Cobargo province, N.S.W. Unpub. Ph.D. Thesis, Univ. N.S.W. Rinais, J., 1962. The geology of the Toongi-Sappa Bulga district. Unpub. B.E. Thesis, Univ. N.S.W. STEGGLES, K., 1961. The geology of the Toongi- Dulladerry district. Unpub. B.E. Thesis, Univ. N.S.W. STEVENS, N.C., 1950. The geology of the Canowindra district, N.S.W. Part I. The stratigraphy and structure of the Cargo-Toogong district. J. Proc. Roy. Soc. N.S.W., 82, 319-337. STEVENS, N.C., 1951. The geology of the Canowindra district, N.S.W. Part II. The Canowindra-Cowra- Woodstock area. J. Proc. Roy. Soc. N.S.W.., Geology of the Parish of Unpub. B.E. Thesis, Univ. Ann. Rept. 84, 46-52. WILKINSON, C. S., 1885. Tomingley-Peak Hill Gold- field. Ann. Rept. Dept. of “Mines; WN.S.Wwe 128-129. STRATIGRAPHY, OF HERVEY GROUP IN CENTRAL N.538.W. 83 Explanation of Plates PLATE 1 Looking eastwards towards the Hervey’s Range from a locality six miles east of Peak Hill. The Caloma Trig. is the highest peak in the range, approximately 1,800 feet higher than the surrounding plain and distant three miles from the immediate foreground of the photograph. The portion of the Hervey’s Range in this photograph shows easterly-dipping strike ridges (from the closest ridge) of the Clagger Sandstone, Mandagery Sandstone, and the Caloma Sandstone. The Kadina Formation and the Pipe Formation form low hills and valleys between the ridges of the sandstone formations. The Clagger Sandstone and the Kadina Formation dip steeply to the east, the Mandagery Sandstone and Pipe Formation dip more gently to the east and the Caloma Sandstone has sub- horizontal dips to the east. Recent deposits of boulder drift and alluvial gravels occur at the front of the range. PLATE [1 1. Spillway of Lake Endeavour Dam, Bumberry Syncline east of Parkes looking eastwards towards the dam wall. Planar and current bedding units of the Mandagery Sandstone dip at a shallow angle to the east. A current- bedded unit on the left centre of the photograph reaches thicknesses of four feet and is overlain by planar beds of sandstone, six inches to two feet thick. 2. Spillway of Lake Endeavour Dam, Bumberry Syncline east of Parkes looking eastwards down the plunge of a basin-shaped current-bedded unit of the Mandagery Sandstone. This unit is typical of the style of current bedding within the Mandagery Sandstone. Measurements of the dips of the current bedding will normally be always in the direction of the plunge of basin. In this locality, these dips indicate palaeocurrents that flowed from west to east. The tape measure resting on the upper surface of the current-bedded unit in the foreground of the photograph is approximately six inches in diameter. 3. Spillway of Lake Endeavour Dam, Bumberry Syncline, east of Parkes, looking eastwards. Uniformly bedded fine-grained white orthoquartzites of the Mandagery Sandstone dip towards the east at 10°. The thickness of the beds of sandstone varies between six inches and two feet. 4. Spillway of Lake Endeavour Dam, Bumberry Syncline, east of Parkes, looking north-eastwards. Lenticular and arched beds of Mandagery Sandstone overlying planar beds. Some beds show evidence of movement due to slumping after deposition, but prior to the deposition of overlying beds. The sledgehammer in the centre of the photograph is approximately three feet in length. PLATE III 1. Four miles south-west of Gooloogong, looking eastwards at the basal sandstone beds of the Peaks Sandstone. These beds are coarse-grained red grits and pebbly sandstones forming the basal beds of the Hervey Group. The sandstones are quartzose and fragments of acid volcanics are fairly abundant. However, they unconformably overlie the Eugowra Granite. A boulder of this granite outcrops some 15 feet from the massive outcrop of the Peaks Sandstone. A sledgehammer is resting on this granite outcrop in the immediate foreground of the photograph. 2. Spillway of Lake Endeavour Dam, in the Bumberry Syncline, east of Parkes, showing slumped beds of Mandagery Sandstone. Two slump units can be seen, an upper large unit and a lower smaller unit near the lower right-hand edge of the photograph. The individual sand layers of the slumps rarely show any convolution or fracturing but form symmetrically arranged folds with a common fold axis. 3. Same locality as 2, showing the smaller slumped unit in 2; the tape measure is marked in inches. CONOLLY Plate I ts i & * teen ‘defied a $ ot ins. 4 k 3 — 4 ' + ‘ t eae ea % « ‘ ee rea ‘ dep Caloma Trig Caloma SS. Clagger SS. Alluvium Supplement to Journal Royal Society of New South Wales Printed in England CONOLLY Plate II CONOLLY Plate HI Journal and Proceedings, Royal Society of New South Wales, Vol. 98, pp. 85-90, 1965 A Note on the Stratigraphy of the Devonian Garra Beds of New South Wales DD: L. Srrusz Department of Geology and Geophysics, University of Sydney* ABSTRACT—The reconnaissance name ‘‘ Garra Beds ’’, introduced by Joplin and Culey (1938) for the southern portion of a belt of Devonian limestones near Molong and Wellington, N.S.W., is formally replaced by the name “ Garra Formation ”’’. The formation consists of reef and detrital limestones and shales, whose lateral and vertical relationships are highly complex. Because of this complexity, the discontinuity of outcrops, and the presence of extensive folding and strike faulting, it has not been possible to subdivide the formation. Overlying the limestones are sandstones and shales of the Upper Devonian Catombal Group ; the junction is commonly gently unconformable. Conformably beneath the limestones is a succession of sediments and volcanic rocks extending well down into the Silurian. The formation is probably either upper Lower or basal Middle Devonian in age. Introduction The purpose of this Note is to provide a formal definition of the Devonian limestone outcrops of the Molong-Wellington region of N.S.W., limestones which have hitherto been known as the “Garra Beds’. These rocks crop out in a linear tract some 60 miles in length, and up to five miles in width. This tract extends southward from the vicinity of Geurie, past Wellington and Molong, almost to Cudal (see Text-fig. 1). Matheson (1930) was the first to publish a map showing some of these limestones, but the first detailed work was done by Joplin and Culey, who (1938) published the name “ Garra Beds ”’ for the Devonian limestones and shales west and south of Molong. Basnett and Colditz (1946), in mapping the Dubbo-Wellington region, recorded a northern extension of the Beds, to the west of Wellington. Joplin and others (1952) compiled a map based on all the available information for the region of the Molong Geanticline, including work done by honours students within the University of Sydney. Finally, the southernmost outcrops of the Beds were included in the map published by Walker (1959). Palaeontological research on the abundant fossils of the Garra Beds began with the work of Etheridge jr. (1895, 1898a, 1898, 1903, 1907). Later papers, all on corals, are: Hill (1942), Hill and Jones (1940), Jones (1944) and Jones and Hill (1940). Packham (1954) described a * Present address: Department of University College, Townsville, Qld. Geology, new Hadrophyllum, Ross (1961) included four polyzoan species in her study of Australian Palaeozoic Polyzoa, and lastly Strusz (1964) described several trilobites. The present Note stems from a detailed study of the Garra Beds, and is a preliminary to several papers dealing with the taxonomy of the numerous corals collected during that study. It is proposed to designate the Beds as a Formation, consisting of a complex of limestones and detrital beds of variable calcareous content, the whole being the deposits associated with an area of reef development. It was found that outcrops presented a bewilder- ing picture of facies and thickness variation. It has not proved possible to subdivide the rocks into clearly defined units, because in most areas the outcrops are sporadic. Because of this outcrop discontinuity, in many places individual strata could not be traced around the numerous folds, nor correlated across the many faults. It is nevertheless clear that the Garra Beds are readily distinguishable from the units above and below, and can be mapped as a unit. Their designation as a formation is therefore a desirable step in the study of the stratigraphy of this part of the Tasman Geosyncline. Formal Definition LOCATION, NAME: ‘The Garra Formation takes its name from the village of Garra, on Mandagery Creek some 63 miles west of Molong (Bathurst 1:250,000 sheet SI 55-8, grid reference 171.904). The name was first applied as a reconnaissance term by Joplin and Culey 86 : Do ES SERUSZ —_-_ ----- ?-- geological boundary oot ———’?+ anticline D—<_ type section (accurate, approximate, inferred) i —_——? syncline ee oe ee eee Pm fault + zi oo railway, town <—— trend of fold axes in tightly folded strata ee Duc LBA — “HY ofod{oy ——— == _ arr rr Vo EU) 11 a 1 YW Wh Wie TA __] A ya Y yy YW Wh, LA 4 LAZA_/ TAZA . y, *Forbes Bathurst Ld BY, LATA 147° 30° General locality map, NS. 5 feet x10? ; ? NE INGTON pers SON 4 LLL = SS SESS ee leeeseilel BiGe i Locality map (inset), geological map, and diagrammatic tentative stratigraphic columns of the Garra Formation. The general areas for which the columns have been constructed are indicated. Note that much of the small-scale folding of the limestones has of necessity been omitted. 12 > STRATIGRAPHY OF DEVONIAN GARRA BEDS OF N.S.W. TERTIARY basalt Biohermal limestone Fossiliferous calcilutite calcarenite, a OY, JURASSIC sandstone Biostromal limestone Are ees late COR ates Upper DEVONIAN eee Sperry fossiliferous aie =o elope I ela calcarenite, Foo GARRA Formation (undiff.) east ie pe eee acres = Shale RS Pre-Garra strata Bog Fossiliferous calcirudite eae eae aes a Horizontal scale 1:400,000 feet x10° 10 miles \\ 0" SA sfs® Nata Rag LEEN\SS aI GGRE EE : = CUMNOCK | prem Z q roe Wh _ MM: = 4 7, le One / ae -y c—P Fic. 1 (cont.) Nh Ww 4 feet x10? [ 86 D. L. STRUSZ type section —----- 2—— geological boundary —j— ———’+ anticline D—-1 tye (accurate, approximate, inferred) 3 —?= fault SF A ently APE railway, town <4+—> trend of fold axes in tightly folded strata raat Dubbo oe Fringe i Mudgee Newcastle “Orange Forbes thurs CANBERRA En M730" 50° 52°30" General locality map, NSW. ‘blelele|e[ejofale Fic. 1 Locality map (inset), geological map, and diagrammatic tentative stratigraphic columns of the Garra The general areas for which the columns have been constructed are indicated. Note that much of the folding of the limestones has of necessity been omitted. Formation. small-scale Horizontal STRATIGRAPHY OF DEVONIAN GARRA BEDS OF N.S.W. 87 TERTIARY basalt JURASSIC sandstone Upper DEVONIAN Catombal GARRA Formation (unditf.) Pre-Garra strata scale Group 1; 400,000 0 miles Biohermal limestone Biostromal limestone Foetid, black, fossiliferous calcarenite @jed Pellet and odlite calcarenites, @.0]q algal limestone Fossiliferous calcirudite feet x10? Duc 0 5 Garra lithologies (sections only): =] Fossiliferous calcarenite, eS calcilutite “Rubbly limestone” (thinly interdedsed shale and fossiliferous calcarenite) A Sparsely fossiliferous calcarenite, FT calcilutite —] Shale =| Calcareous to non-calcareous hisniees arenites Fic. 1 (cont.) 88 Dele SLRUSZ (1938). The choice of name was unfortunate in so far as outcrops are very sparse in the vicinity of Garra, but the name has been widely used, and so is retained. Better outcrops, typical of the major lithologies of the formation, occur north of the region mapped by Joplin and Culey, for a distance of some 12 miles north from The Gap (west of Larras Lee). TYPE, SECTION: In a complex reel ‘suite such as is represented by the Garra Formation, certain reservations must be held when designat- ing a type section. The danger is that later workers will try to apply too literally the mtype * idea; for in the deposits of a reef environment, variation is so rapid and complex that any section will both include a large variety of lithologies, yet probably omit many more. Therefore it is most unlikely that any one section will be fully representative of the suite. Could the Garra Formation be divided into a large number of distinct, relatively uniform, and mappable units of small extent, then this difficulty could be resolved, but such division is apparently not possible. So it must be accepted that a “‘ type ”’ section, in the sense of a section showing the full lithological content of the formation, cannot be designated. A further, pragmatic, reason why this cannot be done is the unfortunate fact that there is no fully exposed section extending from base to top of the formation. Probably the most nearly complete section, and therefore the one here designated as the formal “ type section ”’ (with the above reserva- tions), is in a gully, a tributary to Spring Creek, about 24 miles north of The Gap (see Text-fig. 1). This section covers about a third of the forma- tion, but shows neither base nor top. The outcrops start some 100 yds. east of the road, and extend eastward through portion 53, parish of Eurimbula. The best exposures of the topmost beds of the Garra Formation are in the Wellington district, in two areas. The first is a complex biostromal layer cropping out south of the Macquarie River west of Wellington, in Oo Macquane ‘Park’, por. 103; “ph. ) Ponte: The second is a large area of massive limestone, with some biostromal layers, along the west bank of the Bell River, opposite the Wellington Caves Reserve and golf links (parish of Curra). On the basis of the close similarity of the contained faunas, the most extensive of the biostromes in the latter area is almost certainly the same horizon as that cropping out in “Macquarie Park ”’. Basal beds are exposed in a number of — localities. Typical are the outcrops in Mountain Waterhole Creek (por. 25, ph. Curra, between Curra Creek and the Wellington-Cumnock road ; Dubbo sheet SI 55-4, grid ref. 182.965). Others are: in Loombah Creek and the western part of Sawpit Gully (ph. Catombal; Dubbo sheet, grid ref. c. 176.941) ; and in por. 2, ph. Cudal (Bathurst sheet, grid ref. c. 171.887). At the last locality, there is a transition, over a thickness of some two feet, from tuffaceous sandstone belonging to the underlying formation, to a fossiliferous calcarenite at the base of Garra Formation biostromal limestone. It is highly likely that the basal beds exposed at various localities over the length of the formation vary somewhat in age, although probably deposition nowhere ceased long enough for there to be significant erosion. This con- trasts with the top of the formation, which is transected by an unconformity. LiTHoLoGiEs: The Garra Formation consists essentially of interbedded and intertonguing clastic limestones, biostromal limestones, and bioherms. The clastic beds range from very coarse calcirudites, through calcarenites, to calcilutites, and from pure calcareous rocks to non-calcareous shales and siltstones; a few thin beds of calcareous tuffaceous sandstone ~ occur near the base of the formation, and two lenses of quartzose sandstone near the top. There are also areas in which the limestones are massive beds of pellet calcarenites, odlites, and algal limestones—these are extensively developed north of the Macquarie River, and along both sides of the Bell River in the Wellington Caves region, both areas being at the northern end of the formation. The predominant lithology is _ fossiliferous calcarenite to calcilutite. Thin beds of these are frequently interbedded with lesser quantities of non-calcareous shale, forming distinctive outcrops of “ rubbly limestone ” THICKNESS: Because of the difficulties intro- duced by sporadic outcrop, together with complications from folding and extensive strike- faulting, it is possible to do no more than estimate the thickness of the formation. More- over, available evidence strongly suggests that there is considerable variation over the 60 miles of outcrop ; this of course is to be expected in a reef environment. Over the greater part of the formation, the thickness seems to be of the order of 3,000 to 4,000 feet. Some idea of the variation in estimated thickness is shown by the tentative and diagrammatic stratigraphic columns in Text-fig. 1. STRATIGRAPHY OF DEVONIAN GARRA BEDS OF N.S.W. 89 FAUNA AND AGE: Hill (1942) recognized two distinct coral faunas, one probably Coblenzian at the base of the formation, and the other Couvinian at the top of the formation, in the Mickety Mulga region west of Wellington. The more detailed mapping, and much more extensive collecting, that could be done during the author’s study have shown that this sub- division of the fauna is not tenable. Until considerably more work is done on eastern Australian faunas, an accurate age cannot be assigned to the Garra fauna, but its closest associations appear to be with the faunas of the Murrumbidgee district, near Yass, N.S.W., the faunas of the Sulcor and Loomberah lime- stones of Tamworth, N.S.W., and the Buchan fauna of Victoria, all of which have been previously regarded as Couvinian, possibly ranging down into the Emsian. Pedder (1964) has suggested that some of these may be older, perhaps Siegenian. Dr. G. M. Philip (in litt.) has noted that ‘“‘ The ammonoid evidence for the Middle Devonian age of the Buchan sequence is not unequivocal, and is amenable to the interpretation of an Upper Lower Devonian age’’. At present, it seems that the Garra Formation is either Emsian or early Couvinian, and most probably the former. CONTIGUOUS FORMATIONS: The Garra Forma- tion conformably overlies a sequence of acid to intermediate volcanic rocks and sediments, which were included by Joplin and Culey (1938, pp. 270-272) in their Manildra Beds. These and related strata are at present being studied by Mr. D. Maggs of the University of New South Wales, and Mr. N. Savage of the University of Sydney; their findings so far indicate a continuous succession from Lower Silurian strata into the Garra Formation. Overlying the formation are the ortho- quartzites at the base of the Catombal Group (see Conolly, 1963), considered to be of Late Devonian age. Joplin and Culey (1938, p. 275) considered the Catombal Group to overlie conformably the Garra Formation, but Basnett and Colditz (1946, p. 46) and later Joplin and others (1952, p. 86) proposed a broad regional unconformity. The author agrees with Dr. Conolly (1963, p. 74) that the relationship is structurally conformable in the north (there is probably a disconformity), and mildly uncon- formable near Molong (see Text-fig. 1). It is possible that near the Orange-Parkes highway in the south the relationship is again dis- conformable. See also Walker (1959, p. 45). STRUCTURE: The overall pattern of folding and faulting which has affected both the Garra Formation and its adjacent formations has been summarized by Conolly (1963); it consists of large doubly-plunging folds, cut by numerous strike and oblique faults. The poorly competent calcareous shales and thinly-bedded limestones of the Garra Formation show a considerable amount of small-scale folding and crumpling. Acknowledgements This work was carried out in the Department of Geology and Geophysics, University of Sydney, under a Sydney University Research Grant Studentship. Details of lithologies, strati- graphy, and faunal lists may be found in Strusz (1963). I would lke to express my thanks for encouragement and assistance given by Professor C. E. Marshall, Drs. G. H. Packham and T. B. H. Jenkins, and Mr. A. J. Wright, all of the University of Sydney; to Professor D. Hill, of the University of Queensland, and to Dr. J. R. Conolly, presently of the Lamont Geological Observatory. References BasnetTtT, E. M., AND Co.pitTz, M. J., 1946. General Geology of the Wellington District, N.S.W. /. Proc. Roy. Soc. N.S.W., 79 (1945), 37-47. Cono_t_y, J. R., 1968. Upper Devonian Stratigraphy and Sedimentation in the Wellington-Molong District, N-s.W. J. Proc. Roy, “Soc. NoSaz. 96, 73-106, I-III. ETHERIDGE, R., Jr., 1895. An Undescribed Coral from the Wellington Limestone, N.S. Wales. Rec. Geol. Surv. N.S.W., 4, 160-162, XXI-X XII. ETHERIDGE, R., Jr., 1898a. On a New Form of Syringopora, allied to Syringopora tabulata Van Cleve. Rec. Geol. Surv. N.S.W., 5, 149-154, XVI. ETHERIDGE, R., Jr., 18985. New or Little-known Lower Palaeozoic Gasteropoda in the Collection of the Australian Museum. Rec. Aust. Mus., 3, 71-77, XV-XVI. ETHERIDGE, R., Jr., 1903. An Unusually Large Form of Rhizophyllum lately discovered in N. S. Wales. Rec. Geol. Surv. N.S.W., 7, 232-233, 47. ETHERIDGE, R., Jr., ]907. A Monograph of Silurian and Devonian Corals of N.S.W. Part II. The Genus Tryplasma. Geol. Surv. N.S.W., Palaeont. Mem. 13, 2, ix+41-102 pp., pls. X-X XVIII. Hitt, Dorothy, 1942. Middle Palaeozoic Rugose Corals from the Wellington District, N.S.W. /. Proc. Roy. Soc. N.S.W., 76, 182-189, V-VI. Hii, D., anD JoNnEs, O. A., 1940. The Corals of the Garra Beds, Molong District, New South Wales. J. Proc. Roy. Soc. N.S.W., 74, 175-208, II-VIII. Jones, O. A., 1944. Tabulata and Heliolitida from the Wellington District, N.S.W. J. Proc. Roy. Soc. N.S.W., 77, 33-39, I. Jonres, O. A., AND Hii, D., 1940. The Heliolitidae of Australia, with a Discussion of the Morphology and Systematic Position of the Family. Proc. Roy. Soc. Qid., 51, 12, 183-215, VI-XI. 90. Dil. SURUSZ Jopiin, G. A., AND CULEY, A. G., 1938. The Geological Structure and Stratigraphy of the Molong-Manildra District, fs" Pyoc. hoy..So0c-N.S.W:,.7 2 (1937); 267-281, II. Joptin, G. A., AND OTHERS, 1952. A Note on the Stratigraphy and Structure of the Wellington- Molong-Orange-Canowindra Region. Proc. Linn. Soc. N.S.W., 77, 83-88, I. MATHESON, A. J., 1930. The Geology of the Wellington District, N.S.W., with Special Reference to the Origin of the Upper Devonian Series. J. Proc. Roy. Soc. N.S.W., 64, 171-190. PacKHAM, G. H., 1954. A New Species of Hadro- phyllum from the Garra Beds at Wellington, N:S.W. J. Proc. Roy: Soc. N.S.W., 87, 121-123. PEDDER, A. E. H., 1964. Zelolasma and _ Sulcor- phyllum gen. nov., Devonian Tetracorals from. Australia. Proc. Linn. Soc. N.S.W., 88, 3 (1963), 364-367, xix. Ross, J. R. P.; 1961. Ordovician, “Silurian and Devonian Bryozoa of Australia. Bur. Miner. Resour. Aust., Bull. 50. STRusz, D. L., 1963. Studies in the Palaeontology, Petrography and Stratigraphy of the Garra Beds. Unpublished Ph.D. thesis, Univ. of Sydney. Strusz, D. L., 1964. Devonian Trilobites from the Wellington-Molong District of New South Wales. J. Proc. Roy. Soc..N.S:We 97, 2, 919 ie WALKER, D. B., 1959. Palaeozoic Stratigraphy of the Area to the West of Borenore, N.S.W. J. Proc. Roy. Soc. N.S.W., 93, 39-46. a. Se _ OFFICERS FOR 1964- 1965 oe Le OA ORG ey Ride ON Ms es. Se if i ks Ree ; ; ? * Ay ; : j "Patrons ae ee ak i ie Rigut ont a i Dz LISLE, V.c., Pe Gens, G.6.v.0., Kst. Nis i ant ay gl A Ne a ’ ae : a ee er) a / Ws LA ae Ru hy Bt Pha , ie Mee : President PM bP ee pag a ba Bees tae : MO Wl os w. ‘HUMPHRIES, B.Sc. OPA Tiga an Ri : | Viee-Presidents, | an a i HAY SR nau Ree ti 4 a ie r ; a RAN a WWE. H. es POGGENDORFF, B.StAgt, a Ga ee Ne havin W. 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Journal and Proceedings, Royal Society of New South Wales, Vol. 98, pp. 91-100, 1965 The Foundations of the Geological Survey of New South Wales ANN MOZLEY Adolph Basser Library, Australian Academy of Science, Canberra ABSTRACT—The background of events leading to the appointment of the first geological surveyor in New South Wales is traced with an account of the pioneering survey work carried out by Samuel Stutchbury and the Rev. W. B. Clarke which laid the foundations of geological survey in New South Wales. Australia had been settled for over sixty years before the attention of the British Government was seriously called to the need for a government-sponsored geological survey in the eastern colonies. Adolarious Humphrey, it was true, had been appointed mineralogist to the Territories of New South Wales by the Home Government in 1803 and sailed with David Collins to plant a new settlement on the southern coast. But Humphrey gave little mineralogical service in New South Wales. When the settlement at Port Phillip foundered, he transferred with the party to Van Diemen’s Land, and it was here that most of his geological investigation was made. No reports, however, commemorate his work and it was evidently with some relief that he resigned his lonely scientific post in 1812 and became a magistrate. Britain had established her Geological Survey in 1835, Canada in 1842, while the small Colony of Newfoundland enjoyed the services of a geological surveyor from 1839-41. In America by the same period, geological surveys had been independently launched in at least fifteen of her States.2. In Australia, however, the climate of colonial opinion was unfavourable to expenditure on science. ‘‘ Zoology, Mineralogy, and Astronomy, and Botany, and _ other sciences ’’ declared one Sydney newspaper in 1833 “are all very good things, but we have no great opinion of an infantile people being taxed to promote them. An infant Colony cannot afford to become scientific for the benefit of mankind.’? As one eminent citizen per- tinently summed up the philistine spirit of the time: “ The only animals whose natural history it is deemed of consequence to investigate in New South Wales are the sheep and the bull ”’, and the only branch of study that has hitherto engrossed the pursuit of all classes is, “ how to make the most of it’’* By the decade of the forties, however, the zeal of a handful of scientific men had revealed A encouraging evidence of the Colony’s mineral wealth. Paul Edmund Strzelecki, visiting Polish explorer, in 1839 found particles of gold in the Vale of Clydd, while the Cambridge trained geologist, the Rev. W. B. Clarke, searching with his hammer among the granite and the quartz- iferous slates of the Great Dividing Range, discovered traces of the metal near Hartley in 1841. Clarke communicated the news to his friends and began enthusiastic prediction of the Colony’s potential wealth. He drew the attention of the Legislature to his finds,® and in April 1844 called upon the Governor, Sir George Gipps, with some gold speckled specimens of rock found a month earlier on the banks of the River Page. His visit, the clergyman reported later, caused the agitated Governor of a convict settlement to exclaim, “ Put it away Mr. Clarke or we shall all have our throats cut ’’® which schoolboys have relished for over a hundred years. But Clarke did not put his gold away nor desist in his predictions of wealth, and evidence suggests that it was less fear than apathy that held back an official mineralogical search. For Clarke’s opinion coloured the thinking of another active cleric, the Rev. Dr. John Dunmore Lang, who moved in the Legislative Council in August 1845 that a sum be placed on the estimates for the commencement of a geological survey in New South Wales. The motion was rejected by fifteen votes to ten, eight who voted against the measure, Lang noted, being paid officials or crown nominees. ‘“‘ Had this useless lumber not interfered to clog the wheels of the legislature’’, Lang reflected acidly, “this important measure should have been carried by a majority of three. As a consequence gold might have been discovered in New South Wales before it was found in California.’’? It was Strzelecki, in his pioneering work on Australian physiography, who first directed British attention to the importance of a 92 Ara e: ~ ANN MOZLEY geological survey of New South Wales and Van Dieman’s Land. Although his own strange verdict, after travelling some seven thousand miles on foot and horseback, claimed that “the scarcity of minerals was such as might have discouraged the most ardent and persever- ing mineralogist who had ever devoted himself to science ’’,® he pressed the needs for a govern- ment financed survey’ ‘conducted on liberal principles to hasten the pastoral and agricultural destinies of the eastern colonies, in which he profoundly believed, and to throw scientific light on the geological analogies of Australia with the rest of the world. The Polish ‘‘ Count ”’, with influential friends in London, was well placed to promote such a plan, and in June 1845 he wrote encouragingly {o"his’ Syditey ‘friend;“Captain P,P, Kine There is great probability that I should be able to secure to the two Colonies a Government Establishment called the Economic Geology, which will be a branch of the office of the Ordnance Geological Survey of Great Britain under the direction of Sir Henry de la Beche—with a Geologist and a Chemist and through which a thorough Geological Survey of the two Colonies will be made and such questions of chemistry and mineralogy solved, as the developments of mining and agriculture may require. 9 In England Roderick Murchison, active and illustrious geologist, interested himself in Strzelecki’s work, and the resemblances he discerned between the explorer’s specimens brought from the Great Dividing Range and those of the gold-bearing Ural chain, from which he had lately returned, led him to make positive predictions of Australia’s auriferous wealth,’ and, as news of gold began to trickle back to London," to urge upon the Secretary of State the desirability of instituting a mineralogical search.!2 While the British Government remained unresponsive to these pressures, the spread of speculative mining in the Colonies and the warning of experienced scientists of the dangers and waste of unregulated mining activity in Australia directed a more immediate interest to the rocks that lay beneath the pastoral soil. “ Thousands of pounds will probably be thrown away by misdirected efforts ’’ counselled the visiting geologist J. Beete Jukes, “which a mere outline survey of the districts, conducted on sound principles would direct into proper channels’’ and from his own experience as former geological surveyor of Newfoundland, he urged that “positive and direct benefits could hardly fail to result from a good survey, not only to the mining interests, but also to the agricultural, the engineering, and all other operations connected with the soil and with the recks below it .™ By the beginning of 1849, the Colonial Government was ready to proceed on such advice. | Subsequent interpretations of the history of gold in Australia were to attribute to the Californian discoveries an undue influence in shaping Government policy in New South Wales. The pressures, however, came from nearer home. The successful development of the copper mines in South Australia; the appearance of the ore in New South Wales at Carcoar, Molong and Bathurst; the discovery of iron ore at Berrima and of copper and lead at Yass, and the many unconfirmed reports that gold had been found in several places across the mountains prompted the Government to act and on 1 March 1849, the Governor, Sir Charles FitzRoy, addressed a despatch to the Secretary of State for the Colonies requesting the appointment of a Geological Surveyor to New South Wales. I am desirous of bringing under your Lordship’s notice [wrote FitzRoy] the expediency of causing a Mineral and Geological Survey to be made of the Colony in order to determine the mineral resources which it may possess. . . I have thought it necessary to trouble your Lordship in order to show the probability that if the country were examined by a competent Geologist who would be at liberty to devote his time exclusively to this object, valuable metalliferous ores would be dis- covered, which would not fail to add greatly to the resources of the Colony, extensively to benefit the Land Fund, and thus to open out a new field for British Emigra- ‘tion. . .The information thus obtained would, there is little doubt, he found highly valuable both in an economic and scientific point of view.14 Samuel Stutchbury The task of selecting a well-qualified geologist was entrusted to the Director of the British Geological Survey, Sir Henry de la Beche. He offered it to the experienced J. B. Jukes, then a member of his own Survey. “I hesitated a little before I declined it ’’, Jukes confided to his friend W. B. Clarke, ‘‘ I should have enjoyed FOUNDATIONS OF GEOLOGICAL SURVEY OF NEW SOUTH WALES 93 it much—but I have had some experience of colonial appointments, and have little faith in their permanency.”!>, H. W. Bristow, another member of the British Survey, was next approached, but resigned for family reasons, aortly before he was due to sail for the Colony. as a Coal Viewer, and is perfectly acquainted not only with Mineralogy as a science, but also practically with the mode of. occurrence of the ores of the useful metals.’’!6 : Expectations of the new geological surveyor were less sanguine in New South Wales. “ It Samuel Stutchbury, first Government Geological Surveyor to New South Wales. A harried Binector enpacel Samuel Stutchbury, Curator of the British Philosophical Institute, in May 1850 and committed him without delay to a free passage to Australia. A man, “ well instructed in our mode of work on the Geological Survey of Great Britain’, de la Beche assured the Governor, Stutchbury had “ great experience By courtesy of the Mitchell Library. is understood’”’, a Sydney Morning Herald editorial announced on November 4th, a fortnight before Stutchbury landed, “that a naturalist of some eminence, Curator of a Museum in England, is to come out; but it 1s very unlikely that that gentleman will feel himself ready to undertake a geological survey, 94 ANN MOZLEY though highly useful as an observer and collector.” The writer was the Rev. W. B. Clarke, scientific doyen of the Colony and since 1839 “cock of the geological walk’’. After many years of private geologizing in the Colony, Clarke hoped to publish his researches with government aid; he had not been conspicuous among those who had pressed for an official geological survey of New South Wales,!’ and he fretted keenly at the choice of one whose qualification for this arduous undertaking appeared to be long service in the sanctuary of a Bristol museum and the publication of a paper on the growth of young corals of the genus Fungia. His critical comment, under the shadow of anonymity, left little doubt among the knowing, of his own aspiration to the post. “There might perhaps have been found in the colony ”’, he concluded pointedly, “ the means of carrying out the desires of the Government without going further and faring worse; but is is certain that, for some time to come, the colony must be content to wait for anything more official than the zeal and intelligence that volunteer services may supply.”’ Samuel Stutchbury, a quiet and conventional Englishman about whom little is known before his acceptance of the geological surveyorship carried him to an unenthusiastic reception in New South Wales, arrived in Sydney on 16th November 1850. His appointment, he found, was not regarded as a permanent one, though it was considered not unlikely “that it may extend over a period of several years’’. His salary was £600 a year. After four months at sea, he was eager to take up his task, proceeding as his letter of appointment urged to districts where metalliferous ores had been found, and advising the Government in quarterly reports of the range of the mineral areas. The Governor's absence at Bathurst, however, obliged Stutchbury to wait and it was not until 18th February 1851 that he set off with a dray and two servants to begin his methodical survey of the Colony at the Bathurst copper mines. It was just three weeks before Edward Hargraves, newly returned from California, was to ride up the same path to the mountains ; and only a few weeks more before that talented adventurer was to dazzle the Colonial Secretary with his showman’s confidence and his tiny particles of gold. From his camp at the Bathurst Cornish settlement Stutchbury noted in his diary on 3rd March “ There can be no doubt that the whole of these ranges are highly metalliferous ’’.1® It was indeed, as he advised the Colonial Secretary in April, what in his own part of the west of England would be called “‘a kindly sort of country ’’.19 From the Government viewpoint, however, such information was already too late. Hargraves had cradled the tich alluvial gold of Lewis Ponds and, presenting the Government with an ultimatum that April, had destroyed all prospect of orderly mining development in New South Wales. Just how kindly the ranges had proved, Stutchbury learnt from a newspaper in Carcoar on 4th May, and six days later he received directions from the Colonial Secretary that the successful prospector was on his way to consult him in reference to the discovery. From that day, the geological surveyor’s role became a secondary one. He met Hargraves at Coombing on 10th May and saw his four ounces of gold. Four days later they met again to ride to Lewis Ponds, where several parties were already digging for gold. Stutchbury reported to the waiting Government the existence of grain gold, but it was not until his fuller report from Ophir on 19th May that “gold had been found in_ considerable quantity. . .I have found it far above the high flood line of the Creek in various places, proving it to originate in the mountains, and washed down by the rain ’° that the Adminis- tration stirred and, frustrated in their hopes for a regulated mineral survey, made public the news that would release the flood of diggers across the Dividing Range. W. B. Clarke In this unexpected emergency in the affairs of the Geological Survey, the chief adviser to the Government was not the accredited surveyor, Mr. Stutchbury, but the Colony’s geological savant, the Rev. W. B. Clarke. ‘‘ We were in frequent communications with him’”’, Deas Thomson recalled some years later, “for he was considered a great authority, and he was very kind in giving information to the Govern- ment that was useful to it’’.24_ Clarke offered his services voluntarily to the Government in May and from his own fieldwork and extended study listed the areas in the north and south of the Colony where gold might be found. It was Clarke who drafted the revised instructions sent to Samuel Stutchbury and Sir Thomas Mitchell, the Surveyor-General (recruited to conduct a survey from Canobolas to the north) on 21st May defining the geological data to be sought in connection with gold, and who appeared like an eminence gris in the Colonial FOUNDATIONS OF GEOLOGICAL SURVEY OF NEW SOUTH WALES 95 Secretary’s office early in June when Hargraves himself was called to receive instructions as Commissioner of Crown Lands, and wrote down at Deas Thomson’s request the scientific sign- posts to the location of gold.” In the event, Hargraves never again discovered fresh sources of gold, though he remained in the employment of the Government for several years. ordinating board. But to this proposition, the pioneering geologist flatly declined to accede. ‘““ When you consider ”’, he wrote Deas Thomson on 7th July 1851, that I have been at work unassisted in any way for 12 years, that I have nearly finished a survey of the whole country, and that it is my wish to complete it by myself, Rev. W. B. Clarke, c. 1851. Clarke’s opportunity to serve the Government and to put his own theories to the test of fieldwork came later in the year. In July he discussed with the Governor and the Colonial Secretary a plan to extend the gold survey systematically throughout New South Wales. It was the Government’s intention to sponsor a joint survey conducted by the two geologists Clarke and Stutchbury reporting to a co- By courtesy of the Bassey Library. you will see at once how completely opposed it will be to my design and desire to be bound and shackled by those who will not keep pace with me, and whom I must either work for, or yield to, often perhaps against my own conclusions. . . With an able practical geologist who has really acquired his experience in the field I should be glad to work in company, but 96 VL DNAS oe / as this cannot be. . . can only in common justice to myself and what is expected of ‘me, offer my _ services unfettered by connection with others. With a Government not entirely satisfied with its own geological surveyor, Clarke’s point prevailed, and on 11th July Stutchbury was advised to ‘“‘ proceed with the general Geological Survey’ according to instructions received before the gold discoveries had interrupted his work. The more pressing matter of the gold survey was entrusted to Clarke alone and at the beginning of September this enterprising clergy- man was added to the Colonial Estimates as a geological surveyor at a salary (fixed to remunerate him for the loss of his clerical stipend) of £300 a year. Eleven days later, he rode off from his rectory at Saint Thomas’, North Sydney, with a cart and two servants assigned by the Government and with cradle, picks and prospecting pans, to begin his survey in the south. With him he carried his Bishop’s blessing, and a licence in his pocket to minister God’s word and His eternal riches as he searched the earth for the evidence of gold. W. B. Clarke was engaged for nine months on a survey of the southern goldfield which took him from Marulan south-west to Tumut and Kosciusko, south to the sources of the Snowy and the Bendoc Rivers, east to Cape Howe and Pambula, and inland by way of Monaro to complete his examination of the country where he began," upon, a ‘field of gold’ ”’. His eighteen reports written in camp at the end of an arduous day present a strikingly co-ordinated picture of the physiography and structure of this broken region of uplift, igneous intrusion and trappean?4 overflow; and _ his generalizations on its stratigraphy have stood the test of later detailed research. From his starting point on the Shoalhaven, Clarke carried his earlier identification of the carboniferous formation of the Colony to its outliers between Marulan and Goulburn, where it passed into the older sedimentary rocks and made positive identification of the palaeozoic basis of southern New South Wales. At Molonglo and. the Limestone Plains, he observed the Silurian formation “distinctly marked by alternations of beds. . . and by abundance of fossils that leave no doubt as to its geological epoch ’’,?° and he traced the same alternations and succession in the rocks to Queanbeyan, along the Murrumbidgee, to the Colony’s southern heights. Despite a comparative absence of fossil evidence, his determination of ANN MOZLEY the Devonian strata was equally | precise; fossils discovered in the ranges between Yass. and the Murrumbidgee he assigned to this epoch, and he tentatively placed the grits and sandstone of Pambula in the county of Auckland in the Devonian system.?® . In 1851-2, therefore, his able stratigraphic identifications in the southern districts were sufficiently firm to dispel the suspicion long entertained in geological circles in England that Australia was of recent geological age. Although the information obtained may not be sufficient to arrange the Australian succession in intimate analogy with the succession in Europe, [Clarke wrote from Eden in March 1852] I nevertheless desire to record in this place my conviction, that the general order of succession appears to be so far certain, that further enquiries will be conducted with less difficulty than heretofore. . . The existence of the fossils of the Silurian system, and, as I believe, also. the. existence ..{ ,of; a formation analogous to, if not identical with, some portion of the Devonian system of Europe, have been made out. . . These facts and inferences are important, as they demon- strate unequivocally that the greater portion of New South Wales is occupied by Palaeozoic formations of the older class, and that, therefore, it is one of the oldest countries on the face of the globe.?? Clarke was also to note down on this expedition the first evidence of glacial phenomena in Australia at Kosciusko; and less than a decade after Agassiz’s controversial theory of glacial action had been adopted by European scientists, he observed “ Probably in earlier times glaciers did form ; for I saw more than one unmistakable bloc perché, a mass resting on upturned strata ’’.?8 Against this background of geological enquiry he reported to the Government no less than ninety-five productive areas of gold and ended his survey with the confident assertion that gold was distributed though in variable quantities over a region of some 16,000 square miles south of the parallel of Marulan, excepting only the three eastern counties of St. Vincent, Dampier and Auckland. Lead, copper and iron, he believed, would also be found in the county of Murray. In his search for geological constants in the location of gold, Clarke demonstrated that the metal was to be found in southern New South Wales in certain granites, notably hornblende?? ; in the older sedimentary rocks where quartz was common and where river channels dissected FOUNDATIONS OF GEOLOGICAL SURVEY OF NEW SOUTH WALES 97 the meridional line of strike®®; in regions of igneous and metamorphic activity, and, importantly, in connection with trap.*! His evidence, collected over large tracts of auriferous country, attested also to the astonishing variableness of gold in matrix which he had found in quartz veins, ironstone, sandstone and. conglomerates of different epochs. The whole history of the origin of gold the geologist concluded “‘ rested on a more perfect under- standing of the natural history of trappean eruptions ’’? and, at a time when few English geologists had interested themselves in the theory of ore deposits,*? Clarke’s detailed and careful findings from the Australian goldfields were an important contribution to this enquiry. The pioneering geologist also brought evidence from his own fieldwork to bear on Roderick Murchison’s keenly held theory that altitude was an essential corollary to quantity in gold. Clarke had sought the metal in vain in the summit of Kosciusko, finding it rather in the granite at a much lower level in the range he named Muniong, and, in general, most prolifically at a level of 2000 feet; and ardent contro- versialist as he was on this subject, he wrote jubilantly to the Colonial Secretary: “I am glad, if, for no other reason, I have been able to carry a cradle, prospecting pan, pick and shovel, over some of the highest peaks of the continent, and up and down the faces of generally precipitous mountains, the planes of the slope of which are. . . perfect escarpments.’’34 Clarke’s penetrating reports of the southern goldfields, blending observation with theory and seasoned with a practical good sense that was to make them invaluable guides to prospectors when he published them in book form in 1860, were printed as they came to hand, as parliamentary papers, and won high praise from the Government. The Colonial Secretary wrote while Clarke was still in the field to convey the Governor General’s satis- faction with the “ able and scientific manner ”’ in which Clarke had carried out so large and complex a survey, and to express the hope that he might be spared from his spiritual duties to carry the investigation to other parts.® Samuel Stutchbury, meanwhile, had resumed his survey from Bathurst to the north. After his first communications to the Government on the gold discovery, “meagre and unsatis- factory and particularly unscientific and unbusinesslike ’’ a critical administration had described them,?* he had settled into his stride and his ten reports on the present State of New South Wales gain in competence and confidence as he moved northward. In July, he notified the discovery of copper at Canobolas and of rich iron ore at Coombing Park, which he considered, “if all things also were com- patible. . .is sufficient to supply another Sheffield for ages to come ’’.27 His 6th Report describes the coal beds at Dubbo; his 8th the coal fields of Talbragar, and he was to carry these detailed examinations of the carbonaceous formations to the Darling Downs. From the outset of his appointment, however, Stutchbury suffered from a very real sense of isolation in his work, and his personal diary, preserved in the Mitchell Library, bears witness to the loneliness of his private struggle and of his determination to fulfil the terms of the undertaking to which he was pledged. “I may take this opportunity’ he wrote down after some eighteen months in the Colony, “‘of recording my feelings of disappointment and pain at the general treatment I have met with from the Colonial Government from the moment of entering upon the duties of my survey until the present time. Arrived, a stranger in this country, unacquainted with the peculiar requisites for a lengthened sojourn in the Australian ‘bush’; a never ending journey, not alone from township to township, but not infrequently beyond the boundaries of settlement and civilization, I was left almost entirely to my own resources, and did not receive the aid and assistance which I think I was entitled to look for and expect.’’38 Stutchbury criticized in particular the lack of assistance for carrying out his task, and he notes that from his own pocket he paid the wages of an extra servant and a native boy so that no reflection should fall on those friends in England who had helped him to the post.39 It was a serious indictment of the Government, yet the blame was not all on one side. Stutch- bury’s limited experience of fieldwork and his ignorance of the rough conditions of life in Australia left him particularly exposed, and his plight was not eased by the contrast which Clarke’s single-handed and enterprising efforts afforded in the south. ‘‘ You could not have a better foil ’’, wrote Captain P. P. King, charged with the task of editing the reports of the geological surveyors, to Clarke in February 1852 ; and this view of Stutchbury was widely shared. Overshadowed by the pioneering geologist, and cut off throughout his period of service from personal contact with the administrators, Stutchbury, despite the competence of much of his work, never succeeded in winning the confidence of the Government. 98 ANN MOZLEY His few communications with Clarke moreover reveal the distrust and rivalry which lay, not surprisingly, close to the surface in the relation- ship of the two geological surveyors in New South Wales. After three months in his parish Clarke, in September 1852, was again in the field, converging towards Stutchbury in the north. “I thought I was working my way up (geologically) towards the Hunter River beds ”’, Stutchbury wrote him tartly in December,” “and I intended going to Mt. Wingen, and then crossing to New England on the route which I now find you have taken up.”’ He was critical of specimens Clarke had sent him, which he found “so small and indistinct as to be scarcely distinguishable ’’, a criticism, in fact, often levelled at the pioneering geologist. The clergyman, for his part, kindly in all matters where scientific reputations were not involved, had sent Stutchbury a prescription for an ailment that had long hung on. “I have too much faith in my own knowledge of medicines ”’, Stutchbury replied somewhat darkly to this overture, “to take any remedy without being acquainted with its component parts!” Six weeks later, however, he acknowledged its success. Yet little friendliness prevailed. “ If it is not impertinent ’’, he enquired of Clarke in February 1853, “I should lke to know the route you have made and your intended course.” Clarke’s answers, unfortunately, have not been preserved. Clarke spent nine months in northern New South Wales and submitted ten reports to the Government. He examined the diggings at Hanging Rock and the Bingara gold fields, tracing the gold drifts over considerable areas of New England. He pronounced it “local gold’, suggesting that its first dispersion was brought about by the waters of the ocean during one of the oscillations in the vertical ascents and descents of the cordillera. “It will be seen at a glance ’’, he wrote accordingly from Tamworth in December 1852, “‘ that he who would limit his idea of the wealth of our hills and valleys to what has been produced from such scratches and furrows as our Golddiggers have hitherto contented themselves with making, or who would dogmatically and presumptuously say that the Gold fields are limited to what can be scanned with the eye alone, has yet to learn very much. 2°. The more Isee oli the) backbone of this Continent, the more I am impressed with the high probability of the extension of the Gold fields far beyond the present lmits of Seancii.ic* In November 1852, he reported the existence of oxide of tin with tourmaline near Dundee and in Paradise Creek, a tributary of the McIntyre (he had recorded it earlier in the southern Alps), and noted the probability that the ore would be found plentifully distributed in the alluvia of other tracts, “‘ as I have found it amidst the spinelle, rubies, oriental emeralds, sapphires and other gems of the detritus from granite*’’’; anticipations abundantly realized when the rush to the New England tin mines broke in 1872. In his most elaborate and thoughtful report from the northern districts, written from the Severn River in May 1853, Clarke set down some pioneering observations on the structure and origins of the highlands of New England on which the first detailed surveys by Wilkinson, David and Andrews were laid. He found the solid nucleus of New England, the Upper Clarence districts, and part of Gwydir and Liverpool Plain was granite of some kind, some “of the oldest formation ’’, while “ bursting through both granite and porphyry and over- flowing them, basalts, amygdaloids, and small proportion of greenstone, form a third kind of igneous rock’. These formed the culminating point of the Dividing Range on the Ben Lomond Range, breaking out along the spurs in various places on the western falls. The period of this overflow, Clarke attributed to “ posterior to the carboniferous formation ’’.*% In his Northern reports, Clarke also followed the beds of the carbonaceous formations of the Colony from the coastal deposits of the Hunter, the basins of the Karau, Gloucester, Clarence and Richmond Rivers to the western coalfields and thence to Darling Downs and Moreton Bay ; assigning them all, at this time, to a palaeozoic age. His tenth report took him to southern Queensland, where he described the basin of the Condamine, the Darling Downs and Moreton Bay, exploratory work to which Jack and Etheridge paid tribute in their classic work on the geology and_ palaeontology of Queensland.*4 Clarke completed his survey in June 1853, and returned to his parish in Sydney. “ My labours ’’, he replied to the thanks of a grateful Government, ‘“‘ were nothing compared with what geology must do hereafter.” Yet he had, geologically, cut a swathe through the entire eastern sector of New South Wales and offered explicit evidence of the varied metal and coal resources of the Colony. Samuel Stutchbury, following Clarke into Queensland in October 1853, was to carry the FOUNDATIONS OF GEOLOGICAL SURVEY OF NEW SOUTH WALES 99 exploratory reconnaissance northwards, and, in his last two years in Australia, to set down. the pioneering foundations of geological survey in Queensland (separated from New South Wales in 1859). Writing of Stutchbury’s contribution a century later, Professor W. H. Bryan nominates the surveyors twelfth report from South Brisbane as the most “ significant and interesting’ on that State. Init, Bryan recounts,*® Stutchbury described that are now known as the Capalaba Conglomerates, reported on the working of the coal measures near Mogill ; noted the limestones and Ipswich tracing them south for some eleven miles; observed the evidence of recent uplift on the shores of Peel Island and named several of the recent corals so exposed. Moving northwards, he was to determine that a basal series of Silurian or older schists and slates was followed in geological succession by a series of fossiliferous limestones of Devonian age, and that these were succeeded by the coal measures, which, like Clarke, he assigned to the Carbon- iferous age. Stutchbury’s sixteenth and last report was written from Port Curtis on 20th November 1855, and submitting it, this reticent field geologist sums up something of his own sustained contribution to the geology of both New South Wales and Queensland. “If the maps accompanying my reports are put together ”’, he advised the Colonial Secretary, “it will be found that the area coloured occupies an extent from south to north exceeding eight hundred and fifty miles, with an east to west average breadth of thirty eight miles, thus making a total over 32,000 square miles by traverse work; and I have much confidence it will be found closely approximating to the truth.’’46 Eleven days later, on 1st December 1855, Stutchbury was on a ship for England. No newspaper noticed his departure nor marked his five years of uninterrupted field work in the Colony; and he readily became one of the forgotten men of Australian science. It was, however, the once critical Clarke who paid public tribute to Stutchbury after his death, when he gave evidence before a Select Committee in 1861. “Mr. Stutchbury has done his part for the neighbouring Colony of Queensland ’’, he then conceded, ‘‘as has Mr. Selwyn for the Colony of Victoria, and myself for New South Wales.’’47 Samuel Stutchbury’s resignation brought to an end the official geological survey of New South Wales. The new Governor-General, Sir William Denison, an enlightened friend to science, had private hopes of promoting “‘a proper survey of the Colony ” into which all available know- ledge of the country should be poured; “ yet how difficult it is’, he confided to Sir Roderick Murchison in 1855 while Stutchbury was still in the field, “‘ to persuade either individuals or governments, that it is both cheaper and better to do a thing well at once, than to act upon the principle that everything is good enough for the infancy and early life of the colony ’’.48 His words were curiously prophetic. Clarke's reports, together with Stutchbury’s, were shelved by the Administration, and his determinations on the Colony’s mineral wealth exerted no real influence on the mining policy of the Government. Indeed, as one angry miner protested publicly in 1861, “ The Government have not,. . . and never had, a mining policy. They have been actuated throughout by a blind empiricism, and a thriftless expediency. It is seen alike in their treatment of the geologist (the Rev. W. B. Clarke), and in their shelving of his reports, and in their utter ignorance of the present wants of the mining population.’’49 It was not until 1873, seventeen years after Stutchbury’s departure from the Colony, that the incontestable evidence of the Colony’s mineral resources with the rush to the New England tin mines at Tingha, Inverell and Glen Innes, forced the Government to act and a Department of Mines was established that year. In1874C.S. Wilkinson, a former member of Selwyn’s team on the Victorian Geological Survey, was nominated geological surveyor and, the following year, was placed in charge of a separate branch of the Survey Branch of the Mines Department. In the long intervening years, however, it was the clergyman geologist William Branwhite Clarke who, declining the appointments of geological surveyor in Queensland, Tasmania and New Zealand, continued from his own private researches and at his own expense to advance the knowledge of the Colony’s strati- graphy and palaeontology. In this _ period Clarke, in effect, filled the place of an official geological survey, conducting a correspondence with scientists and prospectors that might well have proved daunting to a government depart- ment; assembling collections of specimens from all parts of Australia ; filling the cabinets of the Cambridge Woodwardian Museum, the Geological Society of London and the Australian Museum ; and acting as a source of consultation and exchange for the growing regiment of geological surveyors in the other Colonies. Clarke’s major work Remarks on the Sedimentary 100 Formations of New South Wales reached its fourth edition in 1878, the year the pioneering geologist died, and two years later the accumu- lated details of his long and voluntary service to geology in the Colony formed the basis of the first geological map of New South Wales issued by the Mines Department. On these pioneering foundations, the systematic work of the permanent Geological Survey of New South Wales has been soundly laid. References* 1 Hist. Rec. N.S.W., 1803-5, p. 47, and Australian Dictionary of Biography, A.N.U., Canberra. 2,W. B. Hendrickson, ‘‘ Nineteenth Century State Geological Surveys : Early Government Support of Science ’’, Jszs, 1961, 52, p. 361. 3 Sydney Monitor, 20 July 1833, editorial. 4John Dunmore Lang, A Historical and Statistical Account of New South Wales (Lond. 1834), p. 183. 5 W. B. Clarke, Researches in the Southern Gold Fields of New South Wales (Syd. 1860), p. 290. 8 Niuwo.W.., Lee. Ass. Votes G Proc. 1861,, 2: Select Committee on the Claims of the Rev. W. B. Clarke, p. 1165. 7 John Dunmore Lang. Chiefly Autobiographical A799. 10 1878»... ~Ed.«.Archibald Gilchrist (1951), Vol. 1, p. 360. 8 P. E. Strzelecki, Physical Description of New South Wales and Van Diemen’s Land (Lond. 1845), po sol. ®5 June 1845. King Papers. Mitchell Library. 10To the Royal Geographical Society of London in 1844 and to the Royal Geographical Society of Cornwall in 1846. 11 At least two experienced prospectors in New South Wales, William Smith and Thomas Chapman, sent gold samples to Murchison during 1847 and 1848. 12 Letter to Earl Grey 5 Nov. 1848. N.S.W. Leg. Coun. V. & P. 1853, 2. Discovery of Gold in Australia. Sir R. Murchison’s Claim. Enclos. I. 13 Tas. Jour. Nat. Sci. 1846, 2, p. 12. a Neo. Wa Lee. Coun, Ve Po) W815, 22. Relative to Geological Survey No. l. 1520 Feb. 1850. W. B. Clarke Papers, Library. 1626 April 1850. Papers Rel. op. cit., Enclos. 3 in No. 3. Lethbridge Collection. Papers Mitchell Geological Survey, * Acknowledgement is made to the Trustees of the Mitchell Library, Public Library of New South Wales, for permission to quote from the manuscript papers in their keeping. ANN MOZLEY 17 Professor Tate in his valuable survey ‘‘ A Century of Geological Progress’’, ANZAAS, 1893, V, attributes a substantial influence to Clarke in establishing the survey in N.S.W., and this view has been perpetuated by other writers. The evidence of Clarke’s own papers and press cuttings, however, does not support it. 18 Diary of a Geological and Mineralogical Survey of New South Wales, 1850-1855. MS Mitchell Library, p. 92. 19 Papers Rel. Geological Survey, op. cit., No. 21. First Report to the Government 12 April 1851. 20 Tbids. «Nor 1 2. 21 N.S.W. Leg. Ass. V. & P. 1861, 2. Select Com- mittee on the Claims of the Rev. W. B. Clarke, pag. 1190. 22 Papers Rel. Geological Survey, op. cit., No. 32. Colonial Secretary to E. Hargreaves, 10 June 1851. 23 Report XVII, 1 June 1852. searches, op. cit., p. 242. 24 T have used Clarke’s description “‘ trap ’’ throughout. It included basalt, greenstone, phonolite, and amygdaloids of various kinds. 25 Report IV, 10 Nov. 1851, Researches, op. cit., p. 73. 26 Report XI, Part 1, 6 Mar. 1852, ibid., p. 196. AtEDIC,, De kG te 48 Ibid., p. 225. *9 Report III, 21 Oct. 1851, Researches, op. cit., p. 32. 30 Report IV, 10 Nov. 1851, ibid., p. 69. $1 Report XI, Part 1, 6 Mar. 1852 \ibid pa 72. S27 bid. 33 Cf. T. Crook, History of the Theory of Ore Deposits (Lond. 1955), p. 565 ff. 34 Report VII Jindebein, 24 December 1851, Researches, Op: Clt., Pp. s30: 35 Letters to Clarke 13 March and 19 April 1852, Researches, op. cit., p. 212 fn. 36 Colonial Secretary to Stutchbury 26 May 1851. Papers Rel. Geological Survey, N.S.W. Leg. Coun. V. & P. 1851, 2. 37 Ibid. Stutchbury Second Report 18 July 1851. 38 Diary of a Geological and Mineralogical Survey, op. cit., 1 May 1852, p. 317-8. 39 Tbid., p. 320. 40'W. B. Clarke Papers, 20 December 1852. 41 Report III Papers Rel. Geological Survey, N.S.W. Leg. Coun. 1852, 2. 42 Report IV, 30 Nov. 1852, ibid. 48 Report VIII, 7 May 1853, N.S.W. Leg. Ass. V. & P. 1872-3, 2, p. 1038-9 and 1040. 44 Geology and Palaeontology of Queensland and New Guinea (1892). 45 “ Samuel Stutchbury and some of those who followed him ’’, Qld. Govt. Mining Jour., LV, Aug. 1954, p. 642. 46N.S.W. Leg. Coun. V. & P. 1855, 1. 47 Select Committee on the Claims of the Rev. W. B. Clarke, N.S.W. Leg. Assembly V. & P. 1861, 2, pag. 1181. 48 Varieties of Vice Regal Life (1870), Vol. 1, p. 309. 49 Sydney Morning Herald, 9 Sept. 1861. Reproduced in Re- Journal and Proceedings, Royal Society of New South Wales,-Vol. 98, pp. 101-104, 1965 Radioactive Laterites in the National Park Area I. A. MuMME Introduction During the last two years, the writer has been conducting a programme of measurement of normal gamma radiation intensities from various geological units exposed in the Sydney Basin. These determinations were made along several hundreds of miles of traverses with an aerial scintillometer set up in a vehicle. While conducting measurements of gamma-ray activity in the National Park area, the nodular lateritic masses covering the Hawkesbury sand- stone were found to be weakly radioactive. Gamma-ray spectrometry measurements showed that the radioactivity was mainly due to thorium series with a small contribution from radium C. Purpose of the Gamma-ray Measurements The purpose of this survey was twofold, namely (1) to determine the actual levels of radio- activity occurring in the general Sydney area, and (2) to determine whether or not it was possible to discriminate between the characteristic levels of radioactivity associated with the different geological formations. Type of Instrument Used The scintillation counter used was built by Canadian Atomic Energy Pty. Ltd., and included two 3” x4” sodium iodide gamma-ray detectors and associated electrical circuits, and indicators. The detecting elements of sodium iodide (activated by thallium) scintillate under irradiation by gamma-rays. This equipment is quite portable and because of its high sensitivity and short response time measurements could be carried out at a reason- able speed. A conventional vibrator type power unit was used to provide the necessary 115 volts A.C. for the instrument from a 12 volt D.C. battery system. A recorder was used to record the variations in radioactivity as measured by the counting rate- meter during the traversing. Calibration The measurements of gamma-ray intensity were expressed in absolute units using a radium standard, and applying the equation Dose rate (in milliroentgens/hour) = 0-84 x mec d2 where mc=the source strength in millicuries, and d=the distance in metres. Corrections for Cosmic Rays As it was necessary to subtract the effect of the cosmic rays to determine the intensities of the gamma-radiation from the various types of rock, reasonably accurate determinations of the effect of the cosmic rays had to be made. This was done by reading the instrument in a boat in Botany Bay at a distance of over a mile from the shore. Interpretation of Radioactivity Records While interpreting the radioactivity records and computing the levels of radioactivity for the various geological units traversed, anomalous readings were located which were significantly larger than the normal radiation from the Hawkesbury sandstone formation. The radioactivity was found to be associated with nodular laterite capping over large areas of the Hawkesbury sandstone in the National Park area. The results of one radiometric traverse from Heathcote to Waterfall across one small isolated patch of laterite in the vicinity of Sebastopol trig. station (locality map—Fig. 1) is presented in Figure 2. I. A. MUMME 102 IMILE PER INCH HEATHCOTE RADIOMETRIC TRAVERSE SCALE Pr > i" lene Il LATERITE MEV WATERFALL IN ENERGY Fic. 3 Gamma ray spectrometry pulse height distribution. Sain Auvarigauy Ni TANNVHD wad asvad SONILNNOD 2 ee ee wes Ly Sapa al : El , | ; tobe t tT TT TA TT ah ft AT hl TT Abed Als tbl ET LAT a AWA CTT SSM Tare Pn Ce Pie ae wT SPOT eee) Tet TCT Pe PERSE 6 SBEes ssa seee AR ee eee ees eee Oe 2oSeeesee i Fes a all eae al @— WATERFALL ae ‘9}OOYPEIFY 0} [[eJ19VeAA WOIJ spulo}KO oSIOAPIT ‘yisodap 9}119}e] DATJOROIPeI—PIOIEI OSIOAPI[—'Z ‘DI RADIOACTIVE LATERITES IN NATIONAL PARK AREA Le J Sutherland. D ot lo Z GARig BEacy Fic. 4 Radiometric traversing showed that large areas of radioactivity are associated with laterite cappings in the National Park area (see Fig. 4). Measurements of the radioactivity of the laterite show that the readings are erratic and quite variable, and activity up to 14 micro- roentgens per hour was recorded in traversing. 103 } Cronulla, 6 pack! a RADIOMETRIC TRAVERSES =m RADIOMETRIC ANOMALIES YM (DuE TO LareritTEs) SCALE IMILE PER INCH The normal levels for the adjacent Hawkesbury sandstone was of the order of 5 microroentgens per hour. Gamma-spectrometry measurements showed that the radioactivity was due to a thorium mineral being present. A small contribution was due to the presence of radium C (see Fig. 3). 104 Nature of Laterite This laterite forms an extensive capping upon the Hawkesbury sandstone in the area investi- It comprises nodular ironstone strongly. The ironstone consists of . gated. cemented together. sesqui oxide of iron and some kaolin. Geological studies by various investigators suggest that the laterite profile represents an exposed alluvial horizon which was formed under humid and wet conditions, possibly from a shale horizon on the Hawkesbury sandstone. Conclusion Anomalous surface gamma-ray intensities were located while conducting a programme ‘of Ai) MUMME | measurement of the characteristic levels of gamma-ray intensities in the National Park area. The radioactivity was found to be associated with extensive areas of laterite capping on Hawkesbury sandstone and investigations show that the radioactivity was due to the presence of a finely divided thorium mineral with a small contribution from radium C-bearing mineral. References BuraGess, A., AND BEADLE, N. C. W: (1952): Aust. j» Sc1., 14, 16)! : CaRROLL, D. (1951): Aust. J. Sci., 14, 41. _ Journal and Proceedings, Royal Society of New South Wales, Vol. 98, pp. 105-109, 1965 The Mesozoic Age of the Garrawilla Lavas in the Coonabarabran- | Gunnedah District J. A. DULHUNTY Department of Geology and Geophysics, University of Sydney ABSTRACT—The purpose of this paper is to place on record field evidence confirming the conclusion, reached by E. J. Kenny in 1928, that extrusive basic lavas occur as interbedded flows in Mesozoic rocks in the Coonabarabran-Gunnedah district. The history of geological work and conclusions regarding the age of the Garrawilla Lavas is reviewed, and results of recent field investigations are presented. Original Surveys and Conclusions In 1927 and 1928, E. J. Kenny of the Geological Survey of New South Wales carried out a preliminary geological survey of the Coonabatabran-Gunnedah district. Results of his survey first were published in summary form in Annual Reports of the Department of Mines in 1928 and 1928 (Kenny, 1928, 1929). The manuscript of a complete report was prepared in 1929, under the title of ‘“ Geological Survey of the Coonabarabran-Gunnedah District with Special Reference to the Occurrence of Sub- surface Water.”’ This report, including Kenny’s original map, has now been published as New South Wales Department of Mines, Geological Survey, Mineral Resources No. 40 (Kenny, 1963). In the foregoing publications, amongst other results, Kenny recorded his conclusions that contemporaneous basalt flows, which he termed the “‘ Garrawilla Lavas’’, occurred interbedded between “‘ rocks of Lower Mesozoic age and beds of undoubted Jurassic age’’. He described the Garrawilla Lavas as lying conformably upon the Napperby Beds, probably of Triassic age, and overlain disconformably by the Purlawaugh Beds and Pilliga Sandstone of Jurassic age. From this it was inferred that the age of the Garrawilla Lavas was either late Triassic or early Jurassic. Kenny described and mapped the outcrop of Garrawilla Lavas over a relatively wide area extending from Binnaway and Coonabarabran, east to Tambar Springs and Spring Ridge, and north-east through Rocky Glen and Mullally to within about ten miles of Gunnedah. Throughout this area (see Fig. 1), but particu- larly on its western, north-western and southern sides, his maps show Garrawilla Lavas out- cropping from beneath areas of Purlawaugh Beds and Pilliga Sandstone. To the east of Tambar Springs and Mullally, within the area of the Liverpool Plains, where overlying Jurassic sediments have been removed by erosion, Garrawilla Lavas are shown covered in places by extensive sheets of Recent alluvium. Flows of Tertiary basalt, from the Warrambungle Mountains on the west, and the Liverpool Range on the south, are shown extending across the top of the Jurassic sediments into the area of outcrop of Garrawilla Lavas. In some places Tertiary basalt flows are shown overlapping Jurassic sediments on to the Garrawilla Lavas. Kenny also’ describes the widespread occurrence of medium to coarse grained intrusive rocks in the form of large sills, probably of Tertiary age, associated with the Garrawilla Lavas, particularly in the north-eastern portion of the area. Before commencing work in the Coona- barabran-Gunnedah district, Kenny had already completed a survey of the Dunedoo-Binnaway area (Kenny, 1928a). Following the mapping of the Coonarababran - Gunnedah district, extensive surveys of Permian and Mesozoic strata were carried out by other geologists in areas to the south-east, south and south-west. These include the Dubbo-Cobborah area (Lloyd, 1935), the Merriwa-Murrurundi district and south-eastern Liverpool Plains (Dulhunty, 1939a), and the Gulgong-Coolah district (Dulhunty, 19390). The Mesozoic stratigraphy of all adjacent areas was satisfactorily correlated with that of the Coonabarabran-Gunnedah district (Kenny and Lloyd, 1935; Dulhunty, 1939d). The Purlawaugh Beds, with their characteristic and persistent “‘ red-bed ”’ lithology, were followed 106 into all adjacent areas, but contemporaneous flows of Garrawilla Lavas were not actually recognized beyond the limits of the Binnaway- Coonabarabran-Gunnedah-Spring Ridge district. It was considered, however, that the highly ferruginous and “ basic’”’ or tuffaceous nature of the Purlawaugh Beds, and equivalent strata in nearby areas, was probably due in part to the influence of contemporaneous volcanic activity, either by addition of pyroclastic material or basalt weathering-products, to the fresh-water lake sediments. In 1944, Mulholland (1950) published a review of the southern Intake Beds of the Great 4 L.) ao) 2 ) 4 > Sco/e in miles pawilla Gq?" Sy COONABARRABRAN 7 Ulamambri \ 4 Bingie Artesian Basin. In this work he accepted Kenny’s original definition of the Garrawilla Lavas as contemporaneous interbedded Mesozoic lava flows, and illustrated their mode of occurrence in a regional section across the Coonabarabran-Gunnedah district. Recent Work and Opinions Throughout the years that have followed the original descriptions and mapping of Mesozoic rocks in the Coonabarabran-Gunnedah and adjacent district, a certain degree of scepticism has arisen in the minds of some geologists regarding the Mesozoic age of the Garrawilla Lavas. Doubt not only exists as to whether Rocky Glen Garrawilla Station Ge agoragilla J. A. DULHUNTY all the flows are Mesozoic, but also as to whether, in fact, any of the flows originally mapped as Garrawilla Lavas represent Mesozoic extrusives or Tertiary basalt flows. In the preparation of an amended Geological Map of the State (1962) by the New South Wales Department of Mines, some basalt flows in the Mullally and Spring Ridge areas, originally mapped as Garrawilla Lavas, were redefined and shown as Tertiary flows. However, G. Rose of the Geological Survey of New South Wales (Rose, 1963), later pointed out that whilst “ the Garrawilla Lavas are considered by some workers to be flows and sills of Tertiary Mullally Curlewis LIVERPOOL 9 ~_ ~_ 9 rz t 3 LEGEND — Rogds ++ Roilwayps & Trig. Stations age, this is not yet substantiated over the whole area, or the type area, of the Garrawilla Lavas, and conclusive proof either way requires further mapping ”’. Wilshire and Standard (1963) examined a small area in the Mullally-Rocky Glen district, in which they concluded that all the basalt flows were of Tertiary age, and overlay Permian sediments. In discussing the regional geological setting of the area, they stated that “ Kenny considered the lavas to be interbedded with sediments of lower Mesozoic age’’, and that “ detail mapping has shown this to be incorrect, and that the lava flows everywhere oveilie the sediments ”’. MESOZOIC AGE OF GARRAWILLA LAVAS OF COONABARABRAN-GUNNEDAH 107 The area examined by Wilshire and Standard is situated almost in the centre of the major area of outcrop of the Garrawilla Lavas, on a pronounced structural high where overlying sedimentary rocks have been removed by erosion. In these circumstances field evidence of the Mesozoic age of the lavas would be difficult to appreciate. It appears that Wilshire and Standard may not have examined in detail the western and southern margins of the area of basalt outcrop, near Rocky Glen and Tambar Springs (beyond the limits of their area) where relations between the basalt flows and adjacent Mesozoic sediments can be seen to good advantage. Also, in their assumption “that the lava flows everywhere overlie the sediments ’’, it is possible that they may have included some of the Jurassic Pilliga Sandstone on the western side of their area, with sediments, in which they recorded the presence of glossopteris, exposed beneath the lavas by dissection on the structural high further to the east. Confirmation of Original Conclusions In 1963, the present author commenced a very critical and detailed investigation of field evidence bearing on the age of the Garra- willa Lavas throughout the Coonabarabran- Gunnedah-Spring Ridge region. During the first stage of this work a careful examination was carried out of all areas in which the lavas occur adjacent to Mesozoic sedimentary rocks and detailed investigations were made along actual field boundaries between the lavas and sediments. Asa result of this work, the author is now convinced, beyond all doubt, of the correctness of Kenny’s conclusions that Garra- willa Lavas occur as interbedded flows, out- cropping from beneath lower Mesozoic sediments along the margins of the basalt areas within the region of his original maps. The author is also convinced that Kenny’s maps, of field boundaries between the lavas and lower Mesozoic sediments, are correct and accurate in all significant details. In places, such as the country -letween Mullally and Tambar Springs, and over parts of the Liverpool Plains, basalt flows extend from marginal outcrops over wide areas from which all overlying Mesozoic sediments have been removed by erosion. In such areas it is very difficult to confirm the Mesozoic age of flows and to distinguish between Garrawilla Lavas and Tertiary flows, which in places were extruded after the removal of Mesozoic sediments. It is B anticipated that further work on _ petrology of the lavas, stratigraphy of the flows, and possibly radioactive dating, will eventually lead to a complete differentiation of basalts of the two ages and a clearer regional picture of the extent of Mesozoic vulcanism. At this stage, however, it is quite definite that basic, Mesozoic lavas do occur over a wide area in the Coona- barabran-Gunnedah district, and the following field evidence is submitted in support and confirmation of their occurrence. (1) Everywhere throughout the entire area of occurrence, the trend of the boundary between Garrawilla Lavas and Mesozoic sediments is strictly related to structure and stratigraphy of the sediments, and in some places to Mesozoic relief on the “ pre- Purlawaugh ” surface of the lavas. In no case is it related to Tertiary topography, as would be the case if the lavas were of Tertiary age, occurring as flows filling Tertiary valleys. The close relationship between the trend of the boundary and sedimentary structure is seen to best advantage in valleys, such as those of the headwaters of Saltwater and Yaminba Creeks, which have dissected gently-dipping Pilliga Sandstone and exposed underlying Purlawaugh Beds and associated Garrawilla Lavas. In such places, the boundary of the lavas, and the well-defined base of the Pilliga Sandstone, run parallel and rise together across valley sides to the general level of the surrounding country, where they continue as parallel outcrops, in the general strike-direction of the sedimentary rocks. This is a simple and well-known relationship of structure and outcrop to contour, which confirms the interbedded nature of the lavas. Where. relief occurs on the ~ pre= Purlawaugh ” surface of the lavas, there is marked disconformity between the lavas and overlying sediments. In some places this has resulted in overlapping of the Purlawaugh Beds by Pilliga Sandstone on to the lavas. However, the regional dip of the lavas remains parallel to that of the sediments. Basalt flows of undoubted Tertiary age do occur, as shown on Kenny’s original maps, at several places such as Coolanbilla, Tamba and Bingie Trigono- metrical Station, and in the parish of Urabrible to the south of Coonarabran. In all cases it is quite evident that such flows lie on Tertiary erosion surfaces, across outcrops of Pilliga Sandstone and Purla- 108 ~—— J. A. DULHUNTY waugh Beds, that their boundaries are determined by Tertiary topography and post-basalt erosion, and are in no way related to structure or stratigraphy of the underlying Mesozoic sediments. Over most of the district surface relief is low, and valleys are wide and shallow. ‘Where basalt occurs in such valleys, it is very difficult to ascertain, by casual field inspection at isolated points, whether the basalt is a residual of a Tertiary flow filling the valley, or an interbedded Mesozoic flow outcropping on the sides and floor of the valley. In such circumstances it is necessary to study relations of outcrop to structure and contour, to appreciate the true situation. It seems highly probable that casual field inspection, without apprecia- tion of the regional picture, has contributed to the incorrect assumption that the Garra- willa Lavas are of Tertiary age. Whilst surface relief is generally low, there are, however, several places in the district where erosion on valley sides has provided exposures in which the lavas can be seen actually outcropping from beneath Mesozoic sediments. In the lower reaches of Saltwater Creek the outcrop of the top of the Garrawilla Lavas can be seen separated by about 10 feet of brown clay from an overlying sandstone unit in the Purlawaugh Beds. Exposures of this section occur on J. S. Darling’s property “ Carnamah”’ in Portions 15, 16 and 20, Parish of Wilson, and on L. G. Thompson’s _ property “ Tallawong’’, in Portions 31 and 32, Parish of Saltwater. Four miles from Coonabarabran, on the northern side of the Ulimambri road, in the vicinity of Portions 90, 108 and 111, Parish of Coonabarabran, the outcrop of the top of the Garrawilla Lavas can be seen in creek beds separated by about eight feet of soft yellow puggy clay from 18 inches of soft white conglomerate at the base of the Pilliga Sandstone. On the southern side of the road at this place, Tertiary basalt flows occur on top of the Pilliga Sandstone. About 16 miles from Coonabarabran on the Rocky Glen road, “at eP. W.Re 07, Parish of Mamum, on the western side of the valley of Yaminba Creek, the top of the Garrawilla Lavas is separated from massive Pilliga Sandstone by 15 feet of soft, yellow- brown limonitic clay with thin bands of hard yellow chert. = Some four miles north-east of Rocky Glen, on E. R. Shannon’s property “‘ Balmoral ’’, in the vicinity of Portions 111 and 293, Parish of Girriwilli, there are excellent exposures of the top of the Garrawilla Lavas outcropping from beneath the base of the Purlawaugh Beds which are 60 feet thick and overlain by the Pilliga Sandstone. At several points along the Tambar Springs-Goragilla road, where it forms the boundary between the Parishes of Urangera and Wilson, there are good exposures of the outcrop of the top of the Garrawilla Lavas, separated by 10 to 20 feet of clay from 40 feet of sandstone in the Purlawaugh Beds, about 100 feet below the base of the Pilliga Sandstone. The occurrence of from 5 to 20 feet of soft, reddish-brown to yellow, puggy clay between the top of the Garrawilla Lavas and overlying sedimentary rocks of the Purlawaugh Beds or Pilliga Sandstone, is very persistent throughout the district. The junction between the lavas and the overlying clay, frequently appears as a transition rather than a sharp change. This suggests that the clay, which is probably a weathered mudstone, represents products of contemporary weathering of the upper surface of the lava before, and immediately after, the deposition of Mesozoic sediments. As described originally by Kenny, sills of doleritic material, probably of Tertiary age, are associated with the Garrawilla Lavas in some places. The presence of intrusive sill rocks appears to have been responsible for suggestions that all the Garrawilla Lavas may be sills rather than lava flows. There is, however, an abundance of field evidence, placing beyond all doubt the fact that they are lava flows, as follows: (a) Nowhere is there any indication of contact metamorphism above the Garra- willa Lava flows. As already described, the lava passes by gradation into a soft mudstone which is followed in turn by normal shales or sandstone. (0) Amongst the Garrawilla Lava _ there commonly occur highly vesicular and amygdaloidal basalt flows up to 100 feet in thickness. At a number of places, including exposures where the Garrawilla Lavas can be seen outcropping from beneath Mesozoic sediments, beds of bole, from 10 to 20 feet in thickness, occur between (c) MESOZOIC AGE OF GARRAWILLA LAVAS OF COONABARABRAN-GUNNEDAH 109 some of the flows. These occurrences exhibit all the features of bole beds normally associated with extrusive, basic igneous flows. Acknowledgements In conclusion, the writer wishes to acknow- ledge that the investigation described in this paper was made possible by financial assistance from the Burma Oil Company of Australia and Planet Oil Company, and by research facilities provided by the University of Sydney. References DuLuHuntTy, J. A., 19394. Merriwa-Murrurundi Mesozoic Stratigraphy of the District and South-Eastern Liverpool Plains. j. Proc. Roy. Soc. N.S.W., 73, 29. Dutuunty, J. A., 1939b. Mesozoic Stratigraphy of the Gulgong-Coolah District. Soc. N.S.W., 13, 150. Kenny, E. J., 1928a. Geological Dunedoo-Binnaway District. N.S.W., Ann. Rept., 1927, 119. ey GPi0c. eiLoy: Survey of the Dept. Mines, Kenny, E. J., 19286. Geological Survey of the Coonabarabran-Gunnedah District with Special Reference to the Occurrence of Sub-surface Water. Dept. Mines, N.S.W., Ann. Rept., 1927, 130. Kenny, E. J., 1929. Geological Survey of the Coonabarabran-Gunnedah District with Special Reference to the Occurrence of Sub-surface Water. Dept. Mines, N.S.W., Ann. Rept., 1928, 117. Kenny, E. J., 1963. Geological Survey of the Coonabarabran-Gunnedah District with Special Reference to the Occurrence of Sub-surface Water. Dept. Mines, N.S.W., Min. Res. No. 40. Kenny, E. J., and Liovp, A. C., 1935. Table of Correlation of Geological Formations of the Dubbo-Gunnedah Region. Dept. Mines, N.S.W., Ann. Rept. 1934, 86. Lioyp, A. C., 1935. Geological Survey of the Dubbo District with Special Reference to the Occurrence of Sub-surface Water. Dept. Mines, N.S.W., Ann. Rept. 1934, 84. MULHOLLAND, C. St. J., 1950. Review of Southern Intake Beds, New South Wales, and their Bearing on Artesian Problems. Dept. Mines, N.S.W., Geol. Repts. 1939-45, 125. Rose, G., 1963. ‘* Foreword.’ Min. Fes. No. 40. WILSHIRE, H. G., and STANDARD, J. C., 1963. The History of Vulcanism in the Mullally District, N.S.W. J. Proc. Roy. Soc. N.S.W., 96, 123. Dept. Mines, N.S.W., iH 7 ie if a : ‘ 7 : : 7 a iar a b j i ui ‘ yaa ou: Wr if Loe ¢ , io er Fi : Os on fat M ’ . _ 7 , S the om ‘ Wh Ft b a ‘ ’ , oe ag ; in : ; ‘ a y y i ya ee Journal and Proceedings, Royal Society of New South Wales, Vol. 98, pp. 111-120, 1965 Clay Mineralogy of some Upper Devonian Sediments from Central New South Wales JOHN R. CONOLLY School of Applied Geology, University of New South Wales, Sydney* ABSTRACT—The clay mineral fraction of 48 sediments from the Upper Devonian of central New South Wales has been determined using standard X-ray and petrographic techniques. The clay deposited in the Upper Devonian sediments consists mainly of illite, chlorite and mont- morillonite with a little kaolinite. Impermeable shales and siltstones generally have a significantly different clay mineral content compared to the more permeable, associated siltstones and sandstones where post-depositional degradation processes have formed mixed-layered illite, chlorite and montmorillonite minerals and resulted in the precipitation of kaolinite from solution. A higher chlorite content in the east is probably due to a large proportion of weathered volcanic rocks in the source area, whereas a higher illite content in the west is probably the result of the source rocks being rich in quartz and mica. Introduction In the following investigation, approximately 50 outcrop samples of shales, siltstones and sandstones from the Upper Devonian of central- western New South Wales were examined by X-ray diffraction to ascertain both the original clay composition at the time of lithification and the amount of alteration to this clay due to post-lithification changes. Sample Selection and Preparation Forty-eight samples of shales, siltstones and sandstones were selected from outcrops of the Catombal Group in the Wellington-Molong district (Conolly, 1963), the Hervey Group in the Peak Hill-Parkes-Grenfell-Weddin Range area (Conolly, 1965a, 1965c), and the Cocoparra Group in the Naradhan-Rankins Springs district (Conolly, 1965c) (Fig. 1). Although all samples were weathered to some extent, the effect was minimised by the collection of large samples and selection of the freshest parts during the crushing operation. The list of samples with their lithology described is given in Table 1. Each sample was crushed with a pestle and mortar, and sieved through a Tyler 100 mesh screen. Approximately 20 to 40 grammes of the clay were dispersed in water and the suspension allowed to settle for the required period (Jackson et al., 1950) before drawing off the fraction less than two microns in diameter. Oriented samples were prepared on glass slides from this fraction. * Present address : Geology Department, Louisiana State University, Baton Rouge. X-Ray Diffraction and Determination of Clay Minerals Each sample, which consisted of an orientated aggregate of clay on a glass slide, was X-rayed four times ; firstly without further treatment ; secondly upon glycolation ; thirdly after heating to 450° C for one half to two hours ; and fourthly after heat treatment to 600° C for half an hour. The various clay minerals were identified using the following criteria : Kaolinite and chlorite: Kaolinite was easily distinguished from other clay minerals with the exception of some chlorites. The criteria used to distinguish kaolinite from chlorite have been outlined by Bradley (1954) and later by Smoot (1960). According to these authors, well-crystallised chlorite exhibits sharp first, second and third order peaks at 14, 7 and 4-7 A, but after heat treatment to 575°C, the 14 A peak is intensified whereas the 7 and 4:7 A peaks are less distinct. Kaolinite, on the other hand, loses its structure after heat treatment to 480° C for half an hour due to dehydroxylation. Hence upon glycola- tion and after heat treatment to 450° C, the 7 A peak is unchanged but after further heat treatment to 600°C the 7 A peak disappears. (Fig. 3). Illute: Smoot (1960) recognised two groups of illite. The first, a well-ciystallised, non- expandable material is characterised by sharp peaks at 10 and 5 A. The diffraction patterns of these illites are similar to muscovite, although the clay minerals generally have a weaker second-order reflection at 5 A (Fig. 2). The 112 second group is characterised by a basic mica structure with a small amount of mixed- layered material. Montmorillonite: Montmorillonite minerals are distinguished by peaks in the range of 12 to 14 A which expand to 17 A after satura- tion with glycol in’a normal humidity state. After heat treatment to 450°C. the mineral completely collapses to give a peak at 10 A (Fig. 2). Mixed-Layer Clay: Mixed-layer clay minerals are usually identified by reflections which are combinations of the reflections of the clay minerals making up the mixed-layer. Generally, ankins Springs 8 \ Narrandera ——_ E=q Lambie Group [J Mulga Downs Group *Cootamundra | (oe | Griffith \yardiethan? Be Young | Hervey Group ' JOHN R. CONOLLY of clay minerals including those by Johns, Grim and Bradley (1954), Murray (1954), Weaver (1958) and Schultz (1960). Schultz (1960) has described a method which can be used with a fair degree of accuracy for the common clay minerals in ancient sediments. Schultz reported that chlorite was the only clay mineral for which no consistent method could be found. The writer has used the system outlined by Schultz which is briefly summarised as follows : a. The height intensities of the 7 A (001) of kaolinite and the 10 A illite material are measured. Catombal Group Cocoparra Group Pie? all Geological sketch map of central New South Wales showing the outcrop distribution of Upper Devonian sediments. the mixed-layer clay minerals in sediments are random structures which give broad reflec- tions over a range of 20 values, on the diffraction pattern. Mixed-layer clay minerals are virtually absent from the samples investigated in this study. Sometimes a very small amount of random mixed-layer clay is associated with illite and, where present it has been included with the illite. Quantitative Estimates of Clay Mineral Composition Various papers have been published in the last decade dealing with quantitative estimates b. Heat treatment to 600°C collapses the structure of the montmorillonite material and hence the intensity of the 10 A at 20° C is subtracted from the 10 A intensity at 600° C, to give a peak height for mont- morillonite. Theilliteandmontmorillonite peak intensities are multiplied by two and the kaolinite peak intensity by one. The amount of mineral present is then pro- portional to the new peak intensities. The chlorite content is shown in relative values only. In Table 1, a strong 14 A line, reflecting a high relative percentage of chlorite, is indicated by three plus sign. CLAY MINERALOGY OF SOME UPPER DEVONIAN SEDIMENTS 113 TABLE I Percent Rock Sample Median Percent Rock Kao- Mont- Type no. Formation Colour Grain Clay Frag- _linite [llite Chlorite moril- Size ments lonite in mm. CATOMBAL GROUP Shale 216 Kurrool Fm. green 0:Ol 60 — tr 10 +++ Shale 200 Kurrool Fm. green 0-01 65 — 10 +++ + Shale 212 Macquarie Park green 0-01 50 — l 9 ++ + She), Siltstone 208 Kurrool Fm. white 0-03 18 Path 6 4 Siltstone 144 Kurrool Fm. white 0-06 25 5 4 6 Siltstone 193 Macquarie Park red 0:07 20 10 6 4 Se Fine sandstone 178B Macquarie Park red 0-2 15 12 6 4 Seo. . Fine sandstone 149 Macquarie Park white 0°15 14 11 6 + -- Sher Fine sandstone 154 Macquarie Park white 0-5 22 11 + 6 + Sesr Fine sandstone 148A -Brymedura S.S. _ buff 0-4 15 20 5 5 “PF -l- Fine sandstone 148B Brymedura S.S. white 0:4 ll 16 6 4 + + HERVEY GROUP Shale 516 Mandagery S.S._ red 0-01 70 1 10 +++ Shale 415 Weddin S.S. green 0-01 70 1 9 +++ — Siltstone 586 Bumberry Fm. buff 0-04 20 10 3 7 Siltstone 587 Bumberry Fm. _ red 0:06 16 13 2 8 +++ Siltstone 565 Bumberry Fm. brown 0-06 35 20 4 6 +++ Siltstone :. 966 Bumberry Fm. brown 0-06 15 17 3 7 +++ a Fine sandstone 559 Mandagery S.S._ buff 0-1 4 16 3 eth wae ++ Fine sandstone 520 Mandagery S.S. green 0O-l 38 8 3 7 +-+ + Fine sandstone 563 Bumberry Fm. white 0:1 17 2 6 4 +++ — Fine sandstone 384 Caloma S.S. white 0°12 19 3 7 3 Fine sandstone 385 Caloma S.S. buff 0-13 15 3 6 4 Fine sandstone 578 Mandagery S.S. red 0-15 14 10 5 5 Fine sandstone 549 Mandagery S.S. pink 0-2 10 15 7 3 Fine sandstone 510 Mandagery S.S. white 0:2 1 1 + 6 Fine sandstone 423 Mandagery S.S. white 0-2 13 9 1 9 +++ + Fine sandstone 507 Boona S.S. white 0:2 12 2 8 Fine sandstone 595 Bumberry Fm. _ red 0:2 20 18 3 7 + + + Fine sandstone 550 Bumberry Fm. white 0-2 8 11 4 6 Fine sandstone 391 Pipe Fm. buff 0:2 ii 3 6 4 ++ > Fine sandstone 386 Burrill Fm. brown 0-2 14 1 4 6 Fine sandstone 389 Mandagery S.S. red 0-33 13 18 1 9 Medium sand- 428 Weddin S.S. white 0-5 5 Z 6 4. stone Medium sand- 506 Boona S.S. white 0-6 2 4 6 stone Medium sand- 591 SBumberry Fm. brown 0:8 12 42 2 8 ++ stone COCOPARRA GROUP Fine sandstone 483 Womboyne Fm. white 0-1 20 5 + 6 Fine sandstone 482 Womboyne Fm. white 0:1 16 6 4 6 Fine sandstone 492 Womboyne Fm. red 0-2 8 4 3 if Fine sandstone 489 #Rankin Fm. white 0:22 2 1 10 Fine sandstone 476 Ardlethan S.S. brown 0:2 17 10 2 8 + + Fine sandstone 501 Rankin Fm. red 0:25 18 5 3 7 Fine sandstone 499 Rankin Fm. brown 0:3 14 15 2 8 — — Fine sandstone 487 #Rankin Fm. white 0:°3 15 30 4 6 Fine sandstone 491 Rankin Fm. brown 0-4 4 dl 2 8 Fine sandstone 463 Rankin Fm. white 0-4 6 5 5 Fine sandstone 468 Barrat Con- white 0:3 8 4 3 i | glomerate Fine sandstone 469 Barrat Con- white 0-4 4 2 3 7 glomerate Medium sand- 486 Rankin Fm. ~ white 0-7 4 6 7 3 stone 114 JOHN R. CONOLLY Lute (001) lite (002) lute (003) + quartz Chlorite (001) Kaolinite (001) + Chlorite (002) Room temperature Intensity Glycolated 450° c 20! 1 degrees 286 ics 2 X-ray diffractometer patterns (Cu radiation) of the clay fraction of a green shale from the Catombal Group (sample no. 200). Where the 14 A reflection was moderate or ratio of chlorite to illite was found by weak, two or one plus signs only are used. multiplying the 001 peak intensity for In order that some quantitative assess- chlorite by a factor of four, and comparing ment could be made of the amount of it with the 001 peak of illite at normal chlorite present in the sediments, a method intensity. This method was only used used by Smoot (1960) was adopted. The where the sample showed high peak CLAY MINERALOGY OF SOME UPPER DEVONIAN SEDIMENTS 115 oa ae © se jes oS} S |e Y gy ed) S ole =r =i 2S ¢fe |Fhs Si| wo olfe = £i| ~ Flic O Room temperature O}|)= SI hs o 450 C Intensity 600° C 3 2 (a 1 degrees 26 Fic. 3 X-ray diffractometer patterns (Cu radiation) of a lithic sandstone from the Hervey Group (sample no. 595). intensities for chlorite and hence a d. Montmorillonite never occurred in large relatively high chlorite content, enabling quantities, but the presence of a small a quantitative assessment of the total 17 A peak on glycolation was denoted clay mineral content shown on_ the using plus signs in a similar way to histograms on Fig. 4. chlorite (Table 1). 116 Petrographic Analysis Thin sections were cut from each of the samples studied, and a petrographic analyses were made using the point counter method (Chayes, 1956). The percentage clay matrix, rock fragments containing clay, approximate median grain size, and the colour of the sediment was noted and are listed with the clay mineral analyses on Table 1. Clay Mineral Content of Upper Devonian Sediments Fig. 4 shows the average clay mineral composition of sandstones, siltstones and shales from the Catombal, Hervey and Cocoparra Groups, obtained by calculating the average composition from the analyses listed on Table 1. In general, shales have a significantly different clay mineral content from that of the sandstones occurring within the same sequence. THE CATOMBAL GROUP: The shales of the Catombal Group consist of illite, chlorite and some montmorillonite, with very little kaolinite, yet the interbedded siltstones and sandstones have a characteristic kaolinite-illite clay mineral suite with only small percentages of chlorite and montmorillonite (Table 1). The sediments of the Catombal Group are essentially quartzose and even the siltstones and shales generally consist of 40 to 50 percent detrital quartz. The sandstones vary from orthoquartzites to lithic sandstones (Plates 1 and 2), the majority being protoquartzites with rock fragments and felspar making up 10 to 25 percent of the detrital grains (Conolly, 1963). The clay released during gentle crushing of these sediments is either original clay matrix or is derived from broken clay pellets and rock fragments. The clay released from the shales and siltstones is generally entirely clay matrix, whereas the origin of the clay released from sandstones depended on the composition and texture of the rock. Petrographic examination of the sandstones shows that orthoquartzites contain very small percentages (less than 10 percent) of rock frag- ments and generally similar amounts of clay matrix. Pockets of discrete kaolinite “ books ” occur commonly in these orthoquartzite sands (Plate 2, Fig. 3). Illitic clay patches are gener- ally just ascommon. The remainder of the clay is derived from crushed rock fragments, shale and siltstone and to a minor extent from weathered acid volcanic rock fragments. No differences can be readily observed between the clay fractions of the sandstones JOHN R. CONOLLY Ave ne Crags of the different formations of the Catombal — Group. All have approximately equal amounts of kaolinite and illite and about half have small amounts of chlorite and montmorillonite. THE HERVEY GrRovuP: Similar results were obtained for the sandstones, . siltstones and shales of the Hervey Group (Table 1). There is a gradual transition from low kaolinite and high chlorite in the shales, siltstones and very fine sandstones to high kaolinite and low chlorite percentages in the coarser sandstones. Amongst the sandstones, some of the well- sorted orthoquartzites (Sample Nos. 563, 384, 385 and 391) contain high amounts of kaolinite and some of the lithic sandstones contain significantly high amounts of chlorite and little kaolinite (Sample Nos. 595, 389, 591). Most of the other sandstones lie between these two. There are several exceptions to the above generalisation, for example, the orthoquartzite sandstones from the Boona Sandstone have relatively low amounts of kaolinite. It is suspected that these differences are caused by differences in clay provenance, as the Boona Sandstones outcrop in the Condobolin district west of the area from which the remaining samples were obtained. THE COCOPARRA GROUP: The sandstones of the Cocoparra Group have a characteristic illite-kaolinite clay fraction, with chlorite and montmorillonite occurring in small amounts in only two samples. Once again, the ortho- quartzites contain higher percentages of kaolinite than the more lithic sandstones (Table 1). Mineralogy and Colour of the Sediments Although most shales in the Catombal and Hervey Groups are green, some are red. The occurrence of these two different varieties of shale could imply different environmental con- ditions, however the clay mineralogy remains the same. Examination of the slides in thin- section shows that whereas both varieties of shale contain the green-coloured chloritic clay mineral, the red shales contain so much iron oxide minerals they appear red in colour. The colour of siltstones and sandstones is mainly caused by the colours of the included rock fragments or their weathered products, or by iron oxide fragments. White siltstones and sandstones are generally orthoquartzites or protoquartzites and contain significantly high proportions of kaolinite (Table 1). The lack of colour is due to the lack of “iron-stained ”’ rock fragments and the green clay minerals, chlorite and montmorillonite (Keller, 1953). JOURNAL ROYAL SOCIETY N.S.W. CONOLLY PLATE I Explanation of Plates PLATE I Figure 1 : Brymedura Sandstone, Catombal Group, no. 148A. A fine-grained protoquartzite with most of the rock fragments altered to illite and kaolinite. Fragment in lower left corner is a devitrified acid volcanic rock fragment now greatly altered to kaolinite (light colour) and illite. Large clay area (centre) consists of meshworks of kaolinite filling pore space between quartz grains. Figure 2: Mandagery Sandstone, Hervey Group, no. 520. A fine-grained orthoquartzite with a high percentage of clay matrix. Detrital shreds of illite occur ‘“‘ squashed ’’ between subangular quartz grains. Figure 3: Kurrool Formation, Catombal Group, no. 216. A quartzose green shale or fine siltstone consisting of 60 per cent illite-chlorite clav and 40 per cent detrital angular quartz. Figure 4: Macquarie Park Sandstone, Catombal Group, no. 154. A fine to medium-grained protoquartzite. Consists of rounded to subrounded quartz grains, altered rock fragments and interstitial clay matrix. Rounded grain in upper centre consists of a meshwork of kaolinite surrounded by lighter-coloured illite which forms the interstitial matrix. JOURNAL ROVALYSOCIE TY SNe Seve CONOLLY PATE PLATE II Figure 1: Bumberry Formation, Hervey Group, no. 591. Coarse-grained lithic sandstone. Large amounts of kaolinite and illite clay fill spaces between quartz grains. In upper left and lower right, illitic clay shreds form distinct patches and represent former shale rock fragments. Figure 2: Bumberry Formation, Hervey Group, no. 591. Coarse-grained lithic sandstone. General view of sandstone texture showing mixture of discrete clay patches (altered shale and silt rock fragments, interstitial clay matrix and subangular to subrounded quartz grains. Figure 3: Brymedura Sandstone, Catombal Group, no. 148A. Fine-grained, well-sorted, protoquartzite. Quartz grains contain sutured or interlocking boundaries with adjacent quartz grains. A meshwork of kaolinite (centre) or kaolinite “‘ books’’ fills space between quartz grains. Figure 4: Brymedura Sandstone, Catombal Group, no. 148A. Protoquartzite with a large rounded shale rock fragment between quartz grains. CLAY MINERALOGY OF SOME UPPER DEVONIAN SEDIMENTS The colour of lithic sandstones is mainly the result of the presence of pigmentary iron minerals in the rock fragments, which give the rocks a buff, brown or red colour. However, white lithic sandstones occur in places and are particularly characteristic of the Rankin Forma- tion of the Cocoparra Group (Table 1). The rock fragments in these sandstones are generally altered to illite and kaolinite and there is a lack of iron pigmentation. Origin of the Clay Minerals Potter and Glass (1958), Weaver (1958), Smoot (1960), have shown that the clay mineralogy of sandstones and associated finer sediments (siltstones and shales) is different. For instance, alteration of clay minerals in permeable sediments, such as sandstones, occurs after lithification and during weathering. Glass, Potter and Siever (1956) have shown that the outcrop sandstones of some basal Pennsylvanian sediments in Illinois have a clay mineral content of approximately 50 percent kaolinite, 25 percent mica, 15 percent chlorite and the remainder, mixed-lattice clay (10 percent), whereas the associated shales contain only approximately 25 percent kaolinite, 40 percent mica, 10 percent chlorite and 25 percent mixed- lattice clay. In other words, the sandstones contain relatively much more kaolinite and less illite than their associated shales. These authors considered the differences were due to contrasting post-depositional histories induced by contrasting permeabilities. In other words, the clay mineral content of the shales was considered to be almost identical to that at ‘the time of deposition. Presumably the sand- stones had a clay mineral content similar to that of the shales at the time of deposition and the differences now evident were due to transformations sometime after deposition. The amount of change in clay mineral content depended upon the quantity of water circulating through the rock and, hence, upon the perme- ability of the sandstone. The differences be- tween the clay mineral content of fresh outcrop samples of sandstones and shales is a measure of the amount of change that had occurred due to circulating groundwaters after lithification. Glass (1958) obtained similar results to those of Siever and Potter (1956). He showed that orthoquartzite and subgreywacke sand- stones from the Pennsylvanian sediments in Southern [Illinois contain relatively more kaolinite than the associated shales. Glass considered the kaolinite formed in the sand- stones after exposure. Core samples of sand- aly, stones showed the same type of high kaolinite content but to a lesser degree. Smoot (1960) showed that shale samples of the Pre-Pennsylvanian sediments of the Illinois Basin are composed dominantly of illite and chlorite, whereas the sandstones are composed dominantly of kaolinite, illite and chlorite. Smoot concluded that the clay mineral suites of shales, obtained either from subsurface or surface samples, are those that had been formed about the time of lithification, and have been altered either by weathering at the surface or by circulating formation fluids in the subsurface. Conversely, the clay mineral suites in permeable sandstones are controlled by circulating fluids in the subsurface and by weathering in the outcrops. If the permeability of the sediment is the main factor controlling the amount of degrada- tion of clay, then there should be a direct relationship between the amount of secondary clay mineral, kaolinite, and the permeability of the rock. For instance, well-sorted ortho- quartzitic sandstones are normally more perme- able and should therefore be more kaolinitic than argillaceous lithic sandstones and proto- quartzites. On the other hand, a decrease in grain size, and hence increase in argillaceous matrix, causes sandstones to become less permeable and, therefore, less kaolinitic. The sandstones, siltstones and shales of the Hervey and Catombal groups form a natural sequence of permeable—non-permeable rock types. The amount of kaolinite increases from shales to sandstones and it would appear that in these examples at least, permeability was one of the factors controlling kaolinite forma- tion. Similar differences exist for the sediments of the Catombal Group. Similar mineralogical differences can be ob- served between the well-sorted orthoquartzitic sandstones and more argillaceous lithic sand- stones within the Hervey Group. For instance, the protoquartzites and lithic sandstones of the Bumberry Formation have a different clay mineral suite to the well-sorted orthoquartzitic sandstones of the Caloma Sandstone and the Mandagery Sandstone (Table 1). The Bumberry Formation sandstones have a higher content of chlorite, illite and mont- morillonite clay than the orthoquartzitic sand- stones which have a characteristic kaolinite- illite clay mineral suite. However, although there may not be a difference in permeability between these two types of sandstones, there is the possibility that the differences in com- position have been induced due to differences 118 Percent : 5. JOHN R. CONOLLY kaolinite illite chtorite rrantmorillonite y, N Uf > N vh ‘\ 4 > N 7 6 1. Shales, 4. Sandstones Catombal Group Hervey Group 2. Shales, 3.Siltstenes, 5. Sandstones Cocoparra Group _ 6. Sandstones Fic. 4 Average composition of the clay fraction of some Upper Devonian sediments in central N.S.W. The percentages have been calculated after omission of the quartz content from the clay fraction. in the sedimentary environment and source rocks. In the above example, one of the original controlling factors is the large amount of rock fragments in the Bumberry sandstones. Rock fragments make up at least 50 percent of the clay fraction, and are therefore one of the factors controlling clay mineral composition. It is considered that differences in clay mineral content between orthoquartzitic and more argillaceous sandstones are basically due to both permeability and clay rock fragment content. This does not imply that there was any change in source rock composition because the clay-bearing rock fragments of the lithic sandstones could have been broken up by | greater transportation and reworking to form the clay matrix of the orthoquartzitic sand- stones. The Formation of Kaolinite in Permeable Sediments The occurrence of meshworks of kaolinite “books ”’ or kaolinite “‘ worms ”’ in sandstones was commonly observed in thin sections of the Upper Devonian sandstones investigated in this study. More frequently, kaolinite occurs as irregular and poorly-crystallised particles between detrital grains (Plates 1 and 2). Since CLAY MINERALOGY OF SOME UPPER DEVONIAN SEDIMENTS it has been shown that kaolinite is only present in the permeable siltstones and sandstones, it is concluded that the kaolinite is mainly of a secondary origin. The clay minerals of these permeable sedi- ments are accessible to percolating water and hence susceptible to intrastratal solution processes. Some of these processes occur during diagenesis and others are due to surface weathering. Smoot (1960) refers to solution processes during diagenesis and weathering processes. He shows that illite changes to illite plus mixed-layer clay during degradation processes. Loughnan, Grim and Vernet (1962) studied the weathering of some Triassic shales from the Sydney area, and showed that illite changes to mixed-layered clays, montmorillonite and, with more extensive leaching, kaolinite. Hence, it is concluded that the clay mineral content of the permeable siltstones and sand- stones of the Upper Devonian sediments has undergone similar degradation processes, both during lithification and weathering, with the formation of kaolinite at the expense of illite. Regional Variations in Clay Mineralogy Although changes in clay mineral composi- tion occur within a given suite of sedimentary rocks of similar provenance and environmental conditions, changes should also occur between two suites with different provenance and/or environmental conditions. If the clay mineral- ogy of the Catombal, Hervey and Cocoparra Groups is compared (Table 1, Fig. 4) there are some obvious differences in composition which are probably caused by differences in provenance since the conditions of original deposition and subsequent weathering have been similar for the three groups. For example, although the shales of the Catombal and Hervey Groups have a similar suite of clay minerals, kaolinite is probably less abundant in the former. This slight change in composition may be indicative of different environmental or source rock composition. Similarly, when the clay mineral suites of the sandstones of the Catombal, Hervey and Cocoparra Groups are contrasted, the following trends are suggested :— 1. Kaolinite becomes less abundant toward the west (from the Catombal to the Cocoparra Group) ; 2. Illite is more abundant in the west ; 3. Chlorite is more abundant in the east. 119 The sandstones of the Catombal and Hervey Groups with a high rock fragment content also have appreciable amounts of illite and chlorite. Hence it is concluded that the illite and chlorite are mainly contained in the rock fragments and that the high illite-chlorite composition of the associated shales is the original composition of the clay in the source rocks and has not been greatly affected by the environment of deposi- tion. Similar conclusions have recently been made by Vlodarskaya (1964) in his study of the distribution of clay minerals in Palaeozoic and Mesozoic rocks. The somewhat higher chlorite content of the Catombal and Hervey Group sandstones is probably a reflection of the higher amounts of weathered volcanic detritus being deposited in these Groups (Conolly, 1962). Further to the west, the source rocks of the Cocoparra Group are mainly sedimentary and have a characteristic high quartz and illite content (folded quartzose Ordovician sands, silts and shales—Conolly, 1962). These source rocks are probably responsible for the relatively higher illite content of the Cocoparra Group sandstones. Acknowledgements The writer wishes to acknowledge the assist- ance given by the teaching staff of the School of Applied Geology, University of New South Wales, and in particular, the helpful advice given by Dr. F. C. Loughnan and Mr. P. D. Bayliss. References BRADLEY, W. F., 1954. X-ray diffraction criteria for the characterisation of chlorite minerals in sedi- ments, Nat. Acad. Sci.—Nat. Res. Council. Pub. 327, 324. Cuayves, F., 1956. Petrographic modal analysis, J. Wiley and Sons. N. Y., 113 p. Cono_ty, J. R., 1962. Stratigraphic, sedimentary and palaeogeographic studies in the Upper Devonian rocks of central western N.S.W., Unpub. Ph. D. thesis. University of N.S.W. Cono_iy, J. R., 1963. Upper Devonian stratigraphy and sedimentation in the Wellington-Molong district, N-o.W., j- Proc. Roy. Soc. iN... 96, 73. ConoLty, J. R., 1965a. The stratigraphy of the Hervey Group in central New South Wales, J. Proc. Roy. Soc. N.S.W., 98, I, 37-83 Cono.tiy, J. R., 1965b. Petrology and origin of the Hervey Group, Upper Devonian, central New South Wales, J. Geol. Soc. Aust., 12, 125. ConoLiy, J. R., 1965c. The Upper Devonian rocks of the Lachlan Geosyncline in ‘‘ The Geology of N-S.W..", J..Geol. Soc. Aust., (im: press). Guiass, H. D., 1958. Clay mineralogy of Pennsylvanian sediments in southern Illinois, Nat. Acad. Sci.— Nat. Res. Council Pub., 566, 227. 120 GRIM, R. E., 1951. red and green shales, /. 21, 226. Jackson, M. L., Wuittic, L. D., and PENNINGTON, The depositional environment of Sedimentary Petrology., R. P., 1950. Segregation procedure for the mineralogical analysis of soils. Sozl Sci. Amer. Pyoc., 14, 77. jouns. W. D... Grim, Ihe... and BRADY, SW. be, 1954. Quantitative estimates of clay miunerals by diffraction methods, /. Sedimentary Petrology, 24, 242. KELLER, W. D., 1953. Illite and montmorillonite in green sedimentary rocks, J. Sedimentary Petrology, 23, 3. LoucGuNaN, F. C., Grim, R. E., and VERNET, J., 1962. Weathering of some Triassic shales in the Sydney area, J. Geol. Soc. Aust., 8, 245. Murray, H. H., 1954. Genesis of clay minerals in some Pennsylvanian shales of Indiana and Illinois, Nat. Acad. Sci— Nat. Res. Council Pub., 327, 46. JOHN H. CONOLLY PoTTER, P. E., and Grass, H. D., 1958. Petrology® and sedimentation of the Pennsylvanian sediments in southern Illinois—A vertical profile, Ill. State Geol. Surv. Rept., 204. SCHULTZ, L. G., 1960. Quantitative X-ray determina- tions of some aluminous clay minerals in rocks, Proc. 7th Nat. Conf.on Clays and Clay Minerals, 216. SIEVER, R., and Potter, P. E., 1956. ~Sources' ‘of basal Pennsylvanian sediments in the Eastern Interior Basin, J. Geol., 64, 317. Smoot, T. M., 1960. Clay mineralogy of Pre-Penn- sylvanian sandstones and shales of the Illinois Basin. Part I. Relation of permeability to clay mineral suites, J1l. State Geol. Surv., Circ. 286. VLODARSKAYA, V. R., 1964. Distribution of clay minerals in Paleozoic and Mesozoic rocks, in connection with their origin, Internat. Geology Rev., 6, 1305. WEAVER, C. E., 1958. Geologic interpretation of argillaceous sediments. I. Origin and _ signifi- cance of clay minerals in sedimentary rocks, Bull. Amer. Assoc. Petvol. Geol., 42, 254. Journal and Proceedings, Royal Society of New South Wales, Vol. 98, pp. 121-132, 1965 Photographic Observations of Double Stars kK. P. Sims Sydney Observatory, Sydney ABSTRACT—Photographic measures are given of 152 double stars. The internal mean error of a measure from one plate is +0”-020 in each of the rectangular coordinates in which the measures were made. may be neglected. This series of double star measures depends on photographs taken with the Melbourne astrographic objective (scale 59”-32/mm) to 1956 September 10 and thereafter with the Sydney lens (scale 59”-76/mm). Each plate has a row of about 16 exposures at the centre of the plate with the telescope moved about 0’-5 in declination between exposures. Orientation is obtained by taking one exposure with the telescope 4’-1 west of the central position and another immediately afterward with the telescope an equal amount east of the central position. These distances are set by lines in the eyepiece graticule. The movement between exposures is effected by means of the quick motion in hour angle. An orientation pair of this kind is taken both before and after the central series. The two values of orientation, obtained separately from these pairs, always agree to an accuracy better than is required for the position angle of the doubles except when the telescope has been bumped during the operations. These plates were rejected. The exposures have been regulated in each case to give a satisfactory image of the double. The first plate taken on any double has extra exposures of varying lengths and if unsatis- factory it has been rejected and a new exposure time estimated from these extra exposures. To keep the exposures from becoming too long, that is greater than about 30 seconds, or too short a variety of emulsions have been used. Table I lists for the emulsions used the photographic magnitude to which satis- factory images can be obtained in 30 seconds, the mean error in one coordinate of the measurement on a single image and the number of plates on which the conclusion rests. Measurements on an artificial double star indicate that photographic effects The plates were all measured in rectangular coordinates on a long screw measuring machine by Hilger and Watts. After measurement of all images in one coordinate the plate is turned through a right angle for measurement of the other. Measurement is also done in the reverse direction for each coordinate. The measure- TABLE I Mean Emulsion Type Mag Error Plates Kodak Lantern on 6:0 0-072 15 Process, Kodak or Ilford ae 7:8 0-061 146 Ordinary, Ilford 9-0 0-070 17 Ordinary, Kodak .. 9°3 0-098 188 Rapid Process, Ilford (Experimental) 9-5 0-069 38 Zenith Astronomical, Ilford 9-8 0: 083 6 ments of the orientation-pairs give the trans- formation which is used to refer all the results to the equatorial coordinates of the time. The standard mean error of Ax and Ay from a single image has been found for each plate. The average mean error thus determined was --0"-087 (1-5) for Ax and -+0"-082 (1-4u) for Ay. For the average number of images measured on a plate the standard error for the result derived from all images of the plate was +0”:020 in Ax and -+-0”-019 in Ay. The errors may also be estimated by comparing the results from different plates for the same star and the mean error so derived is +0” :028 in each coordinate. This estimate rests on examination of the results from 304 plates. 122 KP, The only error of the measuring machine which has been taken into account is the periodic error of the screw. Progressive error of the screw, non perpendicularity of the ways and inaccurate orientation between the axis of the measuring screw and the bisecting line were all considered and could not, in any case, give rise to errors appreciable in the above mean errors. Similarly the effect of differential atmospheric refraction is negligible. All of the plates were taken near the meridian and the effect was calculated for the most un- favourable cases and always found less than a quarter of the mean error for a plate. Magnitude equation has been avoided by selecting pairs for the programme which do not differ too much in magnitude. For the wider pairs (i.e. d > 10”) a difference of a little over one magnitude has been permitted and for close pairs, where overexposed primary and underexposed companion might give rise to photographic effects, the difference has been kept below 0™-5. Table II shows the result of an attempt to correlate the mean error with the magnitude difference and it is clear that the correlation is not strong. Two coarse diffraction gratings, with constant 2:5 and 3-7 magnitudes respectively, now exist to assist with this problem. TABLE: IT Mean Internal Error Am for Plate Plates 0-0 < Am < 0-4 0-022 133 0-4 < Am < 0°9 0-018 59 0-9 < Am 0-021 48 Since the plates were taken without a filter the possible effect of atmospheric dispersion must be considered. -194 - 240 -124 -535 -602 -566 228 140 »244 -380 *357 -822 *812 -848 -591 -582 -309 -293 -384 -902 -994 -942 -939 -909 -7197 -290 -401 » 202 -271 -934 - 843 -922 -872 -164 -272 -358 398 371 -469 -410 -397 - 206 -251 -237 *877 -900 -894 -620 -679 »494 © = nA NPN ~ nan = A nn NNN nen & DNA On DN aA nun Dn NHNHM NywW DNA DYNA owns nnes & gn . NES He NNN . A Zou - bs Wd un® Ynn WOW Nyy FH yoy Woe wn nun ~ n NNyw h3686 ‘Hu1376 A18 h3715 h3735 h3763 h3765 A22 Hd77 Argl2 h3830 A26 h3871 A32 h3898 4 PHOTOGRAPHIC OBSERVATIONS OF DOUBLE STARS 40-4 42-9 48-7 56°9 09-8 23-4 26:4 28-1 35°5 01-2 12-0 30°3 38:9 49-1 61 44 53 49 32 43 19 42 20 25 28 65 29 38 56 24 28 38 36 01 28 30 23 29 01 40 30 33 07 TABLE I[V—continued Epoch -760 -023 - 823 -755 -749 -843 -853 S00 -820 -733 -023 064 -870 - 766 - 804 -009 -050 -796 -080 -744 -812 -080 - 766 -804 -769 - 760 -061 -064 -870 -094 -124 -091 -843 -124 -080 “119 -820 -818 -820 -812 -843 -184 *821 -141 -124 °121 -119 -184 -195 m.e€.X. m.e.y. aiieoric) Store) Soe S (= )Kon) SS ooo SoS ooo ooo Sa) -083 -133 -072 -O77 -056 -046 -094 102 -126 -145 -083 075 046 -038 -126 -126 -100 -092 -065 -073 -154 -115 °095 -091 -050 -072 -072 -110 °057 °055 -060 -061 -086 -038 -107 -134 -102 -152 -129 °123 -101 ‘101 °077 »042 *037 °043 -107 -078 -067 ooo SoS oooceo oo ooo ooo ooo of Soo ooaoooeo soee oSeSsewocaoe -068 -083 -034 ‘Ill -060 - 062 -059 *095 -098 -087 079 083 -038 *054 -122 - 166 -084 -088 -065 *051 104 107 °095 -102 -087 -056 -060 -083 -046 -037 *037 *054 -066 -070 *115 Lt -091 - 160 - 160 tt -113 - 067 -076 °031 °037 °032 -107 -086 °052 20 20 23 118- 118- 118- 353° 353° 354: Part hi IT pT ES 310: -00 311 310: bo bo bo 28 58 16 » 268 *272 - 296 » 234 *319 -273 * 229 - 280 -271 *321 -400 -443 -409 *447 *874 -882 -847 -106 -164 -176 -948 -946 -669 *712 -420 -431 -434 -389 -138 ‘O71 -994 -517 -539 -674 -308 -325 -348 *622 *722 *626 °737 -652 -680 -914 -899 *926 -654 -628 -634 125 © = GEE = a Dy UNH YOM Byew Ons nity wun Mn ~ ~ nZe 2 - HEEN nn AS YS vow ow NWN ~ Snns NXrNy~ . . nnn Nas sslesec mes Rept Nan § NyWNn . zzz NNN ~ Aw x Nn Kiy pet wun 2 2" nan . 126 Rmk6 h3966 A49 HNI9 h4031 A63 h4080 Brs3 h4093 h4109 Cor76 Rmk9 h4162 h4166 h4172 h4185 K.- B SIMS TABLE [V—continued 7 18- feral Ne 1 25° 7 30- 8 06: 8 15- 8 15- 8 22: 8 39- 0 52 37 31 60 42 46 44 38 76 47 58 21 33 25 07 06 39 43 44 21 37 12 00 63 38 Epoch 58°119 58-152 58-215 57-163 58-141 59-138 59-149 60-171 61-163 61-215 61-138 61-163 61-179 55-223 57-163 59° 215 58-141 59-215 60-184 60-171 60-184 54-165 54-223 57-258 60-242 56-226 56-272 58-154 58-206 59-280 59-264 60-143 60-231 54-226 54-245 57-198 58-150 59-150 59-195 56-226 57-258 60-171 58-154 59-147 60-231 58-269 60-171 54-166 54-247 55-223 Mme:%. Mme.y No. 0:077 0-077 20 0-080 0-077 22 0-041 0-054 21 0-027 0-027 20 0-054 0-046 21 0-058 0-069 21 0-092 0-054. 27 0-033 0-056 23 0-086 0-081 23 0-058 0-058 23 0-062 0-051 25 0-052 0-032 25 0-044 0-064 21 0-054 0-058 20 0-080 0-096 22 0-034 0-038 20 0-054 0-042 23 0-046 0-023 20 0-029 0-022 21 0-044 0-044 24 0-055 0-058 22 0-118 0-110 14 0-133 0-122 15 0-104 0-100 17 0-098 0-069 20 0-129 0-110 23 0-126 0-133 19 0-069 0-042 19 0-050 0-042 20 0-040 0-032 20 0-061 0-058 23 0-058 0-087 21 0-038 0-037 20 0-106 0-133 14 0-064 0-133 13 0-100 0-115 20 0-054 0-061 22 0-034 0-065 21 0-046 0-038 22 0-118 0-122 20 0-073 0-065 20 0-087 0-061 22 0-054 0-058 22 0-042 0-042 21 0-031 0-035 20 0-084 0-058 20 0-058 0-064 23 0-056 0-087 14 0-133 0-068 14 0-126 0-110 20 152: 152: 152: 219- 219- 245- 244- 243- WS 4 Oowoe ole oie o) loner) Oooo oO CU Ot CEU ON bo bo bo So) or gor) 00 GO CO Or Or Cr Ot Or St -009 -916 -052 *327 -350 -288 °337 -306 -968 -940 »994 -942 °017 -595 -621 -713 *315 -336 -333 -574 -582 -767 744 837 -780 -212 -194 -114 -178 -150 -047 -004 -978 -555 -588 624 140 -124 -142 541 -468 -449 199 -796 -791 -818 -794 -590 -629 -568 © < 24% ee? ~ z= ~ On nn DN Sno Yn Hy pWW WWW WOW pn Woy BWW BDH nnw” wn BWW BWW _pRWD TY Soho h nea bo td te a N eae ~ <3 ~ 2 Was ~ - NAY AAS ~ ~ NNN Bmw NAY Oe nw nA DAN PHOTOGRAPHIC OBSERVATIONS OF DOUBLE STARS 137 TABLE [V—continued Name R.A. Dec. S. Epoch Te GsX: mee.y. No. oy d. O, M h m ie) 4 5 oO uw Rmk10 9 16-7 69 23 57-335 0-050 0-046 21 18-40 10-452 S, B 58-152 0-046 0-065 19 18-14 10-473 S, B h4224 9 31-7 30 47 57-316 0-100 0-080 20 116-49 7:420 R, B 58-150 0-130 0-065 20 116-90 7°388 S, B 61-256 0-094 0-076 20 117-06 7:457 R, B h4232 9 35-3 57-05 59-269 0-050 0-058 22 302-37 10-870 W, B 60-231 0-025 0-035 20 302-30 10-920 R, B 60-324 0-041 0-025 23 302-22 10-871 WwW, B h4235 9 37-7 50 42 54-247 0-152 0-102 14 87-22 5: 236 R, S$ 56 - 226 0-148 0-102 23 87-72 5-162 oh h4249 9 44-5 34 33 56-321 0-126 0-091 20 122-84 4-267 R, B 56-335 0-079 0-038 21 122-26 4-300 S, B 58-152 0-054 0-050 23 122-12 4-331 S, B R132 9 47-0 57 05 54-245 0-087 0-125 14 162-88 7-028 WwW, S 56-264 0-118 0-079 16 162-87 7-048 KS h4301 10 10-9 65 13 54-226 0-170 0-122 14 25-60 6-862 S$; 5 54-280 0-164 0-118 14 25-97 6-878 Ww, Ss 56-272 0-114 0-118 24 25-40 6-785 este) 59-360 0-065 0-088 21 25-34 6-864 ee) Cor103 10 24-3 52-03 57-332 0-088 0-069 20 287-71 5: 647 R, B 58-152 0-107 0-096 24 286 - 60 5-660 > SB 59-324 0-119 0-080 22 286-88 5-612 S, B h4324 10 25-9 46 50 57-324 0-069 0-046 20 244-89 8-270 hs es 8: 59-155 0-100 0-069 22 245-46 8-310 S, B Pz 10 27-7 44 33 58-294 0-054 0-058 20 217-88 13-510 5 5 60-321 0-026 0-043 24 218-34 13-580 Sys 60-327 0-043 0-029 21 218-30 13-549 S, B A91 10 29-4 71 36 57-199 0-096 0-115 21 60-12 9-986 S, B 57-256 0-042 0-069 19 59-40 10-003 W, B 57-316 0-104 0-092 21 60-00 9-988 R, B A97 10 39-4 60 39 55-302 0-110 0-160 20 173-45 12-320 W, 5S 55-382 0-106 0-098 21 173-38 12-354 35 58-324 0-100 0-130 20 173-87 12-316 Ww, S Corl17 10 45-0 41 03 58-245 0-080 0-058 18 176-50 6-308 R, B 60-308 0-083 0-048 21 177-78 6-335 R, B 60-354 0-048 0-058 22 177:°48 6-271 Sab h4399 10 58-3 59 59 56-319 +0-174 +0-156 20 311-44 8-698 Ww, 5S 56-335 0-106 0-114 21 311-20 8-714 Sey 59-310 0-096 0-088 19 310-28 8-766 59 60-343 0-089 0-090 22 310-46 8-780 w,s h4412 11 05-2 29-04 57-199 0-107 0-080 20 266-28 12-614 5,5 57-324 0-080 0-092 21 265-94 12-583 Sas 57-351 0-088 0-061 22 266-16 12-588 W, B R165 11 08-5 46 31 55-343 0-064 0-075 23 67-46 3°328 oF SD 55-382 0-102 0-075 21 67-30 3-391 eS) 59-310 0-058 0-073 20 67-53 3-358 Soo Brs6 11 23-8 42 07 58-382 0-084 0-069 22 166-80 13-156 WwW, B 58-406 0-054 0-058 22 166-41 13-004 W, B 59-116 0-058 0-073 20 167-24 13-108 W, B 128 K. P. SIMS TABLE IV—continued Name R.A Dec. S. Epoch ae Weve, ¢ Tey No. p. h m oe h4446 11 27-2 51 54 59-341 0-069 0-074 22 298-20 59-403 0-084 0-095 20 297-98 60-354 0-098 0-101 21 298-19 HITI96 11 27-3 28 43 57-199 0-069 0-069 21 210-40 57-316 0-100 0-107 19 210-34 57-393 0-054 0-042 21 209-85 59-310 0-058 0-061 22 209-72 h4460 ll 34- 57 11 54-341 0-087 0-087 14 175-48 55-414 0-110 0-114 20 175-40 57-210 0-115 0-111 20 176-42 58-379 0-092 0-088 24 176-54 Hwe70 11 34- 36 53 57-406 0-073 0-077 21 104-86 59-349 0-054 0-051 21 106-30 A116 11] 51- 31 43 59-360 0-054 0-065 21 262-06 60-327 0-035 0-031 23 262-06 60-354 0-046 0-031 22 262-18 h4481 11 52: 21 59 57-324 0-088 0-061 21 193-30 57-335 0-073 0-077 16 193-50 59-401 0-069 0-040 22 193-30 Corl133 ll 54: 62 13 56-379 0-126 0-156 20 21-18 57-346 0-088 0-096 20 21-38 h4487 11 55; 36 11 57-406 0-065 0-069 21 125-10 59-310 0-050 0-080 19 124-77 59-341 0-050 0-050 21 124-75 h4498 12 Ol- 65 09 59-338 0-058 0-058 14 59-74 59-365 0-050 0-050 23 59-66 59-368 0-034 0-050 20 59-60 h4507 12 O7- 44 20 54-210 0-178 0-145 15 222-40 56-234 0-114 0-133 20 222-02 57-351 0-104 0-111 19 222-04 60-401 0-072 0-084 21 222-18 Brs8 12 19- 57 34 57-412 0-034 0-034 20 334-34 58-360 0-069 0-069 24 334-46 59-349 0-038 0-054 20 334-93 h4522 12 19- 68 55 57-439 0-065 0-119 21 67-06 58-158 0-100 0-054 18 66-28 h4540 12 36- 72 14 59-384 0-130 0-152 21 166-53 59-439 0-109 0-095 20 167-03 59-442 0-069 0-101 22 166-44 h4545 12 39: 74 38 56-434 0-110 +0-098 24 192-22 56-472 0-145 0-160 21 191-54 57-346 0-126 0-168 21 . 192-12 57-351 0-142 0-160 20 191-54 A127 12 53- 55 22 57-406 0-107 0-115 23 125-67 57-425 0-154 0-096 20 125-92 h4563 12 55- 33 05 57-412 0-069 0-074 20 237-20 58-158 0-104 0-061 18 237-42 59-155 0-058 0-046 20 236-96 Corl47 12 57- 59 04 54-365 0-061 0-046 15 356 - 04 57-119 0-080 0-088 20 355-76 10-369 — S) aS QO Se OO OO GO OO CO GO OOO wo fer) —_ —_ — OOO — a Ko) © NAW Phe nn ~ nenw NNN Ww 47 vuw DH WWW OY god non WW WWW ynwnn BWW WOW pe YUN DW eH YVyYn WWW nunw ie Aan NNN ~ nae pop dz ann vy ~ YQ pn 248% ~ - An nnn ~ PHOTOGRAPHIC OBSERVATION ON DOUBLE STARS 129 TABLE 1V—continued Name R.A. Dec. S. Epoch 6.x, m.e.y. No. p. d. O. M h m fe) 7 Oo “” Cor156 13 28-4 60 45 54-453 0-137 0-072 15 171-46 14-611 Wr 5 55-341 0-118 0-151 20 171-72 14-623 WwW, B HN69 13 31-3 25 59 55-414 0-075 0-068 21 190-24 10-062 Ses) 55-486 0-057 0-075 21 190-62 10-087 > 58-155 0-058 0-073 21 191-06 10-121 So h4608 13 36-6 33 28 55-341 0-038 0-072 20 185-31 4+ 267 WwW, B 55-414 0-042 0-068 21 185-52 4-318 Sp 58-155 0-031 0-061 20 186-24 4-362 S, B HIII101 13 46-1 32 30 58-152 0-092 0-092 21 106-62 8-116 S, B 58-226 0-050 0-034 21 106-47 8-014 W, B 59-147 0-073 0-058 20 106-74 7-966 S, B Brs9 13 48-3 50 12 59-499 0-090 0-094 21 76-28 17-599 WwW, 5S : 60-401 0-121 0-126 21 76-36 17-629 W,S 60-434 0-101 0-094 22 76-11 17-616 Ww, S h4626 13 49-7 69 50 55-131 0-102 0-118 20 55-69 4-559 RS 56-262 0-142 0-160 19 55-23 4-443 3, 9 57-403 0-137 0-087 17 55-88 4-432 WwW, S A151 13 50-7 55 33 57-428 0-077 0-096 23 47-34 26-422 WwW, B 59-384 0-040 0-042 20 48-65 26-900 R, B 59-439 0-077 0-055 22 48-60 27-167 R, B h4647 14 01-1 47 50 60-163 0-069 0-077 22 294-68 10-968 hee 60-434 0-081 0-073 21 294-94 10-936 Ww, S 60-477 0-074 0-066 20 295-06 10-960 R55 h4661 14 06-3 28 25 54-182 0-220 0-122 15 230-24 4-381 W,S 57-423 0-154 0-107 20 229-99 4-490 Wes 60-513 0-069 0-052 20 230-41 4-548 R, B A159 14 15-4 58 00 57-428 0-092 0-092 21 158-77 9-210 WwW, 5S 58-464 0-073 0-065 24 158-88 9-191 W,S 58-516 0-080 0-073 21 158-57 9-184 W,S Gls204 14 17-9 67 02 56-314 0-098 0-060 21 324-22 12-476 S, B 59-442 0-077 0-061 23 324-30 12-398 W, B h4683 14 26-7 62 50 54-373 0-098 0-126 15 61-85 13-142 R, S 60-163 0-093 0-086 21 62-10 13-275 See) 60-513 0-097 0-077 20 62-16 13-324 ies Hwe75 14 31-0 37 06 57:161 0-104 0-107 20 214-98 4-118 WwW, B 57-502 0-054 0-042 23 215-36 4-178 S, B h4706 14 44-6 47 00 55-486 0-080 0-065 20 219-84 6-651 S, B 56-570 0-064 0-083 20 219-38 6-719 S, B h4727 14 57-6 27 27 54-226 0-083 0-110 14 38-56 7-424 Sie 55-565 0:075 0-106 21 38-80 7-505 5, 9 Cor178 15 03-8 40 38 58-207 +0-077 +0-058 20 75-64 4-946 S, B 60-163 0-053 0-051 22 75 + 62 4+922 S, B h4743 15 05-8 32 27 54-172 0-141 0-160 13 196-54 11-059 =: 54-191 0-166 0-102 14 196-56 11-094 W,S Cor179 15 06-7 36 52 54-202 0-110 0-087 14 227-94 6-572 R, S 54-221 0-110 0-182 14 227-46 6-586 els tS) 56-549 0-091 0-106 21 228-24 6-453 WwW, S 57-565 0-073 0-054 U7 227-39 6-458 Seo 130 Name R.A h m A187 15 26:5 Pz 15 50-5 Hwesl 15 54-0 Brsll 16 03-2 h4837 16 05-4 h4840 16 10-9 HV134 16 14-2 HV124 ~ 16 14-7 h4848 16 17-5 HN39 16 18-4 Cor206 16 55-2 h4916 17 00-9 h4921 17 02-9 A213 17 02-9 h589 17 04-7 Sh243 17 09-2 HITI25 17 11-9 Cor221 17 43-0 33 35 32 43 34 19 19 32 50 49 31 46 24 26 24 31 40) 48 23 23 34 49 53 58 01 20 33 37 49 27 11 58 Epoch 54: 54: 57: 59- 59: 54: 54: 57 54: 54: 60- 54: 56: 55: 56: 55° 56- 58> 54: 54: Di: 60- 55° 56- 58: 54: 55° 57: 58: 59° 60- 60- 55° 55: 56- 54: 55° 34: 54: 56: 56: 57: 58: 59- 59° 55° 55° 210 226 199 265 579 224 570 -369 59- 60- 598 229 265 377 280 224 235 245 262 245 262 598 227 570 565 242 243 565 270 557 237 369 636 579 590 625 606 650 549 279 284 570 625 262 570 584 551 262 631 628 658 m.e.X. ooo oo ooo eo } oo -148 - 224 084 -033 - 064 189 110 065 050 054 125 152 -106 “1295 -126 -129 -126 ‘079 -072 100 137 068 061 -041 -060 -065 -069 106 079 -080 -092 -073 -074 -063 -072 -075 096 -087 -133 -069 -063 064 -098 -092 -054 -042 -053 - 160 133 K. P. SIMS TABLE [1V—continued m.eny: SO SS0° S€o660 102-21 102-36 298-81 298-80 333-17 333-04 p—_ nw | Oo = - nn NM “ NNN ne Wn wn nn nnn & - nn = . Nn ns A su . qn Zn Sy De BCH NNHNYHD HH WYN gt By unn wnuw BD2ON NUN NH WH NHnwHW BHD HH BOW uw ~ . LY NNN A eke nA A222 Brsl4 h5094 h5092 h5117 h5151 Rmk25 A230 h5223 h5246 h5251 h5261 h5288 h5325 18 18 19 ig 19 1 20 20 20 21 21 21 21 22 PHOTOGRAPHIC OBSERVATIONS OF DOUBLE STARS 26: 54: 06- 06- 44- 06- 43- 03° 05- 28: 36: Dec. S. re) 30 40 38 37 34 47 44 37 57 40 56 54 23 86 38 73 ih 32 27 48 01 32 05 09 16 30 46 59 31 TABLE [V—continued Epoch 56- 56- 54: 55° 55° 58: 58- 58: 55° 55> 56- 58: 54: 56: 58: 58- 54: 56- 56: 55: 57- 59: 54° 54: 56- 56- 58: 56- 56: 59- 60- 56- ou 58: 55° 56- 56- 57- 55> 56- 58 - 56- 60- 55- 55: 58-6 56: 60- 60- 311 675 631 284 303 341 636 694 300 650 320 677 631 675 325 688 650 377 680 m.e€.X. Se com) ie¢) ie) 2Sooe Ser> See i=) on S Sa Seqeo SS) — bo for) =) —_ (ey) ~J Sooo Ses Seas) ooo — let =) iY) = ~] ee) (o.6) © oso > __ —_ a Tey, Sa SoS oo — _— [oe ) (anya) (=) SoS Sooo > Soe S or TS Soe — juan S SoS S co — oooo Ss Je) ie.2) o.oo —_ — vo} oo oS 20 20 20 267: 267- 267- -992 -047 -725 -672 “lol -364 -380 -364 -794 -822 -790 -800 22- -318 474 -486 OO G8 Go O&O LO 872 -874 - 844 “811 -856 19 -935 774 -753 -474 -446 “411 -851 -760 -814 -728 -021 -117 -138 -549 -575 -554 -677 -758 7B he -762 -872 -066 -904 -897 -941 -959 -858 -962 ° nn . HAZE gey - ~ NNNMN ~ ning a ~ DN S . ae a cs ~ NNW dit ght . Pies . a NNM wy Wn DOW whe wy an ~ NNN . - ~ ~ - 4 drive ny . ~ nn == nmmnnn - no “ 131 = NN nun 132 K. P. SIMS TABLE IV—continued Name Inge Dec. S. Epoch im.e.X. m.e.y. No. p- d. h m fe) / ie} uw Jcl9 22 18-7 41 57 55-514 0-160 0-091 20 73°69 24-498 58-806 0-065 0-077 19 73-30 24-°120 59-809 0-051 0-052 21 73°23 23° 928 Cor251 22 21-4 40 57 59-765 0-092 0-086 22 183-90 6-492 59-844 0-117 0-082 21 184-10 6-490 h5366 22 46-8 43 19 59-817 0-080 0-075 22 251-54 14-896 60-680 0-071 0-074 22 251-75 14-856 60-852 0-063 0-048 19 251-58 14-802 h5371 22 52-3 26 38 55-514 0-166 0-166 20 343-54 9-038 60-852 0-052 0-031 24 343-95 9-192 h5382 22 59-2 51 54 60-781 0-061 0-091 19 51-32 7-670 60-861 0-083 0-079 21 51-12 7-673 A246 23 01-5 51 14 53-768 0-079 0-076 14 255-97 8-494 54-489 0-087 0-110 14 255-67 8-478 55-506 0-064 0-064 20 256-35 8-528 55+ 833 0-075 0-083 21 255-98 8-587 h3184 23 15-7 19 05 58-877 0-058 0-087 22 284-29 5-424 60-852 0-071 0-066 26 284-17 5+ 246 HII24 23 40-8 19 14 55+ 852 0-091 0-064 20 135-50 6-503 56-549 0-137 0-133 21 135-32 6-566 58-538 0-065 0-077 20 135-92 6-586 60-681 0-052 0-049 22 135-70 6-630 Cor261 23 42-2 61 04 58-877 0-079 0-041 20 100-54 5-661 59-844 0-051 0-047 22 100-76 5-726 60-861 0-052 0-044 20 101-10 5-670 A253 23 49-2 27 36 55-888 0-094 0-046 23 270-22 6-588 56-550 0-156 0-087 20 270-10 6-521 Arg46 23 54-4 27 05 53-806 0-128 0-104 13 169-18 10-607 53-818 0-079 0-083 14 168-98 10-574 O = NNN ~ oun ~ NNW nu ~ 2 ~ a NN WS ~ a ~ N ~ ~ ~ ~ nNnnN a ~ = a ~ ~ nn nO BW tywW DHWW WW YVMNuNM HWY WH WHHYM ww vsueles) Sn Journal and Proceedings, Royal Society of New South Wales, Vol. 98, pp. 133-137, 1965 Minor Planets Observed at Sydney Observatory during 1964 W. H. ROBERTSON Sydney Observatory, Sydney The following observations of minor planets were made photographically at Sydney Observa- tory with the 9-inch Taylor, Taylor and Hobson lens. Observations were confined to those with southern declinations in the Ephemerides of Minor Planets published by the Institute of Theoretical Astronomy at Leningrad. On each plate two exposures, separated in declination by approximately 0’:5, were taken with an interval of about 20 minutes between them. The beginnings and endings of the exposures were automatically recorded on a chronograph by a contact on the shutter. Rectangular coordinates of both images of the minor planet and three reference stars were measured in direct and reversed positions of the plate on a long screw measuring machine. The usual three star dependence reduction retaining second order terms in the differences of the equatorial coordinates was used. Proper motions, when they were available, were applied plate. Each exposure was reduced separately in order to provide a check by comparing the difference between the two positions with the motion derived from the ephemeris. The tabulated results are means of the two positions at the average time except in cases 1760, 1774 where each result is from only one image owing to a failure in timing the other exposure. No correction has been applied for aberration, light time or parallax but in Table I are given the factors which give the parallax correction when divided by the distance. The serial numbers follow on from those of a previous paper (Robertson, 1965). The observers named in Table II are W. H. Robertson (R), K. P. Sims (S) and H. W. Wood (W). The measure- ments were made by Mrs. J. Brannigan and Miss E. Hardaker who have also assisted in the computation. Reference | ROBERTSON, W. H., 1965. J. Roy. Soc. N.S.W., 97, to bring the star positions to the epoch of the 177. Sydney Observatory Papers, No. 49. TABLE I R.A. Dec. Parallax (1950-0) (1950-0) Factors No. Planet U.T h m S ie eg s a 1677 12 1964 July 27 - 64473 21 46 44-18 +04 58 59-2 +0-02 —5:-5 1678 12 1964 Aug. 20-54849 21 29 16-36 +04 22 11-5 —0-04 —5-4 1679 16 1964 July 21-62872 20 49 04-17 —15 43 38-8 +0:04 —2:-7 1680 16 1964 July 27-61680 20 44 19-73 —16 O7 52-8 +0:06 —2-7 1681 22 1964 May 21-58388 15 31 35-47 —15 26 32-0 +0:-07 —2-6 1682 36 1964 July 30 - 63940 20 52 46-50 —42 32 53-4 +0°18 +1-1 1683 54 1964 March 19-53401 10 56 32-66 —05 06 10-4 —0:03 —4-2 1684 54 1964 March 23-53601 10 53 03-07 —04 51 58-2 +0:02 —4-2 1685 65 1964 July 21-62872 20 47 47-94 —15 12 24-6 +0°04 —2-8 1686 65 1964 July 27-61680 20 43 32-19 —15 34 13-1 +0:07 —2-8 1687 92 1964 July O07 - 67552 20 52 40-31 —22 38 08-8 +0:-06 —1-7 1688 92 1964 July 22-62221 20 42 38-42 —24 08 34-1 +0:-04 —1-5 1689 106 1964 Sept. 17-57990 23 43 «454-50 —09 13 05-0 0-00 —3-7 1690 106 1964 Sept. 29 -54595 23 34 53-86 —09 56 17-6 +0:-02 —3-6 1691 112 1964 May 21-53013 14 23 44-72 —18 44 08-1 +0:°05 —2°3 1692 118 1964 May 04 - 66296 16 18 50-59 —23 47 59-9 +0:07 —1:-5 1693 122 1964 July 29-59618 20 21 59-30 —17 29 42-5 +0:-07 —2-5 1694 130 1964 Aug. 20-58472 22 37 27-99 —13 51 31:8 +0:-08 —3-0 1695 130 1964 Sept. 15-50125 22 21 13-60 —19 39 24-7 —0:09 —1-8 1696 131 1964 May 04 - 66296 16 31 42-46 —20 50 22:5 +0:-04 —2-0 1697 131 1964 May 18- 63862 16 19 22-70 —20 59 10-8 +0-11 —2-0 1698 154 1964 July 08 -53229 17 29 47-61 —48 29 00-7 +0:-08 —2-2 1699 174 1964 Sept. 17-55300 22 33 35:88 —03 17 05-8 +0:-07 —4:-5 134 No. 1700 1701 1702 1703 1704 1705 1706 1707 1708 1709 1710 1711 1712 1713 1714 1715 1716 1717 1718 1719 1720 1721 1722 1723 1724 1725 1726 1727 1728 1729 1730 1731 1732 1733 1734 1735 1736 1737 1738 1739 1740 1741 1742 1743 1744 1745 1746 1747 1748 1749 1750 1751 1752 1753 1754 1755 1756 1757 1758 1759 1760 1761 1762 1763 Planet 174 200 200 202 202 206 206 210 210 216 216 224 224 234 234 242 259 261 261 264 264 306 306 308 308 312 312 312 322 323 323 324 324 337 356 362 362 372 372 375 384 387 387 409 409 420 420 426 426 454 454 469 469 503 503 505 505 536 536 554 554 559 559 606 W. H. ROBERTSON TABLE I—continued 1964 1964 1964 1964 1964 1964 1964 1964 1964 1964 1964 1964 1964 1964 1964 1964 1964 1964 1964 1964 1964 1964 1964 1964 1964 1964 1964 1964 1964 1964 1964 1964 1964 1964 1964 1964 1964 1964 1964 1964 1964 1964 1964 1964 1964 1964 1964 1964 1964 1964 1964 1964 1964 1964 1964 1964 1964 1964 1964 1964 1964 1964 1964 1964 10d ie Sept. April May June July May June Dept. Sept. March April April May July Aug. Apri July sept. Sept. April May April May March April March April April May July Aug. May June April July May June May June June May Nov. Dec. June July May May March April April April May May Oct. Oct. Aug. Sept. July Sept. March April July Aug. July R.A (1950-0) bh Sm Ss -49999 22 28 22-74 - 63024 15 10 03-05 -54410 14 46 24-22 -61138 18° 23 923253 -57276 1S ag 502 - 64800 17 23 07-34 -51116 16 50 09-77 -57990 23 39 03-80 - 54595 23 28 47-11 - 60974 12 557 35509 -60186 12 44 35-37 -68198 14 57 10-84 -54550 14 25 32-06 - 56948 19°32 ©2229 -51314 19 21 08-36 -61963 13 37 04-96 -59718 18 34 38-08 -57990 23 30 59-81 - 54595 23 20) 20271 - 65930 15 04 26-34 - 54330 14 34 22-11 - 66294 15 438 36-16 - 55964 15 19 17-80 -68305 12 54 05-96 -59288 12 43 30-36 - 66974 13 05 40-55 -63012 12° 53 «26:05 - 58864 12 47 45-24 -58710 ts 86> 55°13 - 59864 20 11 38-14 -54112 19 51 30-80 -61502 16 27 56-60 -50508 15 50 17-60 -55173 12 48 50-32 -64878 21 O01 21-76 -61264 15 55 13-84 - 54472 15 43 50-43 - 62030 15 52 09-30 -53068 15 28 01-78 - 63422 19 18 18-01 -62611 15 29 45-56 - 63866 03 33 = 18-62 -47956 03 O7 49-82 - 66092 19 44 58-46 - 54576 19 20 04-64 - 66296 16 29 19-36 - 63862 16 19 53-72 - 56639 ll 31 02-57 -55140 11 18 20-90 - 62660 13 56 45-66 -55977 13 31 24-69 -65734 16 54 15-66 - 64352 16 47 59-32 - 54925 23 56 07-90 - 50652 23 49 43-71 - 66756 22 35 24-80 - 52370 22 04 52-34 -67406 PM Wn yi = Way iota) -51909 21 10 32°55 - 59372 12 09 02-93 - 58394 11 56 16-16 -64956 20 40 38:56 - 52476 20 11 51-79 -67520 21 29 15-44 aomnmor"6OS 0 PONOWAR EK ANAGSCHOW HRA WOM WD WON ADORONTEWOWEHODWOWNNWRODNDNOCDHORG Parallax Factors Ss —0:02 —4: +0:02 —0O-: +0:02 —l- +0-11 —2: +0:06 —2: +0:03 —2: 0-00 —2:- +0:-01 —3:- +0:03 —3:- —0:07 —3: +0:06 —3- +0:08 —l- +0:02 —l- +0:02 —4- 0:00 —3:- +0:05 —3- +0:-12 —l- +0:03 —8: +0:05 —3: +0:04 —2: +0:04 —3: +0:05 —4-: +0:02 —4: +0:-17 —4-: +0:04 —4: +0:10 —3: +0:-12 —3- +0:06 —3 +0:05 —l +0:03 +0 +0:03 +1 +0:04 +0 +0:08 +0 +0:-12 —3: +0:09 —l +0-1ll —l- +0:01 —0O +0-1l +2 +0:04 +2 +0:03 +1 +0:06 —2 +0:09 —3 —0:09 —3 +0:04 —3- —0:03 —3 +0:05 —l +0-11 —l1- —0:01 —l +0:09 —l —0:01 —3 +0:07 —3 +0:06 +1 +0:10 +0 0:00 —3 —0:05 —3 +0:13 —l +0:-05 —l +0:20 +1 +0:02 +1 +0:-03 —4 +0°:14 —4 +0-01 —2 —0:02 —l +0:11 —2: u ANOWH MH HK TIDSOCANIGDSHOSDH OW WAOHDSOH WRI MNISSORWOWOOSOHDHNOHHWAHUIANS NOTPR DOR OP MINOR PLANETS OBSERVED AT SYDNEY OBSERVATORY DURING 1964 135 TABLE I—continued R.A. Dec. Parallax (1950-0) (1950-0) Factors No. Planet Ua. h m S a ” Ss ‘ 1764 606 1964 Sept. 03- 49395 20 49 13-47 —16 19 21-0 —0:01 —2-6 1765 639 1964 June 01-57348 16 26 22-34 —28 23 17-3 +0-01 —0-8 1766 654 1964 March 17-58046 12 14 57-56 —39 27 11-8 —0-:09 +0°8 1767 654. 1964 April 01-57708 11 58 58-12 —38 29 02-9 +0:10 +0-7 1768 670 1964 July 08 - 60346 19 31 32-69 —10 32 28-4 +0:02 —3:5 1769 670 1964 Aug. 05-51544 19 09 00-74 —12 16 45-4 +0:03 —3-2 1770 690 1964 June 02- 67343 18 52 25-76 —17 27 01-2 +0:01 —2:-5 1771 690 1964 July 08-56610 18 24 47-99 —15 53 40-7 +0:05 —2-7 1772 695 1964 April 08-55937 12 22 14-56 —25 03 40-1 +0:03 —1-3 1773 714 1964 June 02-64430 18 02 03-72 —12 09 26-9 +0-03 —3-2 1774 714 1964 July 07 - 56372 17 30 30-74 —-09 37 03-7 +0:-14 —3-6 1775 736 1964 Sept. 17-57990 23 40 31-28 —08 29 04-8 +0-01 —3-8 1776 736 1964 Sept. 29- 54595 23 31 32-43 —09 55 08-2 +0:03 —3-6 1777 746 1964 Aug. 05 - 59230 20 30 59-32 —44 40 57-4 +0:13 +1:-6 1778 772 1964 Nov. 03- 59492 02 24 21-09 -—08 40 12-4 +0:-10 —3-8 1779 772 1964 Nov. 23 - 46200 02 06 38-53 --O7 22 16-2 —0°10 —3-9 1780 773 1964 March 23-63864 13. 35 «442-19 —32 56 23-6 —0:02 —0-l1 1781 773 1964 April 09-58578 13. 20 07-06 —33 24 07-9 0-00 0-0 1782 791 1964 July 21-62872 20 56 40-04 —15 43 41-9 +0:02 —2:-7 1783 791 1964 July 27-61680 20 52 37-86 —l16 43 24-6 +0-05 —2-6 1784 791 1964 Aug. 12-56496 20 41 08-42 —19 25 34-0 +0:05 —2-2 1785 796 1964 April 09-61945 13. 42 56-08 --05 52 23-8 +0:05 —4-1 1786 798 1964 May 13-58025 15 09 11-20 —13 46 24-4 +0:04 —3-0 1787 804 1964 June 04- 68497 19 16 46-70 —45 17 16-8 +0-02 +1-8 1788 804 1964 July 06 - 60622 18 44 15-96 --46 14 50-7 +0°16 +1-4 1789 818 1964 Aug. 11-63125 21 52 45-34 —-35 56 31-8 +0-11 +0°3 1790 818 1964 Sept. 08-52928 21 30 25-85 —37 13 06-5 +0:-07 +0°5 1791 850 1964 Aug. 04- 64363 21 51 16-53 —-20 48 03-0 +0:07 —2-0 1792 905 1964 Sept. 29 - 54595 23 31 «441-53 —-10 35 42-8 +0-03 —3-5 1793 924 1964 Aug. 12-63723 21 54 34-79 —l10 56 56-8 +0-11 —3-4 1794 924 1964 Sept. 01-55040 21 40 20-49 —13 32 12-3 +0:04 —3-0 1795 936 1964 July 08 - 64956 20 36 22-36 —?21 50 29-8 +0:02 —1-8 1796 936 1964 Aug. 12-52476 20 09 45-07 —23 37 10-7 —0-O01 —1-6 1797 984 1964 July 07 -67552 20 50 11-91 —21 42 07-9 +0:07 —1-9 1798 984 1964 Aug. 11-58910 20 17 53-10 —21 18 14-4 +0:03 —1:-9 1799 1093 1964 June 01- 60922 17 25 32-88 —39 44 14-5 —0-01 +0-9 1800 1093 1964 June 29-54571 16 50° 10-57 —43 56 16-1 +0-18 +1-4 1801 1095 1964 Oct. 01-58221 00 19 17-23 —13 08 21-2 +0-05 —3-1 1802 1102 1964 June 04- 60590 17 27 12-83 —0O7 02 28-5 0-00 —3-9 1803 1132 1964 June 29 - 64756 19 49 14-94 —35 28 00-2 +0:05 +0°3 1804 1132 1964 July 06- 65229 19 44 04-27 —36 04 20-4 +0°15 +0:-2 1805 1244 1964 March 19-61647 12 52 11-14 —22 39 34-4 —0:03 —1-7 1806 1244 1964 April 08-59529 12 33 56-72 —21 09 10-4 +0-12 —2-0 1807 1334 1964 Aug. 12-60346 21 33 37-25 —l16 42 56-8 +0:05 —2-6 1808 784 1964 July 07 - 63966 20 14 O1-18 —40 57 21-6 +0:°04 +1-1 1809 784 1964 July 27-58756 19 53 51-16 —41 19 19-5 +0-11 +1-1 1810 784 1964 Aug. 05 - 55440 19 45 43-97 —40 58 02-8 +0:°09 +1-1 1811 784 1964 Aug. 11-54947 19 41 17-74 —4)) 34 10-8 +0:-15 +0-9 TABLE I] No. Comparison Stars Dependences 1677 Yale 20 7607, 7611, 7630 0:41844 0- 27164 0- 30992 Ww 1678 Yale 20 7525, 7529, 7542 0-34113 0- 48394 0- 17494 =) 1679 Yale 12 I 7846, 7862, 7870 0-62281 0-19430 0: 18289 S 1680 Yale 12 1 7813, 7827, 7828 0- 25141 0: 45676 0-29183 WwW 136 W. H. ROBERTSON TABLE II—continued Comparison Stars Cape 12 17 17 12 12 14 14 16 11 12 14 12 12 13 13 13 Ere, 17 Ly 13 14 Jia 13 13 13 19 I 5695, 5705, 5713 . D. 15076, 15106, Cape Z. 19122 4180, 4184, 4192 4160, 4163, 4182 I 7842, 7847, 7853 I 7801, 7817, 7827 14488, 14496, 14524 14366, 14397, 14420 8391, 8394, 8405 8229, 8240, 16 8363 II 6019, 6038, 12 I 5364 11437, 11451, 11462 I 7671, 7677, 7695 I 8426, 8431, 8446 I 9491, 9499, 72 II 9500 I 6785, 6789, 6804 I 6739, 6767, 12 II 6753 16751, 16820, 16953 7838, 7839, 7853 7814, 7822, 7827 II 95438, 9566, 9577 10617, 10647, 10653 I 6740, €745, 6768 I 6673, 6685, 6725 I 6235, 6249, 6258 I 6035, 6046, 6066 8368, 8372, 8390 8330, 8338, 8341 4648, 4657, 4668 4607, 4609, 4621 10727, 10747, 10758 10417, 10455, 10468 6805, 6828, 6830 6761, 6769, 6775 4834, 4859, 4860 II 12091, 14 12932, 12944 8217, 8238, 16 8348 8170, 8177, 8182 I 5554, 5573, 5581 5117, 5121, 5139 5489, 5493, 5509 5353, 5368, 5375 4705, 4716, 4717 4664, 4675, 4683 4724, 4733, 4737 4672, 4680, 4681 4642, 4646, 4666 11066, 11079, 11095 10484, 10516, 10522 14517, 14549, 14551 8139, 8165, 8175 7831, 7838, 7869 4616, 4631, 4643 II 13833, 13880, 14 14575 II 9990, 10016, 10038 II 9873, 9895, 9916 6098, 6117, 6153 LPIF 3201, 3214, 3229 Cord. Yale Yale Yale Yale Yale Yale Yale D. 14194, 14215, 14233 II 6400, 6425, 6431 833, 843, 861 TLS TNO 13d 6925, 6926, 6932 6699, 6702, 6727 11498, 11519, 13 I 6782 I 6754, 6759, 6767 -34357 44328 -40212 -31834 -15794 -19555 -42390 - 16065 - 20528 -43028 * 34347 -43083 °48581 -35991 -41112 - 20279 *31330 -42762 -17549 51924 -31728 -37831 24536 - 24926 -40526 - 54236 -47654 -38919 » 23937 *34139 *44598 *38993 - 25416 - 28873 29000 56755 - 75533 -46687 - 25594 28709 - 20461 - 29359 -12157 - 32936 73017 -16921 -50651 -42765 *52977 -67183 -44730 -43095 -31834 22914 26929 49367 35788 -54816 -40343 35294 - 26174 - 25042 -54516 - 30624 37709 - 35068 Dependences -21797 * 23598 -30458 - 22332 52185 30592 32803 55127 55355 -38167 - 30667 -33155 - 30749 - 32945 °45278 *44954 -40193 - 28184 -39583 - 08254 42730 27694 45188 -§2122 °40493 - 26200 - 34559 » 24828 -39767 - 28982 -21516 - 16410 » 24354 *38255 - 25861 -52059 -01759 -40885 -51098 - 26601 -38136 -43558 - 53553 °40855 -98017 *30951 -18551 -40011 - 25007 -09118 - 28338 - 17466 -41982 -O9111 *41567 - 33466 -35651 15166 30204 27824 - 24071 -49634 -19112 -30381 -39124 -50823 SSIS SSS aS) -43846 -32074 - 29330 -45834 -32021 -49852 24807 28808 24117 -18805 34986 - 23762 - 20670 -31064 - 13611 - 34767 - 28477 - 29054 -42868 - 39822 25542 34475 30276 » 22953 18981 19564 17787 - 36253 - 36296 - 36879 -33886 -44597 50230 32872 45139 08814 26226 - 12428 - 23308 -44690 -41403 - 27084 -34291 - 26209 -71034 -52128 30798 -17223 - 22016 - 23699 - 26932 - 39439 - 26185 -67975 -31504 17 167 - 28561 -30018 29453 36882 49754 25324 - 26372 - 38995 - 23166 -14108 ZAVPAAAAADDYO DEV SH SAM SEV ENS SV SADV SEV RONEN EZ DVUVAEVENUNUH Sg seaDV swe WON SE dUAdse MINOR PLANETS OBSERVED AT SYDNEY OBSERVATORY DURING 1964 Yale Yale Yale Yale Cord. Cord. Yale Yale Yale Yale Cord. Cord. Yale Yale Yale Yale Yale Yale Yale Cape Cape Yale Yale Yale Yale Yale Yale Yale Yale Yale Cord. Yale Yale Cape Cape Yale Yale Yale Yale Yale Cord. Cord. Cape Cape Yale Yale Yale Yale Yale Yale Yale Yale Cape Cord. Yale Yale Cape Cape Yale Yale Yale Cord. Cord. Cord. D. Cord. D. 14 14 16 16 D. D. 16 16 14 13 1B D. 17 17 13 14 12 12 13 18 18 11 11 12 12 14 i 16 16 11 1Be 16 16 17 17 12 12 12 17 Ll IDX Dp; 18 18 13 11 Il 12 14 14 13 13 18 D. EE 16 18 18 14 12 12 D. DD: D TABLE IIl—continued Comparison Stars Dependences ee 4828, 4829, 4848 11954, 11955, 11991 11780, 11843, Cape 18 8330 8433, 8440, 8449 8408, 8419, 8429 15304, 15315, 15316 II 143879, 14409, 14 15082 15469, 15534, 15545 15239, 15280, 15296 4510, 4524, 4535 4455, 4457, 4468 I 8853, 8888, 8912 14025, 14065, 14067 I 8088, 8096, 8113 I 7845, 7846, 7871 II 10283, 10308, 10339 5784, 5785, 5812 5651, 5656, 5674 6844, 6868, 6873 6648, 6653, 6662 I 6981, 6984, 7003 I 6749, 6775, 6782 9350, 9378, 9384 6148, 6152, 6170 5933, 5934, 5952 8372, 8377, 8390 8216, 8222, 8229 14866, 14904, 14914 529, 537, 554 452, 458, 465 6898, 6912, 6936 6752, 6761, 6782 I 7880, 7906, 7908 I 7866, 7871, 7886 II 8870, 8903, 13 I 8878 4920, 4931, 4936 5300, 5317, 5321 14166, 14167, 14254 13748, 13799, 13844 11233, 11235, 11269 11068, 11094, 11108 I 9333, 9340, 9360 8208, 8222, 8230 7770, 7771, 7794 I 8150, 11 7703, 7714 14320, 14355, 13 I 8850 14025, 14028, 14065 I 8943, 8970, 14 14479 I 8698, 8707, 8731 8725, 8745, 8765 11845, 11846, 11941 50, 59, 12 I 89 5915, 5921, 5939 10252, 10317, 17 10825 10242, 10252, 10267 9629, 9645, 9652 II 5442, 5445, 5463 I 8120, 8123, 8134 14720, 14728, 14746 14534, 14549, 14565 14464, 14466, 14498 14432, 14441, 14457 eoooqooeceecocnoeoooooooooooocrcoqooococmcoSeee }& -41825 °43017 - 26024 -15134 - 27249 - 29407 *31594 -34417 - 28167 °19357 - 29470 - 26101 -42694 -33743 > 30187 19289 -32788 -38785 - 25845 45563 - 15982 41008 48747 -35911 48870 41659 - 19756 - 34603 -31340 -42253 - 20238 - 26121 -39761 -34978 -32484 - 23122 -38151 - 22379 > 29007 - 24475 - 23073 -37909 - 24511 - 21689 *27787 * 22954 -38778 37813 - 39669 25614 -32954 -42402 -51298 -41926 - 20548 - 28351 - 36742 -53988 - 34576 21960 -08275 23820 40039 -31563 - 18863 qoqoocoooooqoooooqoooooocoococqcooqooocoo$c -49742 -17695 -31164 -40621 -45638 » 25652 -46389 -45922 - 20061 -44364 * 22792 -11624 - 34404 -32431 -40248 - 31620 -44374 - 21388 - 36629 - 16492 - 21858 - 18066 -43671 - 32229 -40404 -37231 31235 -47182 36594 58983 28073 29193 -38491 -44796 ooocococooooooooqooooocoocococoocooorocmhnée“e - 27289 -31073 -46849 -41408 -31130 - 28488 - 23193 -38782 - 28176 -31730 -44773 -45849 - 29439 -43593 -35716 -33343 *35755 -35510 *43285 - 18062 -40032 - 35244 - 28634 - 25678 - 22342 - 34203 -46796 - 30477 -30187 -33823 -40736 - 24137 °42544 -33858 - 26895 -31240 -36197 31232 - 25071 - 55464 - 32563 -39299 - 63864 -43907 -39782 - 36798 - 29602 -17813 -38942 °37757 -50554 -35740 -30635 -14403 -47223 31245 26027 14777 - 18242 41446 -32741 48107 30768 - 29946 -36341 PARZEVESEZP DVO BV EV ERO AAA EDV EN EV EAD RAVER a SWWEM SHVOON dens DH EN EUS 137 7 ; y i : f OFFICERS FOR 1965-1966 fae a Ba gee eee eas ‘Président eye 9 pea te , UA. AL DAY) Bsse, Bb ie Ayan gniicon en : mo ae Vice: Presidents sere ae . | ae Ww. Pauibariis. Bearer ee. Fem NS cats her POCCENDOREF, B.Sc. Agr. pee a ere RN. ‘MSc. Sle ae ws Ee J. W, Le eg ee D.Sc., F.R.S., F.A.A. Honorary Secretaries Bs REICHEL, Ph.D., en ta ke a %, ; : a : id Honorary Pressured be ree. og F. CONAGHAN, M.Sc. eas i ; Members of Council se eran Ne A. BURG, Parte 4 hehe ah J. MIDDLEHURST, msc. F. A. HARPER, msc. De cere Ke Tee BROWN GN GN ETA DS) asec: KEANE, Ph.D., M.Sc. | faa W. H. ROBERTSON, B:sc. his “A KITAMURA, B.A., B.Sc.Agr. A eR day SEAN TON, «Ph.D. a2 eee BED SH es A. UNGAR, Dr.ing. : he a i Es f "s So a 2 % 5 ae "The so Sucidey) et New South “Wales shipdeatal’ in 1921 as. the " : Philosophical Society i a Nee Australasia’; after an interval of inactivity it was resuscitated in 1850 under the name of the nase ae “ Australian Philosophical Society ’’, by which title it was known until 1856, when the name was changed to the “‘ Philosophical. Society of New South Wales ’’, In 1866, by the sanction of Her “Most Gracious Majesty Queen Victoria, the Society assumed its present title, and was mee voted : by Act wb Parliament of New ‘South, Wales in Sass 3 e x ij? ve = . o# N 5 hs ; i bs LA yh A t % , hg R ‘ pl ( ols Sp 1 1 bys Bae sd i shi / ; if ‘ be 7 ( J j “sy pees {Vt ti f ; ? f M Bel i + , ng 4s r Yy iy : . \ | ; nf ; r ¥ i co » ) he > Mey. Fi . StS adit i ‘ belt) , ‘ ( x —s ¥ ~ > Kono ae Nae \ : y Bek in hE Poste by ~ = “fi j . + . BOP AO i ws an Piabdate. of £ Weights ae Measures. ce Ww. Humphries iy 139 Bene i emati¢ ty i Sciences in \ the one World. Ww. B. Smith-White . eres 145 | ny ie ; “4 m0 | : 5 | ax : a i H vee iG ‘ Hy 7 ‘ Forces, in Lossy, Blectromagnetic Systems. WwW. E. Smith . ¢ 151. Be Spee a ei Se See eet = Canowindra. Bast Area, N. s w. 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HUMPHRIES* Presidential Address, 1965 During the course of this address it is proposed to discuss the origin, development and present status of some units and standards of weights and measures. Generally attention will be directed towards those units and standards which have been the concern of the English peoples, but because the Metric System is firmly established in science and technology, and is now assuming an ever-increasing 1m- portance in trade, some time must be devoted to a description of this System as well. Units and Standards of Measurement It is important to distinguish between units and standards of measurement. A umt of measurement is an abstract con- ception and cannot be used as the practical basis of a measurement until it has been defined and realized in one of two ways; either by reference to arbitrary material standards or by reference to natural phenomena, including physical or atomic constants, physical ‘ situa- tions ’ and the properties of specified substances. In general, a unit is fixed by definition and is independent of such physical conditions as temperature. Examples are the yard, the pound, the gallon, the metre, the gramme. A standard is a physical embodiment of a unit. In general it is not independent of physical conditions, and it is a true embodiment of the unit only under specified conditions, e.g. a yard standard has a length of one yard when at some definite temperature and supported in a certain manner. If supported in a different manner it might have to be at a different temperature in order to have a length of one yard. Early History The history of weights and measures goes back into antiquity—how far back we do not know, but according to some authorities there is tenuous evidence to show that weights and * Division of Applied Physics, National Standards Laboratory, C.S.I.R.O., University Grounds, City Road, Chippendale, N.S.W., Australia, A measures were in use in Sumeria and Egypt as early as 7000 B.c. As man emerged from the pre-civilized state of self-sufficiency as a hunter for food and clothing, he began to specialize in elemental crafts such as the making of tools and weapons, growing crops, weaving, making pottery, and the working of metals. Over a very long period of time and from these primitive beginnings arose the necessity for means to measure. Many are of the opinion that the units first used by primitive man were those of length, followed by the appreciation of two-dimensional area and three-dimensional bulk. The early established standards of length were derived from limb measurements and are familiar in their developed form in the ancient Egyptian system of measures. The more abstract idea of mass or weight undoubtedly took longer to dawn on _ the intelligence of early man. The earliest units of weight included weights of kernels of grain and the weight of shells. Before the crudest weighing instrument was devised the process of hefting or lifting an object to assess its weight was probably in use. Weighing with the balance ranks amongst the few really fundamental inventions of pre-historic times and is equally important to our civilization as the wheel and axle, the lever and the screw. . ! Our present knowledge of weights: and measures comes from many sources. Some early standards have been recovered by arche- ologists and are now preserved in museums. The comparison of the dimensions of buildings with the descriptions of contemporary: writers is another source of information, e.g. a fairly accurate idea of the length of the Attic foot used by the Greeks has been obtained by comparing the dimensions of the Parthenon with the description given by Plutarch. By studying evidence from all available sources we are able to gain some idea of the origin 140 and development of the units. We find that the changes have been gradual because of the large number of modifying influences. Origin and Development of some Common Units One of the earliest units was the foot. At first this was the length of the unspecified human foot, later it was the length of the foot of the tribal chief or head of state. Not unnaturally its length has varied. In ancient times 1t was somewhat more than 12 inches but by the time the Greeks arrived it was 114 inches. The foot was brought to Britain by the Romans and was finally defined in Britain as one-third of the yard during the reign of Edward I. The date is believed to be about 1305. An important unit of length used by many ancient peoples was the cudzt, originally defined as the distance from elbow to the tip of the middle finger. About 4000 B.c. the Egyptian cubit was established at a length equal to 18-24 modern English inches. Some authorities claim that it was deduced from measurements of the quarter meridian of the earth. This unit was common to Babylonia, Egypt and later to Assyria. It probably originated in Chaldea. The Egyptian foot was created as a more convenient unit and was made equal to two-thirds of a cubit, or 12-16 inches. Other cubits were later established arbitrarily. Notable among these was the Egyptian Royal cubit of 20-64 inches. Egyptian standards passed to Greece and became known as the Olympic standards. The inch was originally a thumb’s breadth. In the Roman duodecimal system it was defined as one-twelfth of a foot and as such was introduced into Britain during the occupation. The mile was defined by the Romans as 1000 paces, the pace being equal to 5 Roman feet. This Roman mile when introduced into Britain became 5000 English feet and in Tudor times was changed to 5280 feet. The yard is of much later origin than the units previously mentioned and appears to have a double origin. In Northern Europe it was the length of the girdle worn by the Anglo-Saxons, whilst in southern countries it was the double cubit. There is an old tradition that Henry I decreed that the yard should be the distance from the tip of his nose to the end of his tumb. One of the earliest of the units of mass or weight was the gvai, and it is interesting to note that it is a unit which has remained common to several systems of weights and J. W. HUMPHRIES measures throughout the ages. Its origin was probably the weight of a grain of wheat or barley. The early Egyptian units of weight are of considerable interest since they were the fore- runners to some extent of the modern Metric System in that the units of length and mass were inter-related. The talent was the weight of an Egyptian royal cubic foot of water and was divided into 3000 shekels. Its weight was 93-65 pounds, making the shekel 218-5 grains, exactly half the ounce of Plantagenet times. The Roman pound (libra) contained 12 ounces (unciae, meaning twelfth parts) of 437 grains each, i.e. the Roman ounce was equal to two Egyptian shekels. This pound was introduced into Britain where it suffered many changes. Eventually during the reign of Elizabeth I, in 1587, two pounds were legalized, viz. the troy pound and the avoirdupois pound. The Elizabethan avoirdupois pound was larger than the Roman pound and contained 16 ounces each of 437-5 grains, the same as the present standard. The idea of a pound divided into sixteen parts was not a new one as the Greeks had divided their pound into sixteen parts as well as into twelve parts. The history of the pound weight is a fascinat- ing one and is worthy of tracing in more detail. In later Saxon times the Marc of Cologne was introduced, probably to serve as a standard for the minting of coinage as the 12-ounce Roman pound was already established for trade. With the Norman Conquest, in 1066, the Saxon pound became the Tower or London pound containing 12 ounces each of 450 grains. From the Tower pound were coined 240 silver pennies each of 224 grains giving 5400 grains to the pound. Apparently this pound became inconveniently small for trading purposes and we find that an additional ‘ merchants’ ’ pound of 15 tower ounces was in use towards the end of the 13th century. (The exact date of its introduction is uncertain: it may have been in 1266 during the reign of Henry III but 1303, in the reign of Edward I, is considered the more likely.) In addition to the merchants’ pound the ‘avoirdupois’ pound, intended originally for the weighing of wool, came into use and was legalized by Edward III in 1340. This pound contained 16 ounces each of 437 grains, making a pound of 6992 grains; this pound corresponded exactly with one used in Florence. The ‘troy’ system had become established in France (the name is derived from the French SOME UNITS AND STANDARDS OF WEIGHTS AND MEASURES town of Troyes) and this too came into use in England. The value adopted after 1414 was a troy pound of 5760 grains containing 12 troy ounces, each of 480 grains. At about the same time the pound used by the German merchants of the Hanseatic League was also coming into use in England. It was the largest one yet and contained 16 tower ounces making 7200 grains. Henry VII, in 1497, authorized yet another ‘merchants’’ pound of 16 troy ounces, equal to 7680 grains. The only other change was that made by Queen Elizabeth in 1587, when the value of the avoirdupois pound was adjusted to its present value of 7000 grains. The various weights which have been in commercial use in England may be summarized thus : Period Name of Pound Until 1527 .. Tower or London Until 1527 . Merchants’ 1340-1587 ae .. Avoirdupois Mainly after 1414 2 Lroy Mainly after 1527 . Hanseatic Merchants’ 1497 onwards . Henry VII Merchants’ 1587 onwards . Queen Elizabeth avoirdupois The Elizabethan standards of mass and length were to remain the legal English standards for 237 years (1587-1824). During the intervening years several attempts were made to establish the troy pound as the pre-eminent standard but this did not materialize until 1824. The troy pound which then became the legal standard (the term Imperial Standard was used for the first time) was one which had been made in 1758. This standard weight, along with the other Imperial Standards were irreparably damaged in the fire which destroyed the Houses of Parliament in 1834. New standards were prepared and finally legalized in 1855, but instead of the Troy pound of 5760 grains, the Avoirdupois pound of 7000 grains was constituted the ‘ Imperial ’ measure of weight. The Troy pound, although no longer the primary standard, continued a weight of the realm until the passing of the Weights and Measures Act in 1878, when it was abolished, and the decimal multiples and sub-multiples of the Troy ounce substituted. At this juncture it will be convenient to leave the Imperial System temporarily and introduce the Metric System. AA 141 The Metric System The Metric System is the international decimal system of weights and measures based on the metre and the kilogramme. Although its origin is generally associated with the French Revolution it really stems fiom _ proposals dating back to 1670 and earlier. For many centuries the kings of France and their ministers had striven in vain against the use of a bewildering variety of weights and measures. They failed for two reasons. One was the general and ingrained opposition to change, the other, the resistance of the seigneurs or petty rulers in the provinces who foresaw that the proposals would prevent them from using two standards with increased profit to themselves. Units varied from province to province and even from town to town; they No. of Grains Equivalent in Pound 12 tower oz. (450 gr.) 5400 15 tower oz. 6750 16 avoirdupois oz. (437 gr.) 6992 12 troy oz. (480 gr.) 5760 16 tower oz. or 7200 15 troy oz. 16 troy oz. 7680 16 avoirdupois oz. 7000 (437-5 gr.) varied greatly even within the same province, e.g. in Maine—Loire there were 110 different measures for corn alone; in the Nord there were 21 varieties of the pound weight. In eighteenth century France, with the largest population in Europe and engaged mainly in agricultural and domestic industry, the situa- tion could only be described as chaotic. The first effective step towards the formulation and establishment of a national system of weights and measures in decimal notation was taken in France within a year of the Revolution in 1789. The essential features of the system were embodied in a report made to the National Assembly by the Paris Academy of Sciences in 1791. The system became legal in 1795, but its adoption was very slow, and it was not until 1837 that a decree was passed making the use of other than the decimal metric measures a penal offence. Towards the middle of last century, during a period of increasing industrialization and expansion of foreign trade, it was recognized that some sort of international agreement was necessary in the field of physical measurement. In 1864 the metric system was legalized in 142 England for use in contracts, but not in trade ; in 1867 a convention of the International Geodetic Association recommended the inter- national use of the metric system in geodetic work, and advocated the construction of a new European prototype metre to be available for international use, under the supervision of an international bureau ; in 1872 an International Commission, convened by the French Govern- ment, met at Paris and supported the recommendations of the Geodetic Association. Finally the Treaty of the Metre was signed in 1875 by representatives of 17 countries (there are now 38 member nations). This treaty provided international agreement on the bases for the metric system, and established the International Bureau of Weights and Measures (the, B:I.P.M.) at Sévres. near Paris. It is interesting to recall that England was not one of the signatories: the Warden of the Standards was a delegate to the 1872 Commission, but was not allowed to participate in subsequent events because ‘ Her Mayjesty’s Government declared that they could not recommend to Parliament any expenditure connected with the metric system, which is not legalized in this country, nor in support of a permanent institution established in a foreign country for its encouragement. They have consequently declined to take part in the Convention or to contribute to the expenses of the new Metric Bureau, and have directed the Warden of the Standards to decline being appointed a member of the new International Committee or to take part in the direction of the new International Metric Bureau’. Great Britain joined the Metric Convention in 1884. Units and Standards of the Metric System At this stage it will be useful to remember that although the metric system is a decimal system, the words ‘ metric’ and ‘ decimal’ are not synonymous and care should be taken not to confuse the two terms. In the metric system the fundamental units are the metre and the kilogramme. The other units of length and mass, as well as units of area, volume and units such as pressure are derived from these two fundamental units. The Metre. Originally it was intended that the metre should be one ten-millionth of the meridian quadrant, but during the course of the definitive measurements (made between Dunkirk and Barcelona) it was found that although the general shape of the Earth was that of an oblate spheroid, there were differences J. W. HUMPHRIES in the length of the meridians. Consequently a compromise had to be made so that ultimately the fundamental unit of length became arbitrary and the doctrinaire egalitarianism that had once inspired the revolutionary reformers to measure the meridian common to all men and base upon it a universal system of weights and measures had to be quietly forgotten. The material standard resulting from these initial endeavours is the Metre des Archives. It is a platinum bar, 25 mm by 4 mm in section and constitutes an end standard (i.e. the definitive length is the distance between the end faces of the bar). The present international metric standard of length is the International Prototype Metre. This bar, one of several made for the Inter- national Bureau of Weights and Measures between 1872 and 1880, was selected after precise measurements indicated that it was of the same length as the Metre of the Archives. It is an alloy of platinum-iridium (90% Pt, 10% Ir) and is of a special X-form section designed by Tresca to give maximum rigidity in relation to its weight. Two transverse lines are cut on the neutral plane of the bar towards its ends. The Metre was defined as the distance between these lines when the bar is at a temperature of 0°C and supported in a special manner. The Kilogramme. It was also the intention of the originators of the Metric System that the units of length and mass be inter-related and that this end be achieved by taking the unit of mass to be equal to the mass of one cubic decimetre of distilled water at its maximum density. (35) This is the basic result of the paper. The right-hand side will be expressed in terms of terminal parameters which are directly measurable irrespective of the details of the internal meshes. The simple form of equation (35) is due in part to the involvement of the combination {(F,jav+(Fx)av} rather than (/’,)ay alone. In general (F,)ay and (Fy)ay, the force obtained by reversing the relative phases of all exciting currents, are slightly different. Referring to equations (31) and (32) it is seen that the first contribution involving (@Z(%)/dx) is not changed. However, the terms from the coupling to the internal meshes are not equivalent, and 20 (F,)av—(F av} =It (AX/8x) (I) —Im’*) +t (dX/ax)(Io*—I0"). .. 2 ae (36) Use of equation (17) in equation (36) gives 20of (F,)av—(F)av} =J1Ot [Xf (Ze) + (Zo) -* }(OX7/Ax) —(0X/dx){(Z)3A+(ZM)VIXTHIO) ee. (37) The matrix in the square brackets on the right-hand side of equation (37) is seen to be skew symmetric, so that (Fav =(F’y)ay oye) Je) ee "eee © 0 8 0 (0) 0:10 1010) (eet elie: tele LontenisMectie (38) if all elements of I”) have the same or opposite phases. Of course equation (38) is also true for the trivial case of no internal mesh coupling, for which K=O ee visnlect.. eee (39) Returning to equation (35) it may be observed that this result resembles an earlier result, but the specializations of Section (2) and the particular choice of constants in the differentiation have ensured that there is no term involving the internal meshes explicitly. Use of equation (30) in equation (35) gives the terminal-impedance form of (Favt(Fiav}=AUIOn(OZ/Ax)IM} oo. eee. (40) a 2. =T(N)t (OX /ex\IO) ... 6. a (41) Were NK == F(Z). 18 o Boece a yidlie eos. cue es Weigel e ofa ats Say epee Renae te ne (42) is the terminal reactance matrix. For a single terminal-pair network equation (41) becomes simply (Fav =(2a)ERT(OM ex) 3 eee eee (43) where X is the reactance of the network and J the current flowing. The analysis has considered a single frequency of excitation. Should the system be simul- taneously excited at a number of frequencies the average forces from the individual components are additive, (2) and each may be evaluated separately. (4) Applications (4.1) Electromagnetic Levitation In recent years there has been interest in the levitation and melting of alloys and metals by the production of high-frequency eddy currents.) (®) The reaction of the eddy currents on the excitation coil produces the force used for levitation. The levitation force may be estimated crudely from the approximate theory of Okress and his collaborators,‘*) or more accurately from a detailed field solution if this is practicable.“ The field solution of Brisley and Thornton for a sphere on the axis of an axially symmetric coil-system"™) was used by Smith’) to show that in this case the levitation force may be written (Fav 2g OL jOx) ie. ue eR (44) AVERAGE FORCES IN LOSSY ELECTROMAGNETIC SYSTEMS 157 where L is the effective inductance of the coil, J the exciting current, and x the separation of the coil and sphere. Equation (44) leads to a procedure for predicting levitation forces from low-level impedance measurements. Equation (44) was also derived using a circuit-theory model of the eddy-current system, but the axial symmetry was important in obtaining the final result.‘ However, a system of the type considered in Sections (2) and (3) is appropriate as a model of electromagnetic levitation under more general conditions. Each of the internal meshes 1, 2,. . .” (no restriction on ”, which may be increased without limit) represents an eddy-current mesh and their excitation is caused by inductive coupling to the excitation coils. The conditions (a) and (0) of Section (2) are clearly appropriate and the results of Section (3) give the levitation force (F,)ayv if x is the vertical coordinate of the levitated body. The term in (dZ(%)/dx) in equation (31) would be zero unless the levitated body were magnetic. In the usual levitation experiment a single coil is used and equation (43) gives the levitation force. Introduction of the effective inductance, | GL ea ne re ae ee ee a ee (45) gives equation (44) as an alternative form. Thus levitation forces may be deduced indirectly from low-level measurements of inductance changes. At the same time a measurement of the effective series resistance R introduced by the presence of the levitated material gives the heating /*JR to be expected. The amount of heat generated is very important in practice‘® and is controlled by a careful choice of frequency. Conversely, existing levitation measurements and calculations may be used to predict the effect of the presence of conducting bodies on the effective inductance of nearby coil systems. Electromagnetic levitation systems do not usually employ multiple coil systems excited by currents of arbitrary relative phases, but equation (41) is valid should they do so. (4.2) Moving-Iron Measuring Instruments A moving-iron measuring instrument may be represented by the same model as used for electromagnetic levitation in Section (4.1). Of course the object on which the force is exerted would normally be magnetic. For a two-terminal instrument equations (43) and (44) apply. For a multi-terminal instrument equation (41) must be used. Of course the derivation does not allow for non-linearity effects associated with hysteresis if ferromagnetic material is present. (4.3) Dynamometer Measuring Instruments Dynamometer type instruments are important in the laboratory for the measurement of voltages, currents or power, and as d.c./a.c. transfer instruments. The ideal operation may be described in terms of impedance, admittance or mutual inductance changes between circuits. (2) Careful design and construction eliminates any effects from electric forces, dielectric loss or ferro- magnetic materials, but there always remain perturbations from the generation of eddy currents. The results of Section (3) apply even when eddy currents are present, since the internal meshes account for eddy-current behaviour. Referring to equation (31), the generalized deflecting force (F,)ay is produced almost entirely by the first term involving (0Z(%)/dx). This term gives the ideal behaviour of the instrument, the remaining terms being small corrections for eddy-current effects. Likewise, (F,)ay and (Fy)av are very nearly equal, since from equations (36) or (37) any difference is due to eddy currents. Equation (41) may be used for finding the deflecting forces of (Fyav+(Feav} =I (@K/Ax)IM) occa (46) This equation may also be cast into inductance terms by the introduction of an effective terminal- inductance matrix giving E (Ee Nate lay —— LOMO ROX )LOND 5.3 cas «cts a ave ee are ars (48) From the definition of LE it is seen that the element L,, is the effective mutual inductance between terminal circuits A and B. Measurements of 0X/dx or OL/@x at the terminals may then be used for absolute calibration of these instruments.“ 158 W. E. SMITH’ (5) Conclusions It has been shown that for a particular class of networks the average generalized force (F,)ay may be written in terms of the dependence of terminal parameters on the generalized coordinate x. The networks chosen are shown to be appropriate models of the electromagnetic levitation of conductors, and of moving-iron or dynamometer measuring instruments. The results obtained are generalizations of previous work") ©) relating to loss-free or almost loss-free systems. When cast in terms of effective inductance the results are almost identical to magnetostatic results such as that given by equation (4). However, the inductances occurring in equation (44) and (48) are effective inductances at the excitation frequency, which allows for the complex internal eddy-current behaviour. | ! When applied to the electromagnetic levitation problem the results provide an alternative procedure for estimating levitation forces by low-level measurements of reactance. Alternatively, existing calculations of electromagnetic levitation forces provide information on inductance changes produced by the presence of conducting objects. An earlier investigation obtained equations (43) and (44) for the levitation of a sphere by an axially symmetric coil system, but it has now been shown that these equations are of general applicability. The application of equations (46) and (48) to moving-iron, and more importantly, dynamometer instruments, is of particular interest to measurements laboratories. In principle it allows absolute calibrations to be made in terms of previously established impedance standards. Measurements of the rates of change of reactance or effective inductance with x, together with the deflecting force (Fay provide an absolute measure of the exciting currents. Alternatively, measurements of the effective inductance derivatives at different frequencies give the frequency dependence of a measuring instrument. This is important for dynamometer instruments used as precision d.c./a.c. transfer instruments. It is important that the effects of losses, although small, be included since it is just such minor perturbations which give rise to d.c./a.c. transfer errors. By considering the limit as the excitation frequency @ is reduced to zero, it should be possible to estimate the d.c./a.c. transfer error from impedance measurements as an alternative to direct techniques such as that employed by Smith and Clothier.‘®? (6) References Cy SMITH, W. E.; 1960. Instn. Elect. Engrs. Mono- graph No. 366M. Proc. Instn. Elect. Engrs., C107, 228. @) SmMirn, /W." Ei,91961.. Aust. J. Phys: '4, 152: OWHITE,:| DiC. AND “WOODSON, H.- H-— 1958: “ Electromechanical Energy Conversion.” Wiley : New York. (4) Smith, W. E., 1965. Brite-f Appl. Phys., 16, 377. (5) OxrEss, E. C., WrRouGHTON, D. M., COMENETZz, C., Brace, P. H., AND JRE ES etd 19 a2» J. Appl. Phys., 23, 545, and errata 1413. (6) Rony, P. R., 1964. ‘‘ The Electromagnetic Levita- tion of Metals.’’ University of California Radiation Laboratory Report No. UCRL-1411. (7) BRISLEY, W., AND THORNTON, B. S., 1963. Brit. J. Appl. Phys.,;.¥4,, 682: (8) SMITH, W. E., AND CLOTHIER oo Wales 1954. Proc. Instn. Elect. Engrs., 101, II, 465. ; (Manuscript received 25th March, 1965) Journal and Proceedings, Royal Society of New South Wales, Vol. 98, pp. 159-167, 1965 The Marine Permian Formations of the Cracow District, Queensland Rosin Wass Department of Geology and Geophysics, University of Sydney ApstTract—In the extreme south-east of the Bowen Basin the basal Permian volcanics (Camboon Andesite) are immediately overlain by calcareous clastics, formerly regarded as one Formation (Oxtrack Formation of Derrington ef al., 1959) but considered herein, mainly on faunal grounds, to be divided by a disconformity to give two units :—Buffel Formation (Artinskian- Sakmarian in age) and Oxtrack Formation in a restricted sense (Kungurian-Kazanian) each with its distinct fauna. The greater part of the marine sequence near Cracow belongs to presumed equivalents of the Barfield and Flat Top Formations of the Theodore-Banana District, mainly non-calcareous strata of Lower Kazanian age. Fossil lists of all species, showing their local stratigraphic ranges, are given. Introduction The Cracow District, situated about 250 miles north-west of Brisbane, is in the extreme south-eastern portion of the Bowen Basin. A detailed study of the geology was made during 1961 and 1962 while the writer was at the University of Queensland. In early 1963 work by the writer for Utah Development Company in the Theodore-Banana district to the north of Cracow provided correlation with the Cracow section. Before 1961 the stratigraphical terms used in the area were those of Derrington ef al. (1959) who had mapped the area for Mines Administration Pty. Ltd. in 1954. Prior to this, Jensen (1926) and Denmead (1937, 1938) had discussed the marine Permian. Mack (1963) mapped a much larger area from Theodore to Narrabri, N.S.W. The. strati- graphical terms used by previous authors are revised in this paper. A perusal by the writer of the fossil collections in the University of Queensland from Cracow had shown that there were two very different faunas, both being found in the Oxtrack Formation (Derrington ef al., 1959). There seemed to be a possibility of an unrecognised disconformity falling within the Formation. Field studies with a view to elucidating the faunal break were carried out. The result of this was that the Oxtrack Formation was shown to contain two distinct lithological and palaeontological units in some places and in other places only one unit was present. In the writer’s opinion, Derrington ef al. have used the term Oxtrack Formation in two senses. In a restricted sense it refers to the section in Oxtrack Creek, the type locality of the Oxtrack Formation but in a wider B sense, their description of the distribution (“Narrow outcropping pattern from Cracow Homestead to Banana’’) refers to two units which the writer has termed Oxtrack Forma- tion (restricted sense) and Buffel Formation. The two Formations are readily distin- guished west of Rose’s Pride Mine and west of Cracow Homestead. To assist in current geological work in the Bowen Basin this paper is being published as an account of the stratigraphy of the marine Permian and is accompanied by short notes on the palaeontology. Systematic descriptions of new species will appear at a later date. Because of soil cover causing discontinuous outcrop an understanding of the geology of the district is largely dependent on an understanding of the palaeontology ; detailed descriptions of the various rock types present are not included. All map references refer to the Mundubbera 1: 253,440 military map. There are few geographic place names in the area and exact grid references are given in the text for additional accuracy. Stratigraphy The lowest Permian unit in the Cracow district is the Camboon Andesite (Derrington et al., 1959). In this paper the name is used in their sense. One notable addition to the knowledge of this unit is the presence of Glossopteris sp. in shales interbedded in the andesite indicating its Permian age. Because of the faunal assemblage in the overlying Formation the Camboon Andesite is regarded as Lower Permian. A new name, the Buffel Formation, is proposed for the lowest stratigraphical unit overlying the Camboon Andesite. 160 ROBIN WASS PALAEOZOIC GEOLOGY pee kilomebres LEGEND Gyranda Formation 2? Flat Top Formation ? Barfield Formation ZPucd Oxtrack Formation NPUeN Buffel Formation Camboon Andesite LOCALITY — — Geological Boundaries *—* Type Section A Strike & Dip —— Anticline ata Syncline >— Roads Gladstone > ---- Tracks Biloela > Creeks canes ® Mines Buffel Formation Synonymy : Lower Bowen (in part) Denmead, 1937 ; Lower Bowen Marine Beds (in part) Denmead, 1938; Oxtrack Formation (in part) Derrington e al., 1959; Back Creek Formation (in part) Mack, 1963. N.B.— The terms of Denmead (1937) are taken from the map legend (1937, p. 194) and those of Denmead (1938) from the text. Derivation: The name is derived from Buffel Hill, 32128447, 3,600 feet at 290 degrees from Cracow Homestead. Type Section: This outcrops from Buffel Hill, west to 32018441. Distribution: The Formation, which is found in places as a northerly trending belt through- out the Cracow district crops out in the southern part from south-west of Cracow Homestead to 1-8 miles south-east of the Orange Creek road crossing (32078526). It 1 Go/den ‘ l 5a Plateau a =~ 4% "& ym Zz Z HM is not found in the vicinity of the Theodore Road, near the Orange Creek road crossing (31868554). Outcrop is found north of a point, 1-2 miles north of the Orange Creek road crossing (31858573). There, the Forma- tion crops out on the eastern side of small, undulating hills. It does not occur in Oxtrack Creek, the type locality of the Oxtrack Formation. This is 15 miles north of Cracow. Lithology: Predominantly limestone and silt- stones with less amounts of subgreywacke, conglomerate, spiculite, and containing some concretions. In the type section the Formation consists mainly of fossiliferous limestones which grade upwards to spiculite, which in turn passes into siltstone with calcareous concretions. South of the type section the limestone becomes finer grained and darker but the upper lithologies are not exposed. MARINE PERMIAN FORMATIONS OF CRACOW DISTRICT, QUEENSLAND To the north of Buffel Hill the limestone outcrops for 1-7 miles (to 32138483) and is replaced along strike by calcareous siltstone. Northwards from a point 3:3 miles north of Buffel Hill (32138507) the siltstone fails to outcrop and along strike a calcareous petromictic orthoconglomerate appears at a point, 1-8 miles south-east of the Orange Creek road crossing (32078526). The conglo- merate is composed of andesite fragments set in a carbonate matrix. The fragments are similar to the Camboon Andesite and are considered to have been derived from the older unit. The limestone, calcareous silt- stone and conglomerate are all overlain by the spiculite. : The conglomerate is regarded as being part of the Buffel Formation because it occupies the same stratigraphic position as the lime- stone of the type locality, having the Cam- boon Andesite directly underlying it. It contains the same fauna as the limestone. Defining the conglomerate as a member of the Formation would be to no advantage. North of the Theodore Road, the lithology varies from calcareous subgreywacke to lime- stone. Northwards along strike the lithology becomes more calcareous and coarser grained till a conglomerate, similar to that described before, outcrops 0-8 miles north-north-west of Rose’s Pride Mine (31748601). The ande- sitic fragments here are much larger, being up to six inches in diameter with a mean diameter of 1-5 inches. Thickness: In the type section, a practically complete exposure is 640 feet thick. This comprises 270 feet of limestone, 350 feet of spiculite and approximately 20 feet of silt- stone with calcareous concretions. The thickness decreases to the north and at Rose’s Pride Mine, an approximate thickness of 75 feet is exposed. Structures: In general, the Buffel Formation dips west at angles between 12 and 35 degrees, but west of Cracow Homestead the Formation is folded into an asymmetrical syncline with a southerly plunge. The western limb dips at 40 degrees to the east. The strike of the Formation varies from 30 degrees west of north to 10 degrees east of nerth. Io the south of the area this variation increases. Stylolites and chert nodules, together with grain orientation are developed in the lime- stones of the type section. The stylolites are lensoidal and, in part, are parallel to BB 161 the bedding. Their lensoidal outline has some relation to the chert nodules for these are of the same shape. Stratigraphic Relationships : On faunal grounds, the Buffel Formation is considered by the writer to be disconformably overlain by the Oxtrack Formation (as found in Oxtrack Creek). Additional evidence to support this conclusion is gained from isopach maps of the Bowen Basin (Malone, 1964). The exact relationship of the Buffel Formation to the underlying Camboon Andesite is not known, but it may be one of disconformity. This tentative conclusion is reached because of the change from a volcanic to a carbonate facies and because of the andesite pebbles contained by the conglomerates found at the base of the Buffel Formation. Fauna: Characteristic fossils are Eurydesma hobartense (Johnston), Taemothaerus sub- quadratus (Morris), Anidanthus springsurensis (Booker), Terrakea pollex Hill, Strophalosia preovalis Maxwell, Ingelarella denmeadi Camp- bell, Platyschisma rotundatum (Morris) and Keeneia ocula (Sowerby). Age: Lower Permian. This is discussed in the section on palaeontology. Oxtrack Formation The Oxtrack Formation is here restricted to the upper lithological and palaeontological unit in the Oxtrack Formation of Derrington e al. for which the type locality was Oxtrack Creek, between Cracow and Theodore. Just north of Oxtrack Creek the Buffel Formation is found, but in the creek section itself, only the Oxtrack Formation (in the restricted sense) is to be seen. Synonymy : This is the same as for the Buffel Formation. Distribution: The Formation outcrops as a discontinuous northerly trending belt through- out the Cracow-Theodore district. South from the type section the unit can be traced along the western slopes of the small, un- dulating hills towards the Theodore Road, west of Cracow. From north of Rose’s Pride Mine, southwards (to 31848573) the Buffel and Oxtrack Formations outcrop as parallel, adjacent belts, but beyond that point and as far as 1-8 miles south-east of the Orange Creek road crossing (32078526) the Oxtrack Formation directly overlies the Camboon Andesite. South of Back Creek 162 the Buffel Formation reappears between the Oxtrack Formation and the Camboon Ande- site, and the strike swings to east of north. At all localities where the Oxtrack and Buffel Formations are in close proximity, the contact is obscured by soil cover and there- fore their angular relationship is not accur- ately known. Lithology: The dominant rock types are cal- careous siltstones and limestones, both being fossiliferous. The calcareous siltstones occur to the south-west of Cracow and become more calcareous to the north, grading into limestones. The rocks contain a large per- centage of organic fragments, mainly polyzoan and crinoidal. This percentage may be as high as 80%, but in the main it varies between 35% and 45%. The calcareous siltstones of the Oxtrack Formation are more compact than those of the Buffel Formation and the limestones of the Oxtrack Formation are more impure than those of the Buffel Formation. Thickness: Accurate thicknesses are difficult to obtain because of the soil cover. From Mt. Ox, north of Oxtrack Creek to south of the Theodore Road, the thickness is of the order of 75 to 100 feet. South-west of Cracow Homestead, the thickness is of the order of 300 feet. Structures: The dip of the Formation varies from 18 to 40 degrees to the west, and the strike varies from 20 degrees west of north to 10 degrees east of north. South-west of Cracow Homestead, the Formation is folded into two asymmetrical anticlines. Sedimentary structures include orientation of the polyzoan fragments and spines along planes which may be bedding planes. At one locality, 1-3 miles north-west of Cracow Homestead (32018456) there is a grading of both inorganic grains and organic fragments in the siltstone. Stratigraphic Relationships : The Oxtrack Formation is considered by the writer to disconformably overlie the Buffel Formation and the Camboon Andesite. No evidence has been found for an angular discordance between the Buffel Formation and _ the Oxtrack Formation. In all places where the two Formations have been observed in close proximity they can be readily distinguished by the faunal assemblages and by the lithological differences, which, although small, are sufficient for discrimina- tion. ROBIN WASS Fauna: Characteristic fossils are Ingelarella mantuanensis Campbell, Strophalosia clarket Etheridge, Snr., Strophalosia clarket var. minima Maxwell, Martinia sp., Atomodesma (Aphanaia) sp., Volsellina ? mytiliformis Etheridge. Age: Upper Permian. See section on palae- ontology. Overlying the Oxtrack Formation is approxi- mately 5,300 feet of marine Permian, most of this being fossiliferous. Further to the north in the Theodore-Banana district, Derring- ton et al. named the Barfield and Flat Top Formations in that ascending order. How- ever, because of the extensive tract of soil cover in the Theodore-Cracow district it is doubtful in the writer’s opinion whether the Barfield and Flat Top Formations can be definitely related to the sequence at Cracow without the aid of subsurface data. Therefore, the names Barfield and Flat Top are preceded by a question mark in the following text. ? Barfield Formation This Formation was proposed by Derrington et al. for a sequence of rocks conformably overlying the Oxtrack Formation at the type locality, Barfield Station, north-east of Theo- dore. There the unit comprises mudstone, siltstone and subgreywacke, with calcareous concretions. Synonymy : Lower Bowen (in part) Denmead, 1937 ; Middle Bowen (in part) Denmead, 1938; Orange Creek Formation, Acacia Formation, Passion Hill Formation, Derring- ton et al., 1959; Back Creek Formation (in part) Mack, 1963. Distribution : In the Cracow district the ? Bar- field Formation outcrops only sparsely, form- ing the black soil plain west of the Oxtrack Formation. The best outcrops were found in creeks cutting this plain such as Orange Creek, Back Creek, and Cracow Creek. Lithology : Predominantly mudstone and silt- stone, with lesser amounts of subgreywacke and tuff. Tuffs are found in the uppermost 500 feet of the sequence as are concretions up to two feet in diameter. The concretions are enclosed in a rock which varies from a subgreywacke to a mudstone. This rock often contains pyrite and glendonites. The glendonites are found with the concretions west of the Newstella yards on “ Gyranda ,”’ approximately 7-0 miles north of Cracow. MARINE PERMIAN FORMATIONS OF CRACOW DISTRICT, QUEENSLAND The concretions can also be observed in Back Creek (31668520) and where Orange Creek cuts the road from ‘‘Gyranda”’ to the Theodore Road. Thickness : Estimated thickness in the Cracow district is 3,250 feet. Structures : Sedimentary structures are absent except for glendonites and cone-in-cone lime- stone which outcrops in the black soil plain, 3-1 miles south-west of Cracow (31958505). The significance of glendonites and _ their origin has been discussed by Carey and Ahmad (1961). The dip of the Formation varies from 12 to 28 degrees to the west and the strike varies from 20 degrees west of north to 10 degrees east of north. Stratigraphic Relationships: The ? Barfield Formation in the Cracow district is considered by the writer to conformably overlie the Oxtrack Formation, and to be conformably overlain by the ? Flat Top Formation. Fauna: This is characterised by Cancrinella sp. nov., Luissochonetes brevisulcus Water- house, Glyptoleda glomerata Fletcher, Para- conularia derwentensis (Johnston). Age: Upper Permian. See section on palae- ontology. ? Flat Top Formation The Formation was proposed by Derrington et al. for a sequence of rocks conformably overlying the Barfield Formation in the Theo- dore-Banana district. The type locality was given as four miles east of Banana on the Dawson Highway to Biloela. The lithologies present were mudstones and subgreywackes, with lenses of limestone. Synonymy : Lower Bowen (in part) Denmead, 1937; Middle Bowen (in part) Denmead, 1938 ; Mt. Steel Formation (in part) Derring- ton et al. 1959; Back Creek Formation (in part), Kianga Formation (in part) Mack, 1963. Distribution : The ? Formation outcrops as a series of discontinuous ridges west of the black soil plain in which the ? Barfield Formation outcrops. Lithology : Predominantly mudstone with minor amounts of calcareous subgreywacke and tuffs showing shards. The mudstones, if light coloured, exhibit a laminated structure 163 and often show small slump structures. Fossiliferous rocks are rare in this ? Forma- tion in the Cracow district. Thickness : Estimated thickness of the ? Flat Top Formation is 1,900 feet. Structures: The dip varies from 10 to 25 degrees to the west and the strike varies from 30 degrees west of north to 15 degrees east of north. Minor slumping is evident in some outcrops. Stratigraphic Relationships: he ? Flat Top Formation is regarded as being conformably overlain by the Gyranda Formation, which contains a Glossopteris flora and is considered to be of non-marine origin. Fauna: The fauna in the Cracow district is composed of crinoid stems. A more complete list of fossils found in the Cracow-Theodore district appears in the section on _ palae- ontology. Age: Upper Permian. This is discussed in the palaeontology. Palaeontology The prolific nature of the faunas in the Cracow district in number of species and genera as well as of individuals has been known since late last century. There are three main faunal assemblages in the district and to the north around Theodore there are four, as the ? Flat Top Formation becomes more fossiliferous than it is to the south. Some of the fauna from the Buffel and the Oxtrack Formations had been collected previously by Professor Dorothy Hill and other senior staff members of the University of Queensland. The fauna in the ? Barfield Formation had possibly been found before the present work but had not been collected in detail, nor had its lateral extent been esta- blished. The importance of palaeontology in under- standing the area can be gauged if a section is taken west from Rose’s Pride Mine up through the sequence. Overlying the Camboon Andesite are outcrops of the Buffel, Oxtrack, ? Barfield and ? Flat Top Formations, all fossiliferous, consisting of calcareous clastic sediments and all separated by black soil. The fossil lists for each Formation are shown in Tables 1 and 2 with the range of each species. A number immediately after a species indicates that some comment is made on that species after the general discussion of the fauna. 164 FAUNAL DISCUSSION Buffel Formation: The Formation contains the lowest marine fauna in the Cracow district. At all localities where the horizon has been recognised it is characterised by the presence of either Eurydesma or one of the gastropods, Keeneta or Platyschisma. Cancrinella farleyensis may be easily distin- guished from species in overlying Formations by its smaller size, finer costation and poorer transverse wrinkling. Terrakea pollex is characterised by its small size and absence of umbonal thickening, distinguishing it from species in overlying Formations. Species of Spirifer, Trigonotreta and WNeo- spirifer from the Buffel Formation have coarser ribbing with a deeper sulcus and higher fold than the species in the Oxtrack Formation. Spirifer sp. B. from the ? Barfield Formation is a very alate form. The ingelarellids are charactered by plica- tions and the species of Lissochonetes is not as globose as L. brevisulcus from the ? Barfield Formation. Sr Deere tes Buffel Fm. ROBIN WASS Hill (1950), after studying the Productinae came to the conclusion that the age of the fauna was Upper Sakmarian or Lower Artinskian. Maxwell (1954), after a study of the species of Stvophalosia came to a similar conclusion. Hill (1955), on evidence gained from the previous two studies as well as from the ingelarellids, placed the age as uppermost Sakmarian. After a complete study of the fauna it is thought that the age is most conveniently placed at the Artinskian-Sak- marian boundary. In the type section the lmestone may be divided into three parts. In the lowest part the fauna comprises a_ brachiopod-molluscan assemblage, the only polyzoan present being a large ramose stenoporid. Notably absent from the basal assemblage are Amidanthus spring- surensis, Cancrinella farleyensis and Horridonia mitis. Many of the species found in the lowest part are not found in the middle part which contains Foraminifera. Euryphyllum reid is found only in this part and there is a great increase in the number of slender, ramose polyzoa. Associated with these are many Oxtrack Fm. ? Barfield, Him. |) ¢ Plat fap peu Calcitornella sp. Euryphyllum reidi Hill Anidanthus springsurensis (Booker) Cancrinella farleyensis (Etheridge and Dun) Chonetes cracowensis Etheridge Horridonia mitis Hill (1) Grantonia sp. nov. (2) Ingelarella denmeadi Campbell I. ovata Campbell I. cf. profunda Campbell (3) ? Kyrotovia sp. Lissochonetes cf. yarrolensis Maxwell Neospirifer sp. (2) Spivifer sp. A. Spiriferellina sp. Strophalosia preovalis Maxwell Stveptorhynchus sp. Taeniothaerus subquadratus (Morris) T. subquadratus var. cracowensis Hill Terrakea pollex Hill Trigonotreta cf. stokesi Koenig (2) Chaenomya sp. Deltopecten limaeformis (Morris) Eurydesma hobartense (Johnston) Myonia carinata (Morris) Keeneia sp. nov. (4) K. ocula (Sowerby) Peruvispiva sp. nov. (5) Platyschisma rotundatum (Morris) — Ptychomphalina sp. Polyzoa (6) Glossopteris sp. NOTE: (1), (2), etc., refer to notes on species in text. MARINE PERMIAN FORMATIONS OF Species Buffel Fm. Ammodiscus muiticinctus Crespin and Parr Frondicularia woodwardi Howchin Rectoglandulina sevocoldensis (Crespin) Cladochonus sp. Euryphyllum sp. A. Thamnopora wilkinsoni (Etheridge) ? Cancrinella sp. Ingelavella mantuanensis Campbell Martinia sp. Strophalosia clarket Etheridge, Snr. S. clarkei var. minima Maxwell Tervakea solida (Etheridge and Dun) Atomodesma (Aphanaia) sp. (7) Streblochondria sp. Volsellina ? mytiliformis (Etheridge) Euryphyllum sp. B. Thamnopora cf. immensa Hill Cancrinella sp. nov. (8) Cletothyridina sp. Ingelarella sp. A. Lissochonetes brevisulcus Waterhouse Spirifer sp. B. Strophalosia cf. ovalis Maxwell Tervakea sp. A. Glyptoleda glomevata Fletcher Platyteichum sp. Strotostoma sp. Warthia sp. Paraconularia derwentensis (Johnston) Conularia cf. laevigata Morris Lissochonetes sp. (9) Aviculopecten sp. Note: (1); (2), specimens of Horridomia mitis together with Streptorhynchus sp. In the upper part the rock is decalcified and it is here that Anzdanthus springsurensis, Cancrinella farleyensis, Strophal- osia preovalis and Terrakea pollex become prominent. North of the Theodore Road, the Buffel Formation contains fewer specimens, and in particular Polyzoa, Ingelarella, Cancrinella and Euryphyllum are fewer. At Rose’s Pride Mine the Formation outcrops as_ two_ horizons separated by soil cover ; in similar lithologies, both contain the same fauna but not necessarily in the same proportions. Oxtrack Formation: The fauna of this Formation is characterised at practically all localities by Ingelarella mantuanensis, V olsellina ? myttliformis and large crinoid ossicles up to one inch in diameter. The species of Stvophalosia are not as concavo-convex as the species in the overlying Formations. Jngelarella mantuanensts is a broad Oxtrack Fm. CRACOW DISTRICT, QUEENSLAND — 165 ? Barfield Fm. | ? Flat Top Fm. etc., refer to notes on species in text. form with long subparallel adminicula and species found in the overlying ? Barfield and ? Flat Top Formations are more globose with a sharper median sulcus. Maxwell (1954) correlates the fauna with the Mantuan Pvoductus Bed and regards the age as high in the Kungurian. Hill (1955) also regards the age as being high in the Kungurian. The Mantuan Productus Bed is the upper part of the Peawaddy Formation of Mollan e¢ al., 1964. In the writer’s opinion the fauna of the Oxtrack Formation enables correlation to be made with the lower part of the Peawaddy Formation and the age of the fauna is Kungurian-Kazanian. ? Barfield Formation: At all localities where the fauna of the ? Barfield Formation can be observed it is characterised by a species of Cancrinella which appears to be the same as Cancrinella cf. magniplica Campbell (1953, pl. 1, figs. 6-8). It is considered by the writer to be a new species, easily distinguishable from C. magniplica. 166 At first sight this fauna bears some resemblance to that of the Ingelara Formation at Springsure. However, the resemblance is regarded as being ecological. Most of the genera which are of use in correlation bear some similarity to those in the Oxtrack Formation and as the ? Barfield Formation overlies the Oxtrack Formation without any apparent discordance, the age of the fauna is considered to be Lower Kazanian. ? Flat Top Formation: The presence of Strophalosta cf. ovalis, Terrakea solida and Volsellina ? mytiliformis indicates that the ? Flat Top Formation is equivalent or higher than the Mantuan Pvoductus Bed. From the fauna and the stratigraphic position of the ? Formation, the age is regarded as Lower Kazanian. NOTES ON SPECIES (1) In her paper on the Productinae of the Cracow fauna, Hill (1950) erected Horridonia mitis but added that there were no specimens showing enough of the dorsal valve for its description. From the type locality and locali- ties to the north, specimens of both ventral and dorsal valves of a form similar to H. mitis have been collected and they are being examined by Dr. D. J. Gobbett of the University of Malaysia for their precise determination. If they are specimens of Horridonia mitis, a description of them will appear in another paper. (2) Brown (1953) in erecting the genus Grantonia mentioned that specimens from Mt. Britton (Homevale) showed some _ variation from the Tasmanian topotype material. Speci- mens from the Buffel Formation are conspecific with those from Mt. Britton and can be readily distinguished from the type species by their ornament. There is some difference in the internal structures of the ventral and dorsal valve. Plastotype material of the type species of the genera Neospirifer, Trigonotreta and Grant- omnia has been studied and the following con- clusions reached. (a) Neospirifer has bundles of fine ribs. There may be any number on each side of the sulcus and fold and each bundle may contain four to 10 fine ribs. The ornament may be reflected on the internal mould. If any fasciculation takes place it can be observed close to the umbo. (b) Trigonotreta has seven bundles of ribs on each side of the sulcus and fold. The ROBIN WASS ribs are coarser than in Neospirifer and only three make up each bundle. In juvenile specimens, fasciculation is found only on outer ribs, but in mature specimens, it is seen on the ribs adjacent to the sulcus. The external ornament is rarely reflected on an internal mould. (c) Gvrantonia has three or four bundles of ribs on each side of the sulcus. Fascicula- tion is found on both outer and inner ribs. The external ornament is reflected on the internal mould. The observations about Neo- spirifer and Trigonotreta are similar to those of Waterhouse (1964). (3) The specimens appear to be intermediate between Ingelarella symmetrica Campbell and I. profunda. ‘ (4) Keeneta sp. nov. shows some resemblance to K. minor (Fletcher) which has a more flattened whorl profile together with more whorls. All other Australian species of Keeneza are much larger and have a greater or lesser pleural angle with a different number of whorls. (5) Peruvispira sp. nov. differs from other species in the pleural angle, length/width ratio, number of whorls and size. (6) The Polyzoa are being studied at present by the writer at the University of Sydney as part of a Ph.D. project. (7) Previously, this species had been referred to Astartila pusilla (McCoy). Bruce Runnegar, University of Queensland, has informed me that the name used in the fossil lists is more correct. (8) This species is easily distinguished from Cancrinella magniplica by the greater convexity of the ventral valve, the much larger size of the visceral cavity, the coarser costations and by the stronger transverse wrinkling on the anterior portion of the ventral valve. (9) Lissochonetes sp. bears some resemblance to L. brevisulcus, but preservation is too poor to enable a precise determination to be made. Acknowledgements The writer is indebted to Professor Dorothy Hill, F.R.S., of the Department of Geology, University of Queensland, who suggested the project and supervised the work since its inception. He wishes to thank Dr. T. B. H. Jenkins, Department of Geology and Geophysics, University of Sydney, for his critical reading of the manuscript and the University of Queens- land for the award of a Teaching Fellowship during the years 1961-1962. MARINE PERMIAN FORMATIONS OF CRACOW DISTRICT, QUEENSLAND References Brown, I. A., 1953. Permian Spirifers from Tasmania. J. Proc. Roy. Soc. N.S.W., 86 (2), 55-63. CAMPBELL, K. S. W., 1953. The Fauna of the Permo- Carboniferous Ingelara Beds of Queensland. Pap. Dep. Geol. Univ. Qd., 4 (3), 1-30. CAMPBELL, K. S. W., 1959. The Martiniopsis-like Spiriferids of the Queensland Permian. Palae- ontology, 1 (4), 330-350. CaREY, S. W., and AuMmaD, N., 1961. Glacial Marine Sedimentation, their Environment and Nomen- clature. Proc. Ist. Int. Symp. on Arctic Geology, 2, 865-894. DENMEAD, A. K., 1937. Cracow Ore Reserves. Qd. Govt. Min. J., 38, 121-125, 156-159, 191-194. DENMEAD, A. K., 1938. The Cracow Goldfield. Qd. Govt. Min. J., 39, 335-340, 368-375, 406-412. DERRINGTON, S. S., GLOVER, J. J. E., and Moracan, K. H., 1959. New Names in Queensland Strati- graphy. Permian of the South-Eastern Part of the Bowen Syncline. Aust. Oil Gas J., 5 (8), 27-33. Dicxins, J. M., 1961. Permian Pelecypods newly recorded from Eastern Australia. Palaeontology, 4 (1), 119-130. Hiii, D., 1950. The Productinae of the Artinskian Cracow fauna of Queensland. Pap. Dep. Geol. Univ. Qd., 3 (2), 1-36. Hii, D., 1955. Contributions to the correlation and fauna of the Permian in Australia. J. Geol. Soc. Aust., 2, 83-107. 167 JENSEN, H. I., 1926. Geological Reconnaissance between Roma, Springsure, Tambo and Taroom. Publ. Geol. Surv. Qd., 277, 1-215. Mack, J. E., Jnr., 1963. Reconnaissance Geology of the Surat Basin, Queensland and New South Wales. Bur. Min. Res. Petrol. Search. Publ., 40, 1-35. Matong, E. J., 1964. Depositional Evolution of the Bowen Basin. J. Geol. Soe. Aust., 11 (2), 263-282. MAXWELL, W. G. H., 1954. Stvophalosia in the Permian of Queensland. J. Palaeont., 28 (5), 533-599. MoLLaN, R. G., KIRKEGAARD, A. G., Exon, N. F., and Dicxkins, J. M., 1964. Note on the Permian Rocks of the Springsure Area and proposal of a new name, Peawaddy Formation. Qd. Govt. Min. J., 65, 577-581. WATERHOUSE, J. B., 1964. New Zealand. 35, 1-212. Permian Brachiopods of N.Z. Geol. Surv. Pal. Buil., Note Added in Proof Since this paper has gone to press, a specimen of a terebratuloid sent by the writer to Dr. K. S. W. Campbell has been identified and described by him as Maorielasma callosum sp. nov. The specimen comes from the Barfield Formation.—B.M.R. Bull. 68. Journal and Proceedings, Royal Society of New South Wales, Vol. 98, pp. 169-179, 1965 The Geology of the Canowindra East Area, N.S.W. W. R. RYALL ABSTRACT—An investigation of the geology of an area to the east of Canowindra, N.S.W. (Stevens, 1951, 1954), has shown that nine formations can be mapped within the area and that they extend in time from Middle Ordovician to Upper Silurian. New palaeontological finds have enabled the age of the Canomodine Limestone to be defined as Upper Ordovician and that of all but the uppermost part of the Millambri Formation as pre-Silurian. The Silurian sediments occur- ring in the area have been placed in four new formations which make up the Cudal Group. A new interpretation has been placed on the Canowindra Porphyry, it now being considered a flow rather than a sill. flanked by anticlines. The structure of the area has been clarified and is shown to be essentially a syncline Two north-south trending thrust-faults, each indicating considerable vertical movement, are prominent features of the area. Introduction The area discussed in this paper is about 60 Square miles in area and is located astride the Belubula River some five miles east of Canowindra which is itself about 200 miles by road west of Sydney (Fig. 1). The area has received geological attention since 1919 when Carne and Jones reported on the limestone deposits on Canomodine station. The area has been examined by N.S.W. Geological Survey who were investi- gating likely dam sites on the Belubula River (Harper, 1931; Kenny, 1941; Mulholland, 1946). The first detailed work in the area was undertaken by N. C. Stevens (1950; 1951; 1952 ; 1954) who mapped the area at the scale of one inch to a mile as part of a much larger regional study embracing the area from Orange to Cowra. Stevens (1954) described and named several of the formations discussed in this paper and wherever possible these names have been retained. More detailed work has, however, required that some of Stevens’ formations be changed. Stevens did not sub- divide the Silurian sediments in the area, he called them the Cudal Shale—this term has been given group status and four new forma- tions have been placed in it. New palaeontological finds have enabled the ages of the Canomodine Limestone and the Millambri Formation to be more closely defined. Because of the relatively few graptolites found within the Silurian formations the ages suggested in this paper may need to be modified slightly as new finds are made. This paper forms part of a thesis presented at the University of Sydney in 1963, as partial requirement for the degree of Bachelor of Science with honours. Detailed petrographic and palaeontological descriptions together with X-ray powder studies of the garnets can be found in the thesis which is housed in the library of the Department of Geology and Geophysics. Stratigraphy The area to the east of Canowindra consists of volcanic and sedimentary rocks which were deposited in the Tasman Geosyncline from Lower or Middle Ordovician times to Upper Silurian times. The rocks of the area have been placed in nine formations which are summarized in Table I. The Cargo Andesite The Cargo Andesite comprises a number of intermediate to basic volcanic flows which, with interbedded shale and limestone horizons, outcrops near the village of Cargo. The formation was named and described by Stevens (1948, 1950 and 1954). In the Canowindra— Cargo area the rocks of this formation form the oldest units exposed. In the area examined only the uppermost part of the formation is present and _ this outcrops as a wedge-shaped exposure over about four square miles. The stratigraphic position of it cannot be determined since both east and west limits are faulted for their entire length of outcrop. However, north-east of the area, where the formation outcrops again, bedded Canomodine Limestone dips off massive andesite clearly showing that it underlies the Limestone. The junction of the two units is not exposed so that it cannot be said if they are conformable. 170 CARGO W. R. RYALL S, \ MILTHORPE® Se OS, 1G. 1—Locality Map Near the southern limit of outcrop occurs a large mass of limestone, underlain by about 300 feet of well bedded red, green and brown Shales, which was thought by previous workers (Stevens, 1954 ; Adamson and Trueman, 1962) to be part of a Silurian formation (possibly the Wallace Shale of Stevens, 1954) which had been isolated by the complex Columbine Mountain Thrust. It now seems certain that this limestone-shale unit is part of a large lens within the Cargo Andesite since andesitic lavas lie directly over the limestone resulting in its being coarsely recrystallized at the top. Augite andesites are by far the most common rocks in the formation and predominate over hornblende andesites and _ basalts. Augite andesites are generally coloured blue in hand- Specimen and in thin-section are seen to be composed of phenocrysts of euhedral pyroxene crystals and plagioclase laths set in a fine grained pilotaxitic-subtrachytic groundmass which is composed of plagioclase microlites with interstitial pyroxene, quartz, chlorite, carbonate and potash feldspar. Magnetite granules are irregularly scattered throughout the groundmass. Plagioclase laths are sometimes up to 5mm in length and all are more or less completely sericitized and many are _ albitized. The pyroxene is nearly always augite and occurs as euhedral phenocrysts which are fresh in places but are often partially or wholly replaced by either carbonate or chlorite. Hypersthene occurs rarely as phenocrysts. Hornblende andesites occur only near the top of the formation and are composed of THE GEOLOGY OF THE CANOWINDRA EAST AREA, N.S.W. 171 TABLE I Age Formation Thickness Tenandra Formation over 1,200 feet C Upper U Belubula Shale D 700 S A I ibs L U Ghost Hill Formation 450 R I Upper Avoca Valley Shale A Middle 1,200 N G | R | O Canowindra Porphyry U Pca. 1,000 Lower Lower Avoca Valley Shale 340 Millambri Formation 4,100 Upper O Rockdale Formation 250 R D O V I Middle Canomodine Limestone 1,200 Cc I A — ? — ? — ? — P? — P? — ? — N Cargo Andesite over 1,500 Lower large platy phenocrysts of green hornblende with large tabular phenocrysts of plagioclase (near Abs, though much is albitized) and smaller augite phenocrysts set in a felted or granular groundmass consisting of plagioclase microlites with interstitial potash feldspar, hornblende and quartz. The andesites contain few amygdules which are infilled with chlorite, calcite or quartz. All the andesites examined in thin-section show some degree of alteration. Such alteration occurs over the entire area of outcrop, so that it seems unlikely it all can be attributed to deuteric phenomena (Wilshire, 1959). It may well be that some of the alteration effects are due to deuteric action but these cannot be separated from alteration produced by deep- seated diagenesis. Such alteration includes albitization and sericitization of the plagioclase and replacement of pyroxene, amphibole or the groundmass by carbonate or chlorite. The andesites contain many xenoliths which are sedimentary fragments and _ andesitic inclusions. The latter are always rounded and have a similar mineralogical composition as the host, though they are invariably of coarser erainsize. No fauna has been found in any unit of this formation making accurate age-dating impossible. From information obtained from overlying formations, however, it seems that the upper limit of the formation may be about upper Middle Ordovician. The Canomodine Limestone The Canomodine Limestone outcrops as a belt one to two miles wide which extends from Canomodine station on the Belubula River, 172 north about six miles towards the village of Barragan. It forms one of the largest lime- stone outcrops in New South Wales and about one half of this formation as defined by Stevens (1954) outcrops within the area examined. Within this area the Canomodine Limestone forms the core of the Cranky Rock Anticline and around it the younger formations are folded. The formation consists entirely of about 1200 feet of light grey, massive, poorly-bedded limestone. Bedding characteristics are obscured by the strongly developed regional cleavage but in places it is defined by rows of siliceons nodules. Rather marked recrystallization has occurred within the limestone and accounts for the poor preservation of the fauna found within it. Outcropping in the north east of the area is the Cargo Creek Limestone (Stevens, 1954). This mass occurs at a similar stratigraphic horizon as the Canomodine Limestone and appears to be separated from it by fairly simple folding, so that the two masses should properly be regarded as being the one unit. The Canomodine Limestone is poor in faunal content compared with other limestone masses of similar age which outcrop in the Cudal- Canowindra-Walli area (Stevens, 1954). Professor Hill has identified from Stevens’ collection (Hill, 1957): ? Plasmopora ? cargo- ensis sp. nov., ? Plasmoporella ? inflata sp. nov., Propora sp., Streptelasma sp., ? Lichenania sp. and Stromatoporidae. From this fauna she suggested that the age of the Canomodine Limestone may be either Upper Ordovician or Lower Silurian. Further collection has yielded further fauna : Plasmoporella inflata, Calapoecia aff. canadensis, Favistella inflata, Favosites sp., Streptelasma sp., Lvyplasma sp. and Stromatoporidae. This fauna suggests the formation may be _ pre- Silurian. Evidence obtained from graptolites occurring in the overlying formation indicates that the Canomodine Limestone may be lower Upper Ordovician or even earlier. Rockdale Formation The Rockdale Formation is a new formation which has been erected to take the place of the Lower Millambri Formation of Stevens (1950, 1954). Full formation status is warranted since the lithology represented by it differs markedly from that of the Millambri Formation (as now defined). The formation is so named We RERYALL because its maximum outcrop occurs on the “ Rockdale ”’ property. The Formation consists of about 250 feet of soft, finely interbanded dark and light silt- stones. Throughout all its outcrop no detritus coarser than siltstone grainsize is present. The silts are composed of angular grains of quartz and feldspar which, in grain-size, grade into a fine grained silty matrix which is often carbonaceous. The formation contains graptolites but most are poorly preserved. The most diverse fauna occurs at “ The Glen ’’ where have been found : Climacograptus bicornis, Dicellograptus — sp., Climacograptus sp. and Glyptograptus sp. The identification of Climacograptus bicornis and Dicellograptus sp. is unquestionable and indicates an upper Ordovician age for the forma- tion. This age conflicts with that assigned by Sherrard (1962) who records the following fauna iOUleee Uitee Glenuer Monograptus gregarvus (common), M. atavus, M. cf. tnangulatus triangulatus, Glyptograptus tamariscus, Climaco- graptus innotatus and ? Dimorphograptus erectus. From this assemblage she states (pp. 174-175) : “This assemblage from The Glen . . . proves definitely the Silurian age of the Millambri Formation at that locality ”’. At The Glen I have not been able to find any Monograptids. The Diplograptids and Leptograptids are unquestionable and require the formation to be assigned to the Upper Ordovician. Millambri Formation The Millambri Formation is composed of arenites (in the sense of Pettijohn, 1957) and siltstones which conformably overlie the Rock- dale Formation around the Cranky Rock Anticline and unconformably overlie the Cargo | Creek Limestone at the north eastern corner of the area examined. The type section is located at the Belubula River between Millambri and Cranky Rock homesteads where the formation is 4,100 feet thick and is readily divisible into two members : (1) a Lower Member which consists of 1,200 feet of massive, poorly bedded arenites which generally contain only a few thin siltstone beds, (ii) an upper Member which is 2,900 feet thick and consists mostly of banded siltstones which predominate over beds of arenite. The arenites of this member are similar in all respects to those of the Lower Member. Near the top of the formation occur conglo- merate lenses which vary markedly in size. The two largest, one mile south of Mount THE GEOLOGY OF THE ¢ of niv\v Ww MUS ON Sta a Se \ Nv v We: Woes S s Y %) X Lilt le LiL ) Mo LQ Bis, y 32) Vaav LSVa VaaNIMoNVvo Prove AHL 40 dVW 1WV9IDO10489 zx K ERS 3 : vs as SON FS \\ ef sey 9 war PSH’ AN . Yi, 4 ~ ‘ e GAN Se SA iN r DWAIN Ae ASN Ont VN ? ule roca} / | <~ ° 1 Scale in miles a SEGENO [SY] Recent alluvium Tenandra Formation ESQ) Belubula Shale Ghost Hill Formation (MM Upper Avoca Valley Shale [723] Canowindra Porphyry [Lower Avoca Valley Shale BSS Millambri Formation Rockdale Formation Canomodine Limestone Cargo Andesite — Position accurate ==> w approximate inferred Bedding Attitude £35 \nclined Anticlines “AL Position accurate ™~ ” Synclines SR. Position accurate a! opproximate G-Groptolite localities L-Limestone mi GEOLOGICAL MAP OF THE CANOWINDRA EAST AREA Cudal Group Geological Boundaries + Vertical X45 Overturned + Horizontal Faults IN Position accurate ~—S " approximate Das " inferred Folds ~ approximate “WSN ‘VaNV ISVA VACNIMONVO AHL JO ADNOTOAD AHL ELT 174 View homestead and one mile north of Liscombe Pools homestead, are about a mile long. Smaller lenses occur at the same horizon around the Cranky Rock Anticline where they range from 20 to 50 yards long. The conglomerate is composed of well rounded pebbles and cobbles of intermediate volcanic rocks (mostly andesites) set in a matrix of arenite which is the same as that occurring elsewhere in the formation. At a stratigraphic horizon similar to that of the conglomerate bodies, at several localities, occur limestone lenses which contain Favosites sp., Heliolites sp., Halysites sp., Zaphrentis sp., and Stromatoporidae. The siltstones and arenites of this formation are composed of the same minerals, though proportions differ. The silts always contain more carbonaceous matter than the arenites. In hand specimen the arenites are blue-grey in colour, massive, hard and show an even texture. They frequently contain fragments of siltstone. In thin-section they are seen to have a fairly simple and constant mineralogy con- sisting of plagioclase and pyroxene grains set in a fine silty or clayey matrix together with numerous intermediate volcanic rock fragments. Hornblende grains are often present, biotite is less so and detrital quartz is notably lacking. The plagioclase and pyroxene grains occur, in most cases, as either euhedral grains or angular fragments which show some crystal outline. The plagioclase is nearly always albite and the pyroxene is augite. The arenites are not wholly made up of detrital minerals. Diagenetic prehnite and carbonate occur replacing both grains and matrix. These minerals are accompanied by small amounts of epidote and a few narrow and sinuous quartz veins. No pumpellyite has been found in the greywackes of the Millambri Formation. Sedimentary structures are very common in this formation, the most widely developed being graded bedding, a feature which is seen in all but the uppermost part of the formation. Small scale slump structures and unidirec- tional current bedding are common and occur associated with load casts, small scale normal faults and clastic dykes. The sedimentary structures, taken with the poorness of sorting and the nature of the matrix of the arenites, suggest that deposition occurred from turbidity currents in a deepwater environ- ment (Kuenen and Carozzi, 1953). These observations apply to all but the uppermost part of the formation (above the conglomerate- limestone horizon), where no graded bedding has We Ken Y AE been observed. This suggests the uppermost part may have been deposited in a shallow water environment. The sediments of the lower part of the formation are greywackes in the sense of Packham (1954). The mineralogy of the Millambri Formation points to its being derived from a terrain consisting essentially of andesitic rocks. The current bedding and current ripple marks indicate that this terrain lay to the north-east of the area examined. The Millambri Formation is characterized by a lack of shelly fauna except near the very top where Linguella sp. are common. Graptolites have been found near the top of the formation at three localities near Liscombe Pools Creek. To the north of Liscombe Pools homestead Glyptograptus tamariscus occurs whilst near the very top of the formation occur fragments of Climacograptus hughesi and Monograptus sp. (identifications by Dr. G. H. Packham). This latter occurrence defines the top of the formation to lie in the lower Llandovery (lower Keilorian of Thomas, 1960). The Cudal Group The Cudal Group is a new name which has been erected to take the place of the ‘“ Cudal Shale” of Stevens (1951, 1954). The Group contains four formations and represents sedi- mentation from lowermost Silurian to upper- most Silurian or perhaps even Lower Devonian. Avoca Valley Shale The Avoca Valley Shale overlies the Millambri Formation and as such occurs as two distinct outcrops within the area examined—as a thin crescent around the Cranky Rock Anticline and as an elongate north-south trending strip to the east of the area in which the beds generally dip to the west at moderate to high angles. The formation has been divided for con- venience of reference into two units, the distinction being based upon stratigraphic position with respect to the Canowindra Porphyry which occurs within the formation over much of its outcrop. “Lower ” Avoca Valley Shale The type section of the lower unit is in Licking Hole Creek south of Liscombe Pools homestead where it is 340 feet thick and is composed of red, green and brown shales which contain a prominent buff siltstone bed which is graptolitic. At the type section immediately below the contact with the Porphyry in the THE GEOLOGY OF THE CANOWINDRA EAST AREA, N.S.W. red-brown shales occur numerous spherical concretions which are up to 10 inches across. Where this unit outcrops around the Cranky Rock Anticline exactly the same units are present. In thin-section all the shales of this unit are seen to contain detrital quartz, feldspar, white mica, haematite and carbonaceous material together with abundant clay. The presence of abundant detrital quartz contrasts with the formation stratigraphically below. No sedimentary structures indicating direc- tion of provenance of sediments of the lower unit have been found. It is clear, however, that the source of detritus for sediments of this unit is quite different from the source of Millambri Formation sediments. At the end of Millambri Formation time the depositional basin was relatively shallow as evidenced by the limestone lenses with their coelenterate fauna which are found at the top of the formation. Between the Millambri Formation and the “ lower”’ unit of the Avoca Valley Shale no unconformity exists, but there may be a small disconformity. This indicates there was no large scale shallowing of the basin between the time of deposition of the two units. At the west of the area in the buff siltstone band graptolites have been found. Monograpius priodon, M. aff. vomerinus, ? M. spiralis and Retiolites geinitizianus indicate an upper Lower to lower Middle Silurian age for the lower unit. “Upper” Avoca Valley Shale The upper unit of the Avoca Valley Shale occurs above the horizon of the Canowindra Porphyry and in the south of the area is present on both the eastern and western limbs of a synclinal structure. Passing northwards the western limb is terminated by the Canangle Thrust whilst the eastern lmb persists north- wards to the limit of the area examined. North of the Belubula River the base of the unit is missing, it being cut off by the Columbine Mountain Thrust whilst further to the north it is brought against the Cargo Andesite by another fault. The unit consists mainly of green shales but locally red and brown shales are _ present. Immediately overlying the Canowindra Porphyry is a quartzo-feldspathic sandstone which contains fragments of pink garnet. The sandstones are poorly bedded and are characterized by not being uniformly developed within the unit. At the type section on the 175 Avoca Valley property the upper unit is some 1,200 feet thick. The sandstone occurring in this unit is composed of grains of quartz, feldspar and biotite set in a clayey matrix which always makes up less than 20% of the rock. Most grains in the sandstone are distinctly angular and in some cases euhedral bipyramidal quartz crystals are present. Light pink garnet frag- ments occur scattered uniformly throughout the sandstones. The constancy of stratigraphic horizon of the garnet bearing sandstone taken with its wide variation in thickness over short distances and the similarity of the minerals present within it to those of the Canowindra Porphyry point to its being derived from the Porphyry. Current bedding observed in the sandstone unit indicates the depositing traction currents came from a southerly direction. This may mean the Porphyry was emergent there. The shales which make up the bulk of this unit consist predominantly of mica and chlorite-rich clay which contains numerous grains of quartz. Within the shales occur many thin bands of sandstone all of which are less than 6 inches wide. These bands are generally lenticular over short distances and frequently show current bedding and _ basal sandstone deformation. Small scale slump structures present in the sandy bands have a southerly component of movement and may indicate the sea floor had a southerly component of slope at the time of deposition of the Avoca Valley Shale. Near the top of the unit fossiliferous lime- stone lenses are common. The fauna contained within them is the same as that in the lime- stone lenses of the overlying Ghost Hill Forma- tion. The sedimentary structures and the presence of the limestone lenses indicates that this unit was deposited in a shallow water environment. The basin appears to have been shallowing since Millambri Formation time and was probably shallowest at the time of deposi- tion of the Ghost Hill Formation. Stevens (1952, 1954) reports Monograptus cf. dubius from shales within this unit. The age of this unit is difficult to ascertain, but con- sidering information gained from the overlying formations, it seems at least part of it is Wenlockian (Eildonian of Thomas, 1960). G‘ ost Hill Formation The Ghest Hill Formation, so named because it outcrops on Ghost Hill, a prominent feature on Millambri property, conformably overlies the 176 Avoca Valley Shale and as such occurs as a generally north-south trending strip within the area examined. The formation consists predominantly of tuffaceous arenite and tuffaceous arenaceous siltstone in which frequently occur lenses of limestone. To the base of the formation occurs tuffaceous shales which contain graptolites, coelenterates and shelly fossils. At the type section on the southern bank of the Belubula River the formation is 450 feet thick but away from here it thins rapidly. The formation could not be recognized in the south western part of the area. This may be due either to the very poor outcrop or to its not being developed there. The tuffs are composed of grains of quartz, plagioclase and more rarely biotite set in a silty matrix which contains numerous devitrified shards. The quartz grains are frequently embayed bipyramidal crystals. Plagioclase occurs as both angular grains and tabular crystals which are all partially kaolinized. It hes within the oligoclase composition range. Biotite, where present, is always brown and is frequently altered to chlorite. The shards are now composed of aggregates of quartz, chlorite, carbonate and zeolites. North of Ghost Hill, within this formation, occurs an intrusive acid igneous rock which is composed of phenocrysts of quartz, plagioclase and biotite set in a fine grained quartz-rich matrix. The quartz phenocrysts of this porphyry are often bipyramidal and are frequently em- bayed and this, together with other mineralogical and field evidence, suggests the tuffs occurring in this formation may be derived from similar porphyry plugs which intruded and _ broke through the sedimentary cover. The presence of numerous limestone lenses and of a shelly and coelenterate fauna suggests deposition probably occurred in a shallow water environment. The limestone lenses contain a varied fauna which consists of Favosites sp., Heliolites sp., Tryplasma_ sp., Pentamerid and _ Spiriferid brachiopods, crinoid stems and stromatoporids. Near Ghost Hill occur specimens of Monograptus dubwus which indicate a Middle-Upper Silurian age for part of the formation. Belubula Shale The Belubula Shale conformably overlies the Ghost Hill Formation and outcrops as a narrow north-south trending strip extending from the south of the area about nine miles north. It also outcrops in the south-west of the area W. R. RYALL where it is faulted against sediments of the Tenandra Formation. The formation is named after the Belubula River which passes through it. The type section is located about a quarter of a mile west of the Avoca Valley homestead where it is about 700 feet thick and is composed of brown, red and grey shales. South of the type section near the Canowindra road the formation is composed entirely of red and buff siltstones. These are made up of minute angular quartz grains set in a clayey matrix which contains abundant fine white mica. Biotite is rarely present, and when so is always detrital. The sediments of this formation give little clue as to the environment of deposition but the absence of limestone, in contrast to the formation stratigraphically below, may reflect a deepening of the basin near the end of the Ghost Hill Formation time. The lowest units in the formation contain the small brachiopod Sowerbyella. |Mono- graptus aff. bohemicus has been found to the south of the type section and suggests an Upper Silurian age for the Belubula Formation though precise dating is not possible. Tenandra Formation The Tenandra Formation, so named because it lies in the Parish of Tenandra, conformably overlies the Belubula Shale and outcrops as a north-south trending belt which extends from the south of the area north to Canomodine homestead where it is folded to be then truncated by the. Canangle’ (dihnust) ) othe Tenandra Formation is the uppermost Palaeozoic unit within the area examined and is composed of 1,200 feet of interbedded siltstones, arenites and shales. To the north of the type section in Emu Creek the upper part of the formation is missing, it having been truncated by the Canangle Thrust. The shales occurring in this formation are similar mineralogically to shales occurring in lower formations. They are composed of angular grains of quartz and feldspar (generally less than 0-02 mm across) set in a clayey matrix in which white mica flakes are always present. The arenites of this unit) are’ /genenally, resistant to weathering and show out strongly on air-photographs. They have plagioclase as the dominant component but quartz is always present. The plagioclase is oligoclase-andesine and occurs as either angular grains or as euhedral laths. Quartz occurs as angular grains or as embayed bipyramidal crystals. | Hornblende THE GEOLOGY OF THE CANOWINDRA EAST AREA, N.S.W. and biotite are common minor detrital minerals. The matrix of these rocks is silty and always contains abundant fine quartz and plagioclase grains. Epidote is a frequent constituent of the matrix and often rims grains but never appears to replace them. The epidote is inter- preted as being detrital. In some arenites the matrix is composed almost entirely of green chlorite. Minor slump structures and basal sandstone deformation occur at several localities within the formation. Their attitude indicates the sea floor probably sloped north-south at the time of slumping. Current beddmg observed indicates that transporting currents came from a southerly direction. No fauna whatever has been found in this formation and this makes it impossible to assign an accurate age for it. It does seem possible, however, that the Tenandra Formation may range from high in the Silurian into the Lower Devonian. Post Tenandra Formation Deposits No upper Devonian sediments occur on the area examined but they are present adjacent to the eastern boundary, to the east of the Columbine Mountain Thrust. No Tertiary lavas occur in the area. The deposits of river gravel and_ other alluvium occurring within the area are probably of Quaternary age. The principal deposits of gravel, sand and silt occur along the Belubula River where, especially in the west of the area, wide river flats occur. Tracts of alluvium also occur in some of the larger tributary creeks, notably Canomodine Creek, Liscombe Pools Creek and Licking Hole Creek. Canowindra Porphyry The Canowindra Porphyry is the name given to the quartz-feldspar-biotite porphyry, characterized by the presence of sparsely distributed pink garnets, which outcrops extensively in the Canowindra area. It was named and defined by Stevens (1950, 1954) who interpreted it as being intrusive into unconsolidated sediments, but more detailed work has shown that such an interpretation leaves important considerations unanswered in the area examined. Within this area the porphyry occurs as four distinct masses all of which have their lower contact at the same stratigraphic horizon. The upper contact, because of poor outcrop, is more difficult to deal with, but it appears to be conformable. 3G Lying directly on the porphyry within the Avoca Valley Shale occurs a garnet bearing sandstone which varies widely in thickness over short distances along strike and contains only the minerals found in the porphyry. Moreover, these minerals show exactly the same minor features as corresponding minerals in_ the porphyry—they are similar in size, habit, alteration and composition. The garnet in the sandstone is identical with that found in the porphyry. (Refractive Index 1-800--0-002, cell edge 11-540A-+0-005A). If these sand- stones are derived from the porphyry, and considering the constant horizon of the base of the porphyry, then it seems that the porphyry is better regarded as extrusive rather than intrusive. Columnar jointing is common near the base of the porphyry but no flow banding has been observed in the area examined. Flow banding is not prominent in thin-section. The porphyry is a holocrystaline porphyritic rock which consists of euhedral quartz, plagio- clase and biotite phenocrysts set in a fine grained chloritized groundmass. Almandine garnet is a constant accessory mineral which may or may not be associated with any of the numerous xenoliths present. Quartz phenocrysts are frequently euhedral but most are resorbed and many are deeply embayed. Plagioclase phenocrysts are always more or less altered but fresh phenocrysts have a composi- tion near Angy. Biotite phenocrysts are never fresh, they being replaced by chlorite which is often accompanied by epidote and sphene. The groundmass is composed of aggregates of fine anhedral interlocking quartz—feldspar grains and minor biotite and chlorite. Chlorite is a constant and characteristic mineral. Garnet occurs as large anhedral crystals within the porphyry and as xenoblasts within some xenoliths contained in the Canowindra Porphyry. Xenoliths are plentiful in the porphyry and are of two main types: (i) those derived from the Silurian country rock, (ii) those not derived from rocks occurring within the area examined. Those derived from the country rock have suffered little contact metamorphism. Such xenoliths are indurated but show no significant reorganization and have undergone meta- morphic effects similar to that of the shales underlying the porphyry. It is the xenoliths which do not come from the country rocks which are most common. 178 These are all hornfelsic and show no foliation. Three types are recognised : (i) an epidote—plagioclase—biotite—quartz— (garnet) assemblage, (ii) a quartz—plagioclase—biotite garnet) assemblage, (ili) a predominantly quartz—feldspar assemblage with minor epidote and garnet. The garnet of these xenoliths is almandine and frequently contains numerous needles of silimanite, a fact which suggests they may be relics preserved in xenoliths derived from a high grade regionally metamorphosed terrain. The assemblage almandine-sillimanite would be expected from rocks of high alumina content, but as now seen they are rich in calcic minerals- epidote, calcic plagioclase and sphene. These calcic-rich minerals indicate a change in the bulk composition of the original alumina-rich xenoliths. Garnets which occur as “ phenocrysts” in the porphyry are of two types. One contains sillimanite needles and has been interpreted as being derived from the high grade xenoliths. The other has no sillimanite needles and may either be derived from xenoliths (where sillimanite-free garnets do occur) or be pyro- genetic (Edwards, 1936). A characteristic of the Canowindra Porphyry is the virtual lack of contact metamorphic effects with the sediments of the country rocks. The shales immediately underlying the porphyry are indurated and are frequently traversed by networks of thin quartz veins. Shales close to the contact are often “spotted” and in thin-section such spotting is due to aggregations of chloritic minerals. Spots such as these are well known in the lowest grades of thermal metamorphism in argillaceous sediments. From these considerations it appears certain that the Canowindra Porphyry was extruded at a fairly low temperature. The temperature, however, cannot be estimated but it appears to be con- sistent with those prevailing at the lowest grade of the albite epidote hornfels facies. Two miles south of the south-west corner of the area examined occurs the Cowra Granodiorite (Stevens, 1952). This is an elongate body of some 20 miles in exposed length which is intrusive into Palaeozoic sediments and possibly even into the Canowindra Porphyry. Several unusual features common to both the Grano- diorite and the porphyry suggest genetic ties between the two. The porphyry is characterized by the presence of numerous xenoliths, a feature which is also apparent in the Cowra Granodiorite. (epidote— W. RK. RYALL The Granodiorite also contains red garnets ; Stevens (1952) states: “.. . another notable feature of the Cowra Intrusion is the occurrence of abundant red garnets which seem to be associated with numerous xenoliths”. Two garnets from separate xenoliths in the Cowra Intrusion were found to have cell dimensions and refractive index the same as garnets from the Canowindra Porphyry. Strong evidence supporting the genetic ties is given by chemical analyses of the Grano- diorite and the porphyry (in Stevens, 1952). The analyses are strikingly similar and when this fact is considered with the similarities outlined above it must be suggested that the two rocks may be consanguineous. The xenoliths of the Cowra Granodiorite are all at a distinctly higher grade than those of the porphyry and if the two bodies were originally derived from the same magma this may mean that the porphyry was maintained at a relatively higher level and at a lower temperature than the Granodiorite. Structural Geology Within the area examined the rocks have been folded to produce a structure which is essentially a syncline flanked by anticlines. The dominant structural feature is the Cranky Rock Anticline (Stevens, 1954) which controls outcrop over about two thirds of the area. It has an axis which trends north-south and plunges to the south at about 25°. The Cranky Rock Anticline is separated, to the east, from the syncline by the Canangle Thrust, a structure which results in the western limb of the syncline being missing over much of the area examined. The syncline closes at the south of the area near the Canowindra— Walli road and again in the north near Cano- modine homestead to define an elongate basin structure which is truncated to the west by the Canangle Thrust. In the east of the area, south of the Belubula River an anticline is present but its eastern limb is truncated by the Columbine Mountain Thrust. This thrust was named by Stevens (1950, 1954) who has traced it along strike for over 20 miles. It has for much of its length brought Lower Palaeozoic rocks into contact with Upper Devonian—Lower Carboniferous sediments. The Canangle Thrust, like the Columbine Mountain Thrust, is a north-south trending feature which dips to the west at a moderately high angle. Both thrusts have a throw which may be up to 1,500 feet in places. The Canangle THE GEOLOGY OF THE CANOWINDRA EAST AREA, N.S.W. Thrust dies out rapidly to the south of the area but paucity of outcrop makes mapping unreliable here. The only unconformity recognised in the area occurs above the Canomodine Limestone. This is a gentle one and appears not to be related to any of the major orogenic cycles which affected the Tasman Geosyncline. No unconformity exists between Upper Ordo- vician and Lower Silurian sediments. The Millambri Formation represents sedimentation continuous from Upper Ordovician to Lower Silurian times. At the end of Millambri Forma- tion time there is, however, a distinct change in sedimentary provenance. This fact con- sidered with the conglomerate lenses near the top of the Millambri Formation may reflect the effects of the Benambran Orogeny in the source area. The presence of limestone lenses in or near the conglomerate horizon is inter- preted as being due to shallowing of the depositional basin. This may be due either to infilling of the basin or to uplift of the basin by tectonic forces. Although the former may be important it is the latter which seems to best account for the observed facts. This shallowing is the only result of the Benambran Orogeny observed in the area studied. As no Upper Devonian sediments occur within the area it is not possible to directly define the relationship between them and the Silurian sediments of the area. To the east of the area, however, Upper Devonian and Lower Carboniferous sediments unconformably overlie Middle and Upper Ordovician sediments. The Silurian formations in the area examined were deposited in the Cowra Trough (Packham, 1958) which Packham considers to have been folded not at the end of the Silurian Period but somewhat later in the Lower Devonian as either a late result of the Bowning Orogeny or as an early result of the Tabberabberan Orogeny. To the east of the area the Upper Devonian-— Carboniferous sediments are gently folded. Such folding is probably a result of the Kanimblan Orogeny which presumably also folded the area studied. Acknowledgements I wish to thank Professor C. E. Marshall in whose department the work was carried out. I am indebted to Drs. Vallance and Packham for their generous help whilst the study was in progress. I wish also to thank Dr. I. M. Thread- 179 gold who has been a constant inspiration and who introduced me to the X-ray techniques. My thanks are also due to Miss J. Forsyth who produced the map. The residents of the area deserve my special considerations. I am especially grateful to Mr. R. Latham and Mr. and Mrs. Ward of “Millambri”’, Mr. and Mrs. H. McLaren of “Liscombe Pools’’ and Mr. and Mrs. Brown of “Avoca Valley ” for the considerable help they afforded me. References Apvamson, C. L., and TRUEMAN, N. A., 1962. Geology of the Cranky Rock and The Needles Proposed Dam Storage Areas, Canowindra; N.S.W. Dept. of Mines, Geol. Surv. Rept. No. I. Epwarps, A. B., 1936. On the occurrence of almandine garnets in some Devonian igneous rocks of Victoria: Proc. Roy. Soc. Vic. XLIxX, Pt. 1, pp. 40-50. HarPER, L. F., 1931. Examination of suggested dam site, Belubula River: Unpublished report, N.S.W. Mines Dept. Hitt, D., 1957. Ordovician corals from New South Wales: J. Proc. Roy. Soc. N.S.W., 91, pp. 97-107. Kenny, E., 1941. Dam sites on the Belubula River near Canowindra: Unpublished report, N.S.W. Mines Dept. MULHOLLAND, C., 1946. Cranky Rock dam site, near Canowindra: Unpublished report, N.S.W. Mines Dept. PACKHAM, G. H., 1954. Sedimentary structures as an important factor in the classification of sand- stones: Amer. Jour. Sci., 252, pp. 466-476. PackHaM, G. H., 1958. Stratigraphic studies in the Older Palaeozoic rocks of the Tasman Geosyncline in central-western New South Wales: Un- published Ph.D. thesis, University of Sydney. PETTIJOHN, F. J., 1957. Sedimentary rocks: Harper, New York. SHERRARD, K., 1962. Further notes on assemblages of graptolites in New South Wales: J. Proc. Roy. Soc. N.S.W., 95, pp. 167-178. STEVENS, N. C., 1950. The geology of the Canowindra district. Part I. The stratigraphy and structure of the Cargo-Toogong district: J. Proc. Roy. Soc. N.S:W., 82, p. 50: STEVENS, N. C., 1951. The geology of the Canowindra district. Part. Er: The Canowindra—Cowra-— Woodstock area: J. Proc. Roy. Soc. N.S.W., 84, p. 46. STEVENS, N. C., 1952. The petrology of the Cowra Intrusion and associated xenoliths: Proc. Linn. Soc. N.S.W., LXXVII, pp. 132-141. STEVENS, N. C., 1954. Studies in the Palaeozoic geology of central-western N.S.W.: Unpublished Ph.D. thesis, University of Sydney. WILSHIRE, H. G., 1959. Deuteric alteration of volcanic rocks: J. Proc. Roy. Soc. N.S.W., 93, pp. 105- 120. Department of Geology and Geophysics, University of Sydney, Sydney. = ran ale HE Report of the Council for the Year Ended 31st March, 1965 Presented at the Annual and General Monthly Meeting of the Society held 7th April, 1965, in accordance with Rule X XVI. At the end of the period under review the composi- tion of the membership was 359 members, 14 associate members and 9 honorary members ; 15 new members were elected. Six members and 2 associate members resigned ; the names of 2 members and 1 associate member were removed from the list of members in accordance with Rule XVIII. It is with extreme regret that we announce the Joss by death of: Prof. Victor A. Bailey (elected 1924), Mr. John R. Bardsley (elected 1919), Mr. Frederick A. Coombs (elected 1913), Mr. Kenneth P. Forman (elected 1932), Father Anthony G. Fynn (elected 1959), Prof. Jack M. Somerville (elected 1959). Nine monthly meetings were held. The abstracts of all addresses have been printed on the notice paper. The proceedings of these will appear later in the issue of the ‘‘ Journal and Proceedings’’. The members of the Council wish to express their sincere thanks and appreciation to the nine speakers who contributed to the success of these meetings, the average attendance being 28. The Annual Social Function was held on 25th March at the Sydney University Staff Club and was attended by 34 members and guests. The Council has approved the following awards : The Clarke Medal for 1965 to Dr. M. Josephine Mackerras, M.Sc., M.B., M.C.P.A., of C.S.I.R.O., Division of Entomology, Canberra. The Society’s Medal for 1964 to Mr. F. D. McCarthy: Principal Australian Institute of Aboriginal Studies, Canberra. The James Cook Medal for 1964 to Dr. M. R. embers, DPhil. F.K.S., F.A.A.,-ot the Institute of Medical Research, Royal North Shore Hospital, St. Leonards. The Edgeworth David Medal for 1964 to Dr. Mollie E. Holman, M.Sc., Ph.D., Department of Physiology, Monash University, Victoria. The Archibald D. Olle Prize for papers published in volume 97 of the “ Journal and Proceedings ’”’ awarded jointly to Dr. J. Roberts, Bureau of Mineral Resources, Canberra, for his papers entitled ‘“‘A Lower Carboniferous Fauna from Lewinsbrook, New South Wales’’ and ‘‘ Lower Carboniferous Faunas from Wiragulla and Dungog, New South Wales ”’ ; and to Mr. J. L. Griffith, for his paper entitled ‘‘ On the Gibbs’ Phenomenon in n-Dimensional Fourier Transforms ’’. The Liversidge Research Lecture for 1964, entitled ““ Heterocyclic Chemistry and Some Biological Over- tones ’’, was delivered by Prof. Adrien Albert, Ph.D., D.Sc., F.A.A., of the Department of Medical Chemistry, The John Curtin School of Medical Research, The Australian National University, Canberra (see ‘* Journal and Proceedings ’’, vol. 98, pp. 11-22). Cc The Society has again received a gvant from the Government of New South Wales, the amount being £750. The Government’s interest in the work of the Society is much appreciated. The Society’s financial statement shows a surplus of £593 5s. 6d., due to the sale of library assets. The New England Branch of the Society met six times during the year and the proceedings of the Branch follow. | The President represented the Society at the Commemoration of the Landing of Captain Cook at Kurnell; attended the Reception to the Right Honourable Lord Bowden of Chesterfield, Minister of State for Education and Science in the British Government and, during the visit of His Royal Highness The Duke of Edinburgh, the President was a guest at a State Luncheon and attended the, First Dunrossil Lecture which His Royal Highness delivered. The President attended the Annual Meeting of the Board of Visitors of the Sydney Observatory. On 14th October, the President and the Honorary Secretary waited on His Excellency the Governor of New South Wales. We congratulate Mr. F. D. McCarthy, a former President of the Society, on his appointment as Principal of the Australian Institute of Aboriginal Studies; A/Prof. R. L. Stanton, on his award of a Royal Society Bursary and Prof. N. H. Fletcher on the award of a Nuffield Dominion Travelling Fellowship in Natural Sciences. The Society’s representatives on the Science House Management Committee were Mr. H. F. Conaghan and Dr. A. H. Low. Five parts of the “ Journal and Proceedings ’’ have been published during the year. As from Ist January, 1965, the cost of publishing the ‘‘ Journal and Proceedings ’’ rose by 10%. Council held 11 ordinary meetings and attendance was as follows: Mr. J. W. Humphries 10; Mr. C. L. Adamson 4; Mr. H. H. G. McKern 8; Mr. W. H. G. Poggendorff 6; A/Prof. W. B. Smith-White 7; Dr-A. H. Low 11; Dr. A. A. Day 9 Mr. Tia JE, Conaghan 11; Dr. Ida A. Browne 7; Dr. R. Gascoigne 4; Mr. H. G. Golding 1 (absent on leave for 8); Prof. A. Keane 6; Prot. RK. J. W. Le Fevre 23) Mr, J. Middlehurst 3 (absent on leave for 4); Mr. J. W. G. Neuhaus —8; Dr. -A. Keichel 7; Aj Proie sik: Stanton 2 (absent on leave for 5); Dr. A. Ungar 4. During the year Council held 4 Special Meetings to discuss and propose alterations to the Rules of the Society, consideration of which is _ nearing completion. Back numbers of the Society’s “‘ Journal and Pro- ceedings’’ held in the storeroom have now been cleaned, sorted and packed. Students were engaged to do this and the cost of storage expenses amounted to £169 16s. 3d. The Library—Periodicals were received by exchange from 392 societies and institutions. In addition the amount of £123 2s. 0d. was expended on the purchase of 11 periodicals. 182 Book-binding of some of the more rare sets of periodicals has been carried out by Sydney Technical College and the Society, in appreciation, is making a permanent book-binding prize each year to the value of £10 10s. Od. Among the institutions which made use of the library through the inter-library loan scheme were: N.S.W. Govt. Depts.—Dept. of Agriculture, Forestry Commission, Main Roads Dept., Mines Dept., M.W.S. and D. Board, Public Works Dept., Railway Dept., State Fisheries, Water Conservation and Irrigation Commission, Standards Association. Commonwealth Govt. Depts—Australian Atomic Energy Commission, Bureau of Mineral Resources, Commonwealth Acoustics, Commonwealth Forestry and Timber Bureau, C.S.I.R.O. Depts. :—Head Office, Melbourne; Animal Genetics, Epping; Chemical Research Laboratories, Victoria; Coal Research Section, Ryde; Food Preservation, Ryde; Fisheries and Oceanography, Cronulla; Library, Canberra ; National Standards Laboratory, Chippendale ; Textile Physics, Ryde ; Tropical Pastures, Brisbane ; Western Australia Regional Laboratories, Nedlands; Wild Life, Canberra. Universities and Colleges—Australian National Uni- versity, Monash University, Newcastle University, REPORT OF THE COUNCIL FOR THE YEAR ENDED 31st MARCH, 1965 New England University, New South Wales Uni- versity, Queensland University, School of Public Health and Tropical Medicine, Sydney University, University of Western Australia, Wollongong Uni- versity College. Companies—Wm. Arnott Ltd., Aust. Aquitane Pty. Ltd., Aust. Coal Association, Australian Gas- light Co. Ltd., Aust. Sisalkraft Co., A.E.I. Engineering Pty. Ltd., Aust. Consolidated Industries, B.H.P. Co. Ltd., British Aust. Tobacco Co., C.S.R. Co. Ltd., Electrolytic Zinc Co. Ltd., Geigy Agricultural Chemi- cals, I.C.I. Ltd., Johnson and Johnson, Lysaght Ltd., Mauri Bros. and Thompson, Union Carbide Chemical Division, W. D. and H. O. Wills Ltd. Research Institutes—Children’s Hospital, Prince of Wales Hospital, St. Vincent’s Hospital, Victorian State Laboratories, Bread Research Institute. Museums—Australian Museum. Miscellaneous—Institution of Engineers, Australia, Sydney Division ; Geological Survey of Queensland. A. H. Low, Hon. Secretary. 7th April, 1965. Abstract of Proceedings, 1964 Ist April, 1964 The ninety-seventh Annual and seven hundred and ninety-first General Monthly Meeting was held in the Hall of Science House, Gloucester Street, Sydney, at 7.45 p.m. The President, Mr. H. H. G. McKern, was in the chair. There were present 35 members and visitors. The following were elected members of the Society : Torrence Edward Kitamura; Arthur Wyngate Thurstan. ; The Annual Report of the Council and the Financial Statement were presented and adopted. The following awards of the Society were announced : The Society’s Medal for 1963: Professor R. 5. Nyholm, F.R.S. The Clarke Medal for 1964: Dr. Joyce W. Wickeny, MiB. E. The Edgeworth David Medal for 1963: Professor N. H. Fletcher. Office-bearers for 1964-65 were elected as follows: President : J. W. Humphries, B.Sc. Vice-Presidents: C. L. Adamson, B.Sc.; H. H. G. McKern, M.Sc.; W. H. G. Poggendorff, B.Sc.(Agr.) ; A/Professor W. B. Smith-White, M.A. Hon. Secretaries: A. H. Low, Ph.D., M.Sc. ; Alan AY Day; B.Sc., Ph.D. Hon. Treasurer: H. F. Conaghan, M.Sc. Members of Council: Ida A. Browne, D.Sc. ; R. M. Gascoigne, Ph.D. ; H. G. Golding, M.Sc. ; ape Wo wee Pevre, Disc:;, PKS. F-A-A.; AL Keane) Ph. D:.;> J. Middlehurst, M:Sc.; J. W. G. Neuhaus, A.S.T.C.; A. Reichel, Ph.D., Wesco ks. Stanton, Ph.D. ;-A..Ung, Dring. Messrs. Horley and Horley were re-elected Auditors to the Society for 1964-65. The retiring President, Mr. H. H. G. McKern, delivered his Presidential Address entitled “‘ Volatile Oils and Plant Taxonomy ’’. At the conclusion of the address the retiring President welcomed Mr. J. W. Humphries to the Presidential Chair. 6th May, 1964 The seven hundred and ninety-second General Monthly Meeting was held in the Hall of Science House, Gloucester Street, Sydney, at 7.45 p.m. The President, Mr. J. W. Humphries, was in the chair. There were present 24 members and visitors. The following were elected members of the Society : Edgar David Bradley, Colin Frank Bruce and Barrie Stirling Stevenson. The following papers were read by title only: “The Eclogite-bearing Basic Igneous Pipe at Ruby Hill near Bingara, New South Wales’’, by J. F. Lovering; ‘‘On Traces of Native Iron at Port Macquarie, New South Wales’’, by F. M. Quodling ; ‘“Lower Cretaceous Sporomorphs from the Northern Part of the Coonamble Basin, N.S.W.’’, by J. Rade. An address entitled ‘‘ The International Quiet Sun Years ’’ was delivered by Dr. R. G. Giovanelli, F.A.A., of the Division of Physics, National Standards Laboratory, Sydney. 3rd June, 1964 The seven hundred and _ ninety-third General Monthly Meeting was held in the Hall of Science House, Gloucester Street, Sydney, at 7.45 p.m. The President, Mr. J. W. Humphries, was in the chair. There were present 46 members and visitors. The following were elected members of the Society : Charles Dixon Cox and Graeme Maxwell Philip. The following papers were read by title only : ‘“ Lower Carboniferous Faunas from Wiragulla and Dungog, New South Wales’’, by John Roberts ; ‘James Dwight Dana in New South Wales, 1839- 1840’, by Ann Mozley; ‘‘ Minor Planets observed at Sydney Observatory during 1963’’, by W. H. Robertson ; ‘“‘ Occultations observed at Sydney Ob- servatory during 1962-63’’, by K. P. Sims. An address entitled ‘‘ Searching for Meteorites and Australites ’’ was delivered by Mr. R. O. Chalmers, Curator of Minerals, The Australian Museum, Sydney. Ist July, 1964 The seven hundred and _ ninety-fourth General Monthly Meeting was held in the Hall of Science House, Gloucester Street, Sydney, at 7.45 p.m. The President, Mr. J. W. Humphries, was in the chair. There were present 20 members and visitors. The following were elected members of the Society : Noel Charles William Beadle ; Raymond Albert Binns. An address entitled “‘ The Australian High Temper- ture Gas-Cooled Reactor Feasibility Study’’ was delivered by Mr. W. H. Roberts, Deputy Director, Australian Atomic Energy Commission, Research Establishment, Lucas Heights. 5th August, 1964 The seven hundred and ninety-fifth General Monthly Meeting was held in the Hall of Science House, Gloucester Street, Sydney, at 7.45 p.m. A/Professor W. B. Smith-White, Vice-President, was in the chair. There were present 35 members and visitors. The following was elected a member of the Society : Thomas Denis Rice. An address entitled ‘‘ The Philosophy of Science and the Philosophy im Science’’ was delivered by Dr. R. M. Gascoigne, of the School of Philosophy, the University of New South Wales. 184 2nd September, 1964 The seven hundred and _ ninety-sixth General Monthly Meeting was held in the Hall of Science House, Gloucester Street, Sydney, at 7.45 p.m. The President, Mr. J. W. Humphries, was in the chair. There were present 20 members and visitors. Warren Manser was elected a member of the Society. An address entitled ‘‘ Fossil Magnetism’’ was delivered by Dr. Alan A. Day, of the Department of Geology and Geophysics, the University of Sydney. 7th October, 1964 The seven hundred and ninety-seventh General Monthly Meeting was held in the Hall of Science House, Gloucester Street, Sydney, at 7.45 p.m. The President, Mr. J. W. Humphries, was in the chair. There were present 26 members and visitors. The following were elected members of the Society : Robert Kerril Booth, John Albert McGlynn and John Alan Belmore Scott. An address entitled ‘‘ Viruses and Antibodies ’”’ was delivered by Professor S. Fazekas de St. Groth, F.A.A., of the Department of Microbiology, The John Curtin School of Medical Research, The Australian National University. ABSTRACT OF PROCEEDINGS, 1964 4th November, 1964 The Monthly Meeting was held in the Hall of Science House, Gloucester Street, Sydney, at 7.45 p.m. The President, Mr. J. W. Humphries, was in the chair. There were present 16 members and visitors. An address entitled “‘ The Importance of Tetra- pyrrolic Pigments in Biological Systems’”’ was delivered by Dr. P. S. Clezy, of the School of Chemistry, The University of New South Wales. 2nd December, 1964 The seven hundred and ninety-ninth General Monthly Meeting was held in the Hall of Science House, Gloucester Street, Sydney, at 7.45 p.m. The President, Mr. J. W. Humphries, was in the chair. There were present 25 members and visitors. Erich Vincent Lassak was elected a member of the Society. The following papers were read by title only: “The Mesozoic Age of the Garrawilla Lavas in the Coonabarabran-Gunnedah District’’, by J. A. Dul- hunty ; “‘ 4 Note on the Stratigraphy of the Devonian Garra Beds of-N.s.W.”’, by Dy Strusz? An address entitled ‘‘ The Physics of Ice’’ was delivered by Prof. N. H. Fletcher, of the Department of Physics, University of New England. seven hundred and ninety-eighth General ~ Members of the Society, April, 1965 A list of members of the Society up to Ist April, 1964, is included in Volume 97. During the year ended 3lst March, 1965, the following were elected to membership of the Society : BEADLE, Noel Charles William, D.Sc., Professor of Botany, University of New England, Armidale. Binns, Raymond Albert, B.Sc.(Syd.), Ph.D.(Cantab.), Geology Department, University of New England, Armidale. Bootu, Robert Kerril, B.Sc., Dip.Ed.(Syd.), Science Teacher, 46 Jellicoe Street, Hurstville. ISRADLEY, Edgar David, M.B., B.S.(Syd.), D.O., Ophthalmologist, 107 Faulkner Street, Armidale. Bruce, Colin Frank, D.Sc., Physicist, 17 Redan Street, Mosman. Cox, Charles Dixon, B.Sc., 51 Darley Street, Forest- ville. Lassak, Erich Vincent, B.Sc.(Hons.), A.S.T.C., Research Chemist, 167 Berowra Waters Road, Berowra. ManseER, Warren, B.Sc.(Syd.), L. A. Cotton School of Geology, University of New England, Armidale. McGitynn, John Albert, B.Sc.(Hons.), Analyst, Department of Mines, Sydney. Financial The Honorary Treasurer’s Report The Society this year has recorded a surplus of £593 6s: 5d. Income for the year included £626 12s. 7d., from the sale of library assets so that actually the Society operated on a deficit of £33 7s. ld., for the twelve months. The items contributing chiefly to this deficit were cleaning and storage. Cleaning costs have risen 50% to £151 5s. 0d. owing to additional cleaning and polishing of tiles in the Society’s rooms. An amount of £169 16s. 3d. was outlayed on the cleaning of the storeroom and the cleaning and packaging of the back numbers of the “‘ Journal and Proceedings ’’. This outlay was essential for the preservation of the back numbers which represent a significant asset. With the exception of the installation of some wooden shelving some ten years ago, this is the first major expense on the storeroom since the Society has occupied the present quarters. On the credit side a saving of £91 3s. 2d., as against last year has been effected on general printing. This is due to the purchase of a duplicating machine on which Council and Monthly Meeting notices, library selling lists, etc., are reproduced. The machine cost £91 13s. Od., and has paid for itself in five months. A Finance Committee was instituted by the Council of the Society in late 1963. The purpose of this Committee is to advise Council on all matters relating to finance and expenditure. The Committee consists of the President, the Hon. Secretaries, the Hon. Treasurer and certain members appointed by the PuHILttp, Graeme Maxwell, M.Sc.(Melb.), (Cantab.), F.G.S., Geology Department, versity of New England, Armidale. Rice, Thomas Denis, B.Sc., 44 Farnell Street, Glades- ville. Scott, John Alan Belmore, B.Sc.(Q’ld.), 28 Duncan Street, Punchbowl. STEVENSON, Barrie Stirling, B.E.(Mech. and Elec.) (Syd.), A.M.I.E. Aust., 21 Glendower Avenue, Eastwood. THuRSTAN, Arthur Wyngate, A.S.T.C., A.R.A.C.L., Metallurgist, 99 Stoney Creek Road, Beverley Hills. During the same period resignations were received from the following : Ph.D. Uni- Annison, Ernest Frank, Bloom, Pamela Lillian (Associate), Coleman, Patrick Joseph, De Lepervanche, Beatrice Joy, Durie, Ethel Beatrix, Fischer, Stephen, McGlynn, John Albert (Associate), Pickering, William Frederick. and the following names were removed from the list of members under Rule XVIII: Giffen, James Campbell; Kelly, Caroline Tennant. Statement Council. During the current year Messrs. C. L. Adamson, H. A. Donegan and Dr. A. Ungar served on this Committee. Since the last annual general meeting, following investigations and the Finance Committee, has :— Council, recommendations by Purchased a duplicating machine ; had monthly meeting notices duplicated instead of printed ; obtained approval to purchase office requirements through the Government Stores Department ; applied for exemption from payment of Sales Tax—the application was unsuccessful ; had the storeroom cleaned and back numbers of the ‘“‘ Journal and Proceedings’’ cleaned and packaged ; approached Mr. N. S. Rishworth to act as Honorary Solicitor to the Society. The Committee is currently investigating several other matters including the introduction of company membership, the investment of funds other than in gilt-edged securities, approaching the C.S.I.R.O. for an annual grant towards the cost of the Library, the financial structure of the other Royal Societies throughout Australia and approaching the State Government for an increase in the Government subsidy. (Signed) H. F. CONAGHAN, Hon. Treasurer. 7th April, 1965. 186 1964 30 89 4,194 29,693 185 £34,191 2,859 838 13 1 £34,191 ANNUAL REPORTS THE ROYAL SOCIETY OF NEW SOUTH WALES BALANCE SHEET AS AT 28th FEBRUARY, 1965 LIABILITIES Accrued Expenses Subscriptions Paid in Advance : Life Members’ Subscriptions — Amount carried forward : a Trust Funds (detailed below) — Clarke Memorial Walter Burfitt Prize Liversidge Bequest Ollé Bequest Accumulated Funds Employees’ Long Service Leave Fund Provision . Contingent Liability (in connection with Per- petual Lease). ASSETS Cash at Bank and in Hand .. Investments— Commonwealth Bonds and Inscribed Stock— At Face Value—held for: Clarke Memorial Fund Walter Burfitt Prize Fund Liversidge Bequest General Purposes Fixed Deposit—Long Service Leave Fund Debtors for Subscriptions. Less Reserve for Bad Debts Science House—One-third Capital Cost Library—At Valuation Furniture and Office Equipment—At Cost, Depreciation ; Pictures—At Cost, less Depreciation Lantern—At Cost, less Depreciation less 2,053 13 0 1,202 6 11 696 12 3 266 2 7 4,218 30,246 217 £35,306 1,800 1,000 700 4,840 oo°co°o ooco 107 107 14] SS 4,202 8,340 217 14,835 6,800 897 12 1 £35,306 14 11 18 12 15 — i OO Be lo oan) Go or Kor) a ANNUAL REPORTS TRUST FUNDS Walter Clarke Burfitt Liversidge Ollé Memorial Prize Bequest Bequest £. seid: £ 9S. %. 8S. di: £ s. d. Capital at 28th February, 1965 .. 1,800 0 0 1,000 0 0 700 0 O a Revenue— Balance at 29th February, 1964 .. 292 4 7 164 1 4 14 0 6 223 17 7 Income for twelve months .. 69 3 5 38 5 7 26 15 2 42 5 0 ; 361 8 O 202 611 40 15 8 266 2 7 Less Expenditure = ae 107 15 0 — 44 3 5 — Balance at 28th February, 1965 .. £253 13 0 £202 6 11 £3 7 9 £266 2 T ACCUMULATED FUNDS Eos. od. £ s. d. Balance at 29th February, 1964 .. 7 ee 29,692 15 4 Add— Decrease in Reserve for Bad Debts .. 9 6 O Adjustment—Subscriptions Refund .. 3 3 0 Surplus for Twelve Months e ay 593 5 6 30,298 9 10 Less— Transfer for Long Service Leave Fund Provision - a = .. 25 0 0 Adjustment—Salaries oe oe .. 9O 3 0 Adjustment—Subscriptions oe .. 4 4 0 Subscriptions Written Off ee tue VEO 5118 6 £30,246 ll 4 Auditors’ Report The above Balance Sheet has been prepared from the Books of Account, Accounts and Vouchers of The Royal Society of New South Wales, and is a correct statement of the position of the Society’s affairs on 28th February, 1965, as disclosed thereby. We have satisfied ourselves that the Society’s Commonwealth Bonds and Inscribed Stock are properly held and registered. HORLEY & HORLEY, Chartered Accountants. Prudential Building, Registered under the Public Accountants 39 Martin Place, Sydney, Registration Act, 1945, as amended. 25th March, 1965. (Sgd.) H. F. CONAGHAN, Honorary Treasurer. 187 188 INCOME AND EXPENDITURE ACCOUNT Ist MARCH, 1964, to 28th FEBRUARY, 1965 . ANNUAL REPORTS 1964 £* sed? 11. Annual Social ea, 38 Audit .. 37 16 0 50 Branches of the Society 25 0 0 104 Cleaning 151 5 O 45 Depreciation 47 17 6 69 Electricity 50 5 1 4 Entertainment 7 8-6 35 Insurance ae 36 10 1 147 Library Purchases 136 3 5 161 Miscellaneous .. si cf bs Bes Bis ae ag 195 5 2 131 Postages and Telegrams oF Ae a er i: id te 147 17 7 Printing— J ournal— Vol. 97, Parts 2-5 a ae £1,088 3 0 Binding .. bas au e 37 10 0 Reprints | 22 - ey Zoli 6) 0 Cotswold Collotype sf a 131 11 9 Postages .. az a 69 9 4 Provision for Vol. 97, Parts 6A and 6B a ot car 500 0 0O val - 2,108 0 10 Less— Sale of Reprints .. 956 7 6 Subscriptions (to Journal) 288 18 4 Back Numbers a ps 102 6 O Refund Postages .. 1718.8 Transfer — Clarke Memorial 409 | Kectute - ac a's ae 107 21k. .0 1473 1 6 = 634 19 4 187 Printing—General ad : ae Ke a: =e a 95 9 10 1,038 Rent—Science House Management Ey: a hs ¥ a 1,196 4 0 64 Repairs ua a3 e ca an os ae i sie 13 13 6 1,426 Salaries ee aa _ re of : 1501 7 O — Storage Expenses 169 16 3 39 Telephone 41 10 10 2,212 Surplus. for the Twelve Months 593 5 6 £6,170 £5,112 19 4 1964 i iS ke 955 Membership Subscriptions 980 3 6 7 Proportion of Life Members’ Subscriptions 6 6 O 750 Government Subsidy : Ae 750 0 O 2,024 Science House Management—Share ‘of Surplus : 2,362 3 7 234 Interest on General Investments bes 229 13 8 2,193 Sale of Library Assets 626 12 7 4 Donations : 5 3 Sundry Receipts 8 0 0 — Publication Grants Received | 150 0 0 £6,170 £5,112 19) 4 Section of Geology CHAIRMAN: H. G. Golding, M.Sc. Hon. SECRETARY: D. S. Bridges. Abstract of Proceedings, 1964 _ Five meetings were held during the year, the average attendance being about 16 members and visitors. March 20th (Annual meeting): Election of Office- beavers :—Chairman: Mr. H. G. Golding; Hon. Secretary: Mr. D. S. Bridges. Address by Mr. A. J. Gourlay: ‘‘Some Aspects of the Geology of Portuguese Timor ”’. “The address commenced with a brief outline of the history of geological investigation on the island. It was explained that, while many of the early investigations had for their main objective the collection of fossil material, the intricate tectonics of the island were also realised. It was concluded that the tectonics were of the alpine type, with thrust sheets resting on an intensely folded autochthonous substratum—giving rise to two stratigraphies differing widely—one appropriate to each complex. Investiga- tions from 1958 found the overthrust theory to be valid only up to Cretaceous-Eocene time, and only Permian rocks were found to be allochthonous. The stratigraphies of both the autochthonous and allochthonous complexes were outlined, and illustrated by a generalised stratigraphic column, showing average thicknesses, types of facies, and brief lithological descriptions. The autochthonous range in age from pre-Permian to Recent, all intervening ages being represented, and the overthrust consists of the Permian Upper and Lower Maubisse Formations. Attention was drawn to the similarities of many of the formations present to those throughout the Tethyan environment, extending from Europe through southern Asia to the East Indies, among these being molasse, flysch and block clay formations. It was seen that the facies present are characteristic of regions of both high and low relief, and that these conditions alternated from pre-Permian time to the present day. The address was concluded by some observations on the petroleum prospects of Timor. Possible source rocks in the Upper Cribas (Permian), Aitutu (Triassic) and Viqueque (Upper Miocene) Formations were indicated. Potential reservoir rocks were said to exist in the Cretaceous, in the Viqueque Formation and in the Coastal Plain (Plio-Pleistocene) Deposits. It was thought also that the folded and fractured Bedded Limestone Group of the Aitutu Formation has good secondary porosity. The possibility of anticlinal traps in the Cribas and Aitutu Formations, or of unconformity traps between the two Formations, or in the Aitutu Formation near the Tertiary onlap surface, was considered. Strong tectonic movements, however, might be detrimental to the forming of pools of large size ’’. May 15th: Address by Myr. K. R. Glasson: ‘““Some Observations on Overseas Ore Deposits ”’. “Four main areas were considered :— 1. The association of tin mineralisation and structural features near the granite-slate contact at South Crofty in Cornwell. Here, certain features common to the Mount Bischoff deposit in Tasmania were noted, especially in relation to the porphyry dykes. 2. In Ireland, the recently-discovered Tynagh lead deposit was compared with the well-known lead-zinc- copper mineralisation at Silvermines. Despite the strong stratigraphic control exhibited in both areas implying perhaps a_ syngenetic origin for the mineralisation, the bulk of the evidence is that the ore in its present position in both areas is controlled by structural features and an epigenetic origin could still be postulated regardless of the non-outcrop of granite. 3. In British Columbia, the Craegmont copper deposit was discussed in terms of the use of geo- chemistry and geophysics in exploration. This deposit has only recently gone into full production, but presents interesting features in terms of wall-rock alteration. 4. The Pima ore-body—a porphyry copper type in Arizona—was discussed briefly in relation to its geological setting ’’. July 17th: Address by Dr. A. D. Albani: ‘ Geology of the Northern Apennines, Italy ’’. Dr. Albani dealt with the stratigraphy of the autochthon, with the allochthonous cover of the ‘““argille scagliose’’ (i.e. liter. “‘ scaly clays’’), and with the tectonics of the autochthon. Discussing the stratigraphy of the autochthon, three formations were particularly stressed: the “anhydrite series’’, the ‘“brecciole nummulitiche’’ and the ‘“‘ macigno’”’ formation. The ‘“‘macigno’”’ and the “ brecciole ’’ were regarded as the product of the final settling down of turbidity currents. The Migliorini’s basic ideas of the ‘‘ composite wedge’’ as to primary tectonics have been illustrated, as well as the orogenic ‘‘landslips ’’ which are at the base of the formation of the allochthonous cover. Applications of the “composite wedge’’ to the Northern Apennines were discussed and illustrated. Finally, particular stress was laid upon the nature and age of the “exotics ’’ which are included in the allochthon. September 18th: Address by Mr. Jack Taylor: ‘The Collection and Cutting of Gemstones ’’. Mr. Taylor commenced by discussing the history of the uses of some of the more common gemstones, including quartz, chalcedony, agate, opal, sapphire, emerald, ruby, garnet, etc., and showed slides of the excellent ornaments produced with these gemstones in ancient times. Slides showing many recent cut and polished specimens of various gemstones were shown and explained. Of particular interest were the fine samples of Australian black opal displayed. Mr. Taylor then discussed the geographical distribu- tion of many Australian gemstone areas, and referred to the establishment of new Lapidary Clubs in many centres in New South Wales and Queensland, and to the aims and personnel of these Clubs. The address concluded with a discussion of the various methods 190 by which raw gemstones could be cut and polished to produce stones suitable for use in ornaments. November 27th: Symposium on “ Stratigraphic Problems on the Edge of the Great Artesian Basin ’’. Three speakers participated :— 1. Mr. M. Hind (Water Conservation and Irriga- tion Commission) :— ‘““The Great Artesian Basin has an area of about 600,000 sq. miles and a perimeter of about 4,600 miles. In N.S.W. the maximum thickness of Mesozoic strata is about 7,000 ft.; this occurs in the Moree Trough near the Queensland border. An overthrust fault in the basement forms the eastern margin of this trough, but it has not disturbed the Mesozoic sequence. ““The basement of the Basin consists mainly of metamorphic rocks, but granites occupy quite large areas in the floor of the Coonamble Lobe and the Eulo Shelf. Permian strata underlie the eastern part of the Coonamble Lobe, but they wedge out rapidly to the west. ‘““ Temperature gradients are lowest in the east where there is a great thickness of sedimentary strata. They rise steadily towards the west from 1-25°F/100 ft. in the Moree Trough to more than 3-5°F/100 ft. on the Eulo Shelf and in the western part of the Bulloo Embayment. There appears to be a definite relation- ship to the occurrence of granitic basement, either because of the better heat conductance of the granites, or because of radioactivity. ““ The Mesozoic sequence includes Triassic, Jurassic, and Cretaceous sediments. In N.S.W. the Triassic rocks appear to be confined to the eastern part of the Coonamble Lobe. The Jurassic strata are more widespread and cover the deeper parts of the Coonamble Lobe and possibly the Lila Trough, whilst the Creta- ceous overlap the Jurassic except at the eastern margin, and, with this exception, are believed to occupy the full area of the Basin in this State’’. SECTION OF GEOLOGY 2. Dr. J. A. Dulhunty (University of Sydney) :— “There is now no doubt regarding the correlation of Mesozoic formations throughout the _ districts between Dubbo and Gunnedah. Outcrops of the Jurassic Pilliga Sandstone and Purlawaugh Beds, with underlying Triassic sediments, have been mapped throughout the region. Some uncertainty still remains regarding the exact relations between the Triassic sections in the Sydney and Oxley Basins and in the south-eastern margin of the Great Artesian Basin. “ Recent investigations in the Gunnedah-Coonabara- bran district have established the fact that the Garra- willa Lavas, as originally defined by E. J. Kenny, are in fact extrusive and interbedded between the Triassic Napperby Beds and the Jurassic Purlawaugh Beds. Furthermore, it has now been established that trachyte flows, extruded from alkaline plugs in the Mullally-Tambar Springs-Rocky Glen district, are interbedded with the Garrawilla Lavas and are of Mesozoic age ”’ 3. Mr. L. R. Beddoes and Mr. P. T. Stafford (Esso Exploration Australia, Inc.) (delivered by Mr. L. R. Beddoes) :-— ‘“The Surat Basin has a total maximum section of more than 27,000 feet of Permian and Mesozoic sedimentary rocks. These rocks consist mainly of marine to continental shale, siltstone and sandstone. Lesser amounts of coal, conglomerate and tuff are present. The historical geology of the Basin and the stratigraphy of each formational unit is discussed in general terms. ‘‘ One of the main problems as concerns stratigraphy in the Surat Sub-basin is the varying nomenclature used by different workers. It is recommended that in so far as is practical, stratigraphic nomenclature be standardised throughout the Basin. If this is done, then the reader of geological literature can better relate local areas to the regional geological picture ’’. Annual Report of the New England Branch of the Royal Society of New South Wales Officers for the year were :— Chairman ; Jip eriestiey, Secretary—Treasurer: R. L. Stanton, Committee members: P. D. F. Murray, R. H. Stokes, N. H. Fletcher, N. W. Taylor, B. A. G. Plummer. Six meetings were held as follows: 9th April, 1964: Professor N. H. Fletcher, Depart- ment of Physics, University of New England, en. lice 21st May, 1964: Dr. L. E. Samuels, Superintendent of the Metallurgy Division, Department of Supply, on the “‘ Nature of metal surfaces ’’ 3rd August, 1964: Professor B. J. Mason, Depart- ment of Cloud Physics, Imperial College, Uni- versity of London, on “‘ Recent developments in the physics of clouds, rain and snow ”’ 21st September, 1964: Professor R. H. Stokes, Department of Chemistry, University of New England, on “‘ Why does salt dissolve in water ”’ 22nd October, 1964: Dr. D. B. Lindsay, Department of Biochemistry, University of New England, n ‘‘ How much insulin is there in blood ”’’. 13th November, 1964: Mr. Rowan Nicks, Senior Thoracic Surgeon, Royal Prince Alfred Hospital, on ‘‘The evolution of thoracic and cardiac surgery ”’ Financial Statement Credit balance of account at University of New England Banking Company Branch, Commercial of Sydney, as at 25th March, 1964 . £65 1 O Remittance from the Royal Society of New South Wales, 3rd July, 1964 we POU nO Interest to 30th June, 1964 ae ae 19 9 Interest to 30th December, 1964 .. ee a) mee ee Making a Total of .. £92 5 5 Expenditure Reimbursement of R. L. Stanton for expenditure on Society’s behalf (purchase of crockery, duplication, etc.) 2nd July, 1964 ae £10 10° O Duplicating charges by University of New England 7 10 5 Honorarium for Secretarial Assistance £3 3 O 5 Total Leaving a Balance of 3lst March, 1965. Obituary, 1964-1695 Victor A. BAILEY (1924) John R. BARDSLEY (1919) Frederick A. COOMBS (1913) Kenneth P. FORMAN (1932) Anthony G. FYNN (1959) Jack M. SOMERVILLE (1959) . £14 3 . £78 2 O R. L. STANTON, Hon. Secretary—Treasurer. - Medals, Memorial Lectureships and Prizes 1964 Max Rudolph Lemberg, D.Phil., F.R.S., F.A.A. 1965 M. Josephine Mackerras, M.Sc., M.B., M.C.P.A. 1964 Frederick David McCarthy, Dip.Anthr. 1964 Mollie E. Holman, M.Sc., Ph.D. 1964 Adrien Albert, Ph.D., D.Sc., F.A.A. 1964 Victor Albert Bailey, D.Phil.(Oxon.), F.A.A., Emeritus Professor, University of Sydney, was born in Egypt on 18th December, 1895, and died at Geneva, Switzerland, on 7th December, 1964. After graduation from Queen’s College, Oxford, he became a Demonstrator under Professor J. S. Townsend whose strong recommendation led to his appointment as Associate Professor of Physics in Sydney. He embarked on an intensive programme in this field, publishing many papers. In 1936 he was appointed Professor of Experimental Physics, and in 1953 Research Professor; on retirement in 1960 he was appointed Emeritus Professor. He published a total of 86 papers; some of them, notably those on ionised gases and the ionosphere remain as standard authoritative works. Three papers were published in the Society’s “ Journal and Proceedings’’ for one of which entitled ‘‘ Net Electric Charges on Stars, Galaxies and ‘neutral’ elementary particles ’’’, he was awarded the Archibald D. Ollé Prize for 1961. Not long before his death, Professor Bailey learned that the predictions on the Interplanetary Magnetic Field made by him in 1960 (and relevant to the paper for which he received the Ollé Award) had been confirmed by five U.S. Space Satellites. This news was received on the occasion of his visit to Rome for the Galileo Celebra- tions where he read three papers. In 1935, the Society awarded Professor Bailey the Walter Burfitt Prize. Other awards included the T. K. Sidey Medal and Prize by the Royal Society of New Zealand, by his appointment to Visiting Research Professorships in the U.S.A., and by his election to the chairmanship of a committee of the International Union of Scientific Radio. He was elected to membership of the Society in 1924. Professor Bailey is remembered by many of his colleagues for his outstanding achievements and lively personality. Professor Bailey is survived by his wife, two sons and two daughters. Frank Andrew Coombs, who died on 2lst October, 1964, was born in 1877 at Dunedin, N.Z. The late Mr. Coombs studied analytical and practical chemistry under Professor Black at the Otago Uni- versity in 1898-1900. In 1908 he came to Sydney. He applied for the position of Instructor in tanning and currying and was successful in being appointed ; James Langford Griffith, B.A., M.Sc. \ Joint John Roberts, Ph.D. J Award a position he held for 35 years. Mr. Coombs was the first to teach tanning, etc., in Australia or New Zealand, and the first man.to: tan a shark skin. Whilst teaching at Sydney Technical College, he studied at Sydney University, combining with his studies research in Australian barks, wattles, man- groves, eucalyptus, etc., in connection with tanning agents for the leather industry. He was a Fellow of the Chemical Society, and a foundation member of the Australian Chemical Institute. He introduced science into the Australian leather industry and formed the Australian section of the I:S.L.T.C., being its first President. Hor his segvices to this he was made an Honorary Life Member in 1948. - His work was known in Britain, U.S.A., France, Germany. During the last war, he was on loan to the Federal Government to inspect the leather for Army boots, etc. : Several of his papers on Leather, Barks, etc., have been read before the Royal Society of New South Wales and other societies. Mr. Coombs was elected to membership of the Society in 1913 and had had five papers published in the ‘‘ Journal and Proceedings’’ of the Royal Society of New South Wales. He is survived by his wife and three sons and one daughter. John Ralph Bardsley, a member of the Society since 1919, died on 26th February, 1965. Mr Bardsley was born at North Adelaide, South Australia, on 6th November, 1892. He was educated at the Public School, and then at Pulteney Street Church of England School. He came to Sydney with his parents and older brother George in 1902 when they started a family business. He attended Fort Street Boys’ High School 1903-08, and continued his studies at Sydney Technical College in Inorganic and Organic Chemistry, and other minor subjects, to assist him in his business as a hat manufacturer. During most of his business life, and until his death, he was a Director, and in charge of the laboratory and processing work at John Bardsley and Sons, Pty. Ltd. Mr. Bardsley is survived by his wife, four sons and two daughters. MEDALS, MEMORIAL LECTURESHIPS AND PRIZES Kenneth Phillip Forman, who died suddenly on 23rd October, 1964, while on a _ business trip to Melbourne, was born at Brisbane on 16th June, 1902. For the past seventeen years he had been the Australian Field Representative of the McGraw-Hill Publishing Co., New York, and was in charge of the field salesmen in the Far East. At the beginning of World War II, Mr. Forman was appointed to the Aircraft Production Commission, later the Department of Aircraft Production, and eventually took up duties in Washington, D.C., with Australian War Supplies Procurement. Prior to the war he was associated with EMAIL and the Westing- house organization. He was educated at Brisbane and in 1917 was dux of the Church of England Grammar School. Mr. Forman had been a member of the Society since 1932. He is survived by his wife and one son and one daughter. Anthony Gerard Fynn, the son of J. Fynn, Kilmore, Victoria, was born on llth September, 1899, at Yea, Victoria. He was educated at Xavier College, Kew, and at University College, Dublin. He entered the Society of Jesus, lst February, 1918, and was ordained Priest on 3lst July, 1933. 1920-23 he directed the _ seismological station, Dublin; studied Philosophy at Ignatius College, Valkenburg, Holland, 1923-26; taught Mathematics at Xavier College, 1926-30; studied Theology, Dublin and Austria, 1930-35; and was Professor of Philosophy and General Science, Loyola College, Watsonia, Victoria and at Canisius College, Pymble, N.S.W. He joined Riverview Observatory in 1958 and was appointed Director in 1959 which position he held until his death on 2nd February, 1965. Father Fynn prepared the vault and arranged with the U.S. Coast and Geodetic Survey that they install a set of standard instruments at Riverview, and make it a station of the world-wide standard network. The instruments commenced recording in December, 1962. Father Fynn had been a member of this Society since 1959. He was a member of the Council for the years 1960-63. During Jack Murielle Somerville, Professor of Physics in the University of New England, died suddenly on October 15th, 1964. Though his silver hair made him look older, he was only 51. He started his career as a mathematician and, after studying at the University of Sydney, he won a Barker Scholarship to Emmanuel College in the University of Cambridge, the traditional home of British Mathematics. When he returned to Australia 193 in 1937, however, he began to renew his interest in physics and in 1938 he was appointed as one of the foundation members of the staff of the New England University College where he was in charge of all teaching in both mathematics and physics. Thus began his long association with the present University of New England, an association interrupted for only four years during the war when he returned to Sydney University as Assistant Director of Radiophysics Training in a wartime school to train operators and technicians in the then new science of radar. The New England University College began as an institution more devoted to teaching than to research, but on his return to Armidale in 1945 Professor Somerville began the nucleus of a research group which today has some 20 permanent. staff members and 15 post graduate research students. When the University of New England was created in 1954, he was appointed as its foundation Professor of Physics and continued as Head of the Department of Physics until his death. Under his leadership research groups were built up in ionospheric physics, solid state physics and in his own particular field of interest—the physics of 1onized gases, or plasmas, and the electric glows, arcs and other discharges which may occur in them. In this field he was an internationally known expert. He published some 20 papers in scientific journals as well as a monograph on the Electric Arc. He had been invited to write a new book on Spark Channels for an international series on discharge physics and at the time of his death this work was about half written. The many students who have passed through the University of New England Physics Department in the last 25 years will remember Professor Somerville as an inspiring teacher and one who delighted in simple demonstrations, particularly of electrical pheno- mena. He avoided mathematical complexity wherever possible and liked to discuss difficult problems from first principles. To those who became research students and to his colleagues on the staff he was a very dear friend who could always be looked to for advice and help in any complicated situation and for a well-chosen story to lighten the occasion. He was much sought after on committees both within and outside the University and was a member of the Committee at present drafting the new Science syllabus for secondary schools in New South Wales, a member of the Council of the Australian Institute of Nuclear Science and Engineering and a member for many years of the Council of the University of New England. Professor Somerville will be sadly missed by his many friends and colleagues. His permanent memorial will be the Department of Physics which he founded in New England University. Professor Somerville was elected to membership of the Society in 1959. Citations James Cook Medal Max Rudolf Lemberg took his Ph.D. in Breslau in 1921, and of the subsequent 44 years, 30 have been spent in Australia. After some seven years of organic chemical research his attention turned in 1928 to the chromoproteins of red algae; he succeeded for the first time in isolating the prosthetic groups of phyocyanin and phycoerythrin, and established their structures as the bile pigments mesobiliviolin and mesobilierythrin respectively. Through these studies his interests were turned definitely and permanently to biochemistry, and to the pyrrole pigments in particular. Over the period 1933-1949 he made important contributions to knowledge of the chemistry and structure of many bile pigments, and to the mode of their formation by degradation of haemo- proteins. During this period he built up a knowledge of the pyrrole pigments and haemoproteins which enabled him to publish with J. W. Legge in 1949 ‘“Haematin Compounds and Bile Pigments ’’, which because of its extraordinary scope, in depth as well as in breadth, will long be the definitive text in the field. During the studies of the degradation of haemoglobin to bile pigments, compounds had been observed with spectroscopic and apparent chemical relationships to haem a, the prosthetic group of cytochrome oxidase. The structures of some of these compounds (cryptoporphyrin PI and crypto- porphyrin i) have recently been established in his own laboratory ; they are derivatives of protoporphyrin, and the relationship of their structures to porphyrin a is not as close as was suspected. Nevertheless these observations perhaps stimulated JLemberg’s interest in haem a and the cytochromes a, which have furnished the main theme of his studies from about 1949 to the present. At the Haematin Enzymes Symposium in Canberra, of which he was President, the culmination of ten years study of haem a came with his announcement of most of the details of its structure. Since that time his attention has turned more and more from the prosthetic group to the whole cytochrome. He described in 1962 the pre- paration of compounds resembling the natural haemoproteins a, formed by combination of haem a with a variety of pure proteins and lipids, and showed the importance of lipids in the natural cytochrome complex. More recently, his studies of native cyto- chrome oxidase are clarifying the nature and mode of action of this supremely important enzyme. Lemberg’s scientific papers at present number well over 100 and in addition he has published many reviews and general articles. Lemberg’s work and writing are characterized by great scholarship and depth. His thinking is supported by knowledge and understanding which range over the whole field of current biochemical research, and this has frequently allowed him to advance fruitful hypotheses well ahead of experimental confirmation. This was exemplified by his penetrating and imaginative postulate (1949) that the biosynthetic pathway to haems lay through the condensation with glycine of an intermediate arising from the tricarboxylic acid cycle, leading to a key monopyrrolic precursor with acetic acid and propionic acid side-chains. It was not until years later that this was shown indeed to be the case. Dr. Lemberg has been a member of the Society since 1936; has served on Council and was President in 1955. In 1954 Dr. Lemberg delivered the Liversidge Research Lecture entitled ‘‘ Chemical Structure and Biological Function of the pyrrole pigments and enzymes ’’. Clarke Medal Dr. Mackerras (nee Bancroft) graduated M.Sc. at the University of Queensland and M.B. at Sydney. She held a Walter and Eliza Hall Fellowship and practised medicine. Dr. Mackerras was a Research Officer, C.S.I.R. Department of Entomology, Canberra, from 1930 to 1947. During World War II, she served five years with the rank of Major, being in charge of the entomological side of anti-malarial research. From 1948 to 1961, she was Parasitologist at the Queensland Institute of Medical Research, and is still a part-time Principal Research Officer in the C.S.I.R.O.’s Depart- ment of Entomology. Her distinguished work on entomology and parasitology from the medical stand- point is attested by a bibliography of some 70 papers by herself or in joint authorship with T. H. Johnston, with her husband Dr. I. M. Mackerras, and other colleagues. CITATIONS 195 The Society’s Medal The Society’s Medal for 1964 is awarded to Mr. F. D. McCarthy for distinguished contributions to anthropology and service to the Society. Mr. McCarthy’s contributions to the fields of archaeology and cultural anthropology have been impressively numerous and varied but also of the highest standard. His scientific reputation stands high in overseas archaeological and anthropological circles, as well as here in Australia and we feel that this award is a fitting tribute to a scholar who has done much to advance these disciplines. Mr. McCarthy has been a member of the Society since 1949 ; has served on the Council and was elected President in 1956. Recently, Mr. McCarthy was appointed Principal of the Australian Institute of Aboriginal Studies in Canberra. Edgeworth David Medal The morphology and pharmacology of the autonomic effect or systems have been intensively studied since the last century but it is only within the last decade or so that striking advances have been made in our understanding of the physiology of smooth muscle. This has come about largely because of the application of modern electrophysiological techniques and parti- cularly the use of the intracellular electrode. The use of the intracellular electrode was pioneered by Dr. Bulbring and her colleagues at Oxford in 1954 using the smooth muscle fibre in the rabbit’s sphincter pupillae and immediately applied by her to the taenia coli preparation in the guinea pig. It was very soon after this (1956) that Dr. Mollie Holman went to the Department of Pharmacology at Oxford to work under Dr. Bilbring. Here she mastered the techniques involved in the taenia coli preparation and published two important papers on the effects of changes in the ionic environment on the electrical and mechanical activity of smooth muscle. With these papers she established herself as one of the pioneers in the field of smooth muscle physiology and she has continued to play a leading part in the various developments that have taken place since that time. While in Oxford she first became associated with Dr. Burnstock in a partnership which was subsequently to be resumed when she returned to Melbourne. In addition to their physiological studies Burnstock and Holman have also made important contributions to the pharmacology of smooth muscle. Recently, as associates of Dr. Neil Nerrillees, they have published a correlation of the fine structure and physiology of the innervation of smooth muscle in the guinea pig vas deferens using the electron microscope. The importance of the contribution that Dr. Holman has made to the physiology of smooth muscle, and the international reputation she has established for herself has been indicated by the fact that she and her colleague Dr. G. Burnstock were invited to con- tribute the chapter ‘‘Smooth muscle: autonomic nerve transmission’’ in the Annual Review of Physiology, 1963. - CLT ELE — one ee a Ms x i. £-fi4 + + i y : i ; - a —— j ‘ ‘ fe ‘ t 4 i — 5 > > apes f ay als \ os 14 eo Pha: : i ca . ‘ 1 * a p . SU { i i Me a ~ oe ats ‘. 4 ‘i xs : ; : | - Royal Society of New South Wales t . . | OFFICERS FOR 1965-1966 . bh sep HS j | i { H i | hess President A, A. DAY, B.Sc, Ph;D. sf Oe en wanes eM ee, _ Vice-Presidents ci Wi HUMPHRIES, B.SC.) 4 ere _ W. HG. POGGENDORFF, B.SceAgr. : _ HL at McKERN, M.Sc. © - R, J. W. Le FEVRE, Dsc., F.R. S.) FAA. ee oe py a CAS ne 1 am : Honorary. Secretaries H : | A. REICHEL, Ph.D., esc. Honorary leeaauees H. F. CONAGHAN, mse. A eae Ce Soe ee ‘Members of Council TAA faut : se: Wie ee eo Le J. MIDDLEHURST, m.sc. ee Ne Ow, “HARPER, M.Sc. at ate J. W. G. NEUHAUS, a.s.t.c. ye A. KEANE, pPh.p., MESCe i." | W. H. ROBERTSON, Bisc. -T. E. KITAMURA, B. Ai; BiSecAgrs R. L. STANTON, php. nt Be. gee hOY, Ph, ae M.Sc. . ACUNG AR 2 Deng. 0 Go ee ae eed uy) eee NOTICE ‘the ‘Hoyal Society of. New. “South ‘Wales ‘originated in 1921 as the ‘ Philosophical Society of Australasia *’ ;, after an interval of inactivity it was resuscitated in 1850 under the name of the “ Australian Philosophical Society ’’, by which title it was known until 1856, when the name was - changed to the ‘‘ Philosophical Society of New South Wales’”’. In 1866, by the sanction of Her _ Most Gracious Majesty Queen Victoria, the Society assumed its present title; and was incorporated te sae of ‘Parliament of New South Wales in 1981. | ¥ is é y al - : x ' \ ik ¢ “2 y ; y ‘ ‘ AN t Sas x Ke < , 3 Gas : Para +h i ; wd = (2 PS » ~ fx ¥ 4 a i F 7 , "> " tees A he we i OR ‘ Ne eS f ! ‘ \ ae gee % a . | ‘ : f ie re Ss ad ° Seton eles : Be th ais a7. riensis Carpentier (Peltaspermaceae). John A. = ree : RE Sys 2 ae : es Be mai : Be e 2 . 203 ae = : = x Jennings | rmian Sediments from the Lower Hunter Valley of = 8 i " ak ee tee Poe as m4 \ sat 5 So : . eats Pee he ~" See BS ag iE ITAEON pe ee 82h BETS, SYDNEY Puy asa periodical == N OTICE TO AUTHORS | _ General. to the Honorary Secretaries, Royal Society of New South Wales, required : copy; together with two additional copies of the abstract typed on separate sheets. generalystyle adopted in this Journal. - They should be as concise as possible, consistent with adequate presentation. Particular attention ‘should be given to clarity of expression and good prose style. — ; The? typeseript» should be Houde re bed, : preferably on quarto paper, with generous side - margins. Headings should be typed without underlining ; if a paper is long, the headings should also be given in a table of contents typed on a separate sheet, for the Set of | the Editor. 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Ss Dye-line or photographic ‘copies. os heal diagram should be sent so that the’ originals need not be sent to referees, thus’ eliminating Pideners pba. Pictenraaaee ‘Eau ae a cluded only where essential, should be glossy, - ‘When several ye board in the Dida 1 passe Seat for es in : rage ; > Geological - Pancha ee proposed must also submit the letter of app Reprints. Authors who are oe ek ne Journal and Proceedings, Royal Society of New South Wales, Vol. 98, pp. 197-202, 1966 Current Trends in Solid State Science The Pollock Memorial Lecture Dr. FREDERICK SEITZ President, National Academy of Sciences, U.S.A. It is my privilege to spend this hour honoring your great physicist Professor V. A. Pollock by . attempting to give you a broad review of the field of solid state physics—a field which has not only been remarkably coherent during several centuries of the development of western science, but has also been highly productive both as a source of the kind of enlightenment for which we value science so much and as a contributor to technology. In examining the evolution of any field of science, we may note that the process of develop- ment often resembles somewhat the evolution of a mining operation. In the early stages of mining for a new and relatively little used material, one focuses on very rich deposits which give the most concentrated products that can be recovered and used most easily or directly. In fact only such deposits may have significant value in the early stages of the mining operation. Later, as the material being sought becomes more useful, and as the technology for developing it expands, one may find that leaner, lower-grade deposits are exceedingly important. In fact, the major wealth associated with exploitation of the mineral may eventually be associated with the relatively leaner deposits, as is true, for example, for the highly mechanized production of gold in the South African mines of the Rand Area. Something quite analogous to this pattern is visible in the history of the opening of major areas of solid state science, as the field as a whole has gone through successive cycles of advance. In any one stage of development, attention is focused initially on major principles. Many of the details stemming from the principles are, in the main, of intellectual interest only to those few who have a very special appetite for them. Ultimately, however, as the know- ledge of a given area becomes absorbed into useful technology, what were initially regarded as secondary facets of the subject may come to have practical interest. Thus, as time goes on, the apparently leaner aspects of the subject can become of very great practical importance. By way of introduction, let me remind you that the crystalline solids formed by the elements and their compounds can be classified into four broad categories, namely, the salts, metals and alloys, valence crystals, and organic or molecular solids. The alkali halides and alkaline earth oxides are typical salts. About 70 per cent of the pure elements are metallic, that is, are good electronic and thermal con- ductors and tend to alloy readily with one another. Carbon, silicon, germanium, gray tin, and silicon carbide are typical valence crystals. The organic, or molecular solids, comprise the most diversified group, ranging from simple systems like solid carbon dioxide to quite complex crystalline polymers, such as_poly- ethylene, or the natural organic polymers which play such an important role in biological systems. The four categories are not all pure, for many materials have properties that lie intermediate between these of two or more types. For example, there are many alloys which are very close to being electrical insulators and resemble the salts or valence crystals in compo- sition and atomic arrangement. A number of salts and valence crystals, which are good insulators at low temperatures, become electronic conductors at elevated temperatures because bound electrons become free as a result of thermal excitation. These solids are, of course, the semi-conductors; the _ electrons which become free may be either the normal bonding electrons in the valence shelves or may be associated with distinctive impurities or foreign atoms which are added. * Delivered at the University of Sydney, Sydney, Australia, August 1-26, 1965. A 198 In a similar way, the various areas of develop- ment of solid state science may be broken into five major fields which interlock closely with one another, although the “mining” of each of the fields generally started at different times on the historical scale. The five fields are as follows: 1. Macroscopic Properties Lattice Structure bo 3. Electronic Structure. 4. Imperfections 5. Surface Properties. The macroscopic properties are concerned with those characteristics of solids that can be measured on specimens having substantial size, that is having linear dimensions of the order of millimeters, or larger. Initially, the studies were concerned with the geometrical relationships of natural-formed crystals, usually mineralogical specimens, and led to _ the formulation of laws such as those governing the constancy of angles between neighbouring faces in a given crystalline habit form of a specific compound. Eventually the study was extended to the measurement of mechanical, electrical, magnetic, and thermal properties of the specimens in various crystalline directions and various temperatures. The subject is sometimes referred to in terms of the “ tensor ”’ properties of crystals. Systematic studies of natural specimens of this type were responsible for the discovery of piezoelectricity and pyro- electricity. Although such effects were initially of purely scientific interest, they eventually led to very important applications of crystalline Specimens, such as in polarizing prisms, piezo- oscillators, and sonic transducers. A desire to broaden the range of available crystals, starting in the early part of this century, inspired the evolution of a number of techniques for growing large single crystals of interesting materials. Such crystals have turned out to have great technical value in their own right in numerous applications such as in relation to jewelled bearings, magnetic materials, transistors, optical lenses and prisms for the ultraviolet and infrared, and ultimately in the field of laser research. Among the tech- niques used for growing crystals are those of evaporation of aqueous solutions, stress anneal- ing, the Kyropoulos method (drawing from the melt), the Bridgman method based on use of the thermal-gradient baffle, the boule or arc- melting method, the zone method and hydro- thermal techniques. DR. FREDERICK SEITZ It is particularly interesting historically to note that natural radio-activity was discovered by Becquerel incidental to the study of the physical properties of many crystalline materials. Similarly, superconductivity was discovered by Kammerlingh Onnes in 1911 as the result of a systematic investigation of the conductivity of metal at low temperatures. Although we think of crystalline masers and lasers, which generate coherent electromagnetic radiation in the high radio or optical range of frequencies, in quite modern terms because they were developed in the recent past as a result of the study of quantum phenomena in gases and molecular beams, the action of these solid state systems actually can be regarded to lie in the macroscopic domain since the underlying pheno- mena depend on the co-operative interplay of the entire assembly of radiating atoms with the radiation field. Thus, even though the study of the macroscopic properties of crystals is old, the field continually yields new dividends as more and more techniques in which the macroscopic properties of crystals can play a role are developed. Lattice Properties. At the time of Dalton, early in the last century, when the atomic hypothesis was gaining ground, the conjecture was offered that the regular form of natural crystals implies an orderly stacking of the constituent atoms into lattice-like array. In brief, it was postulated that crystals contain a basic geometric unit of atoms or molecules, the lattice cell, which is repeated over and over in a periodic way in three directions. This relatively speculative concept evolved steadily during the last century, until, near 1900, imaginative scientists began to propose detailed structures for the simpler crystalline compounds. In the meantime, the geometrical theory of three dimensional lattice arrays had been worked out in much detail by mathe- maticians, starting with Bravais in 1830, and extending on toward the end of the century. The study of the lattice properties of crystals entered into a completely new era when in 1913 it was discovered that crystals diffract X-rays in a manner determined by the lattice arrangement. This discovery was augmented by the discovery of electron diffraction in 1929 and neutron diffraction in 1944. At first, diffraction techniques were used to determine the properties of the simpler inorganic crystals. Eventually, however, the methods were em- ployed both in the investigation of more complex inorganic organic structures such as the silicates CURKENT TRENDS IN SOLID STATE SCLENCE and of relatively imperfect crystals. The highest points in the development of diffraction tech- niques achieved thus far occurred in the last ten years in connection with organic crystals, for example, in the discovery that the long mole- cules in crystals of polymers are folded, and in the discovery that the molecules of Deoxyribose Nucleic Acid (DNA), which enter in such a crucial way in gene material, are double spirals, each member of the spiral being closely correlated along the length according to precise rules of combination. One can only feel a sense of inspired awe when contemplating the fact that the early speculations on the lattice properties of crystals nearly 150 years ago eventually led to the evolution of techniques- for determining the pattern of arrays in the genetic material responsible for the replication of biological species. Along somewhat different lines, it may be noted that the dynamic properties of the crystal lattice have made it possible to use crystalline materials to obtain valuable specialized in- formation regarding nuclear energy levels in a number of elements. When a stationary, isolated nucleus emits or absorbs a gamma ray, the net momentum transferred to the nu- cleus is sufficiently large that the absorbed and emitted quanta have energies significantly different from the spacing of the nuclear levels involved in the transition. On the other hand, when the nucleus is in an atom bound into a crystal, it is possible, under proper circum- stances, for the entire crystal specimen to absorb the momentum so that the energy of the absorbed or admitted quanta is very nearly the same as the nuclear level spacing. This effect, discovered by Mossbauer, makes it possible to use crystalline emitters and absorbers to obtain much detailed knowledge concerning nuclear energy levels. Electronic Properties. In the 1880's, early in his long and productive career, the Dutch physicist H. A. Lorentz postulated that insu- lating materials contain bound charges which are held in position by harmonic forces, much like weights which are attached to a fixed point by an ideal spring. The existence of such changes had been surmised earlier from the laws of electrochemical equivalence but they had not been employed previously in con- sidering the dynamical properties of atomic structure. In terms of this picture, Lorentz was able to explain the variation of the optical dielectric constant of crystals near regions ‘where the crystals absorb light. In this way the concept of the electron entered solid state 199 science. Much more tangible evidence for the electron was developed a decade later when investigators began studying the fragments of atoms produced in gaseous discharges. Then, at the turn of the century, Drude proposed that metals contain a gas of free electrons which are responsible for their high electrical conductivity and started a very fruitful period of study of metals. The understanding of the electronic properties of solids remained in a very primitive state until quantum mechanics was developed about 1925. Following that, it became possible to discuss the detailed behaviour of the valence electron in many crystalline materials. In- vestigation of the wave equation showed that the energy levels of electrons could be grouped into bands whose relationships gave, in turn, a simple and direct explanation, not only of the characteristic differences between metals and insulators, but of the ways in which transitions between the two types of materials occur. By 1940 one had an excellent semi- quantitative understanding of the behaviour of the valence electrons in many typical simple solids. The development of electronic computers during and after the war made it possible to expand the detailed investigation of the elec- tronic states in solids on a relatively enormous scale. Today, because of such computers, it is feasible to hope to obtain quite detailed knowledge of the levels or bands in many monotomic or diatomic solids. Studies of this kind have been accelerated substantially by the widespread practical interest in the detailed behavior of conduction electrons in the useful semiconductors such as silicon and germanium, and the compounds of elements in the third and fifth columns of the periodic chart. One of the greatest triumphs of the electron theory of solids has been the achievement, within the last decade, of a high degree of understanding of the phenomenon of super- conductivity, particularly as a result of the work of Bardeen, Cooper, and Schrieffer. These investigations have shown that in cases in which the free valence electrons in the metal are disturbed sufficiently by the vibrations of the crystal lattice, or, to use the accepted language, interact sufficiently strongly with them, this interaction may have a significant influence on the behaviour of the motion of the electrons relative to one another. At relatively low temperatures, within a few degrees of the absolute zero, this effective electron interaction, originating in the inter- 200 action of the electrons with the lattice vibra- tions, may cause the electron gas to freeze into a mode of motion in which pairs of electrons which move in opposite directions with equal momentum are closely correlated even though they may be separated in space by many atomic distances. This correlation not only influences the way in which the electron gas conducts an electric current, inducing typical superconductive characteristics, but also deter- mines the behaviour of the electrons in a magnetic field. In effect, the ideal homogeneous specimen behaves like a perfect diamagnetic for which the permeability vanishes (Meissner effect), that is it rejects lines of magnetic force. --The development of a consistent quantum mechanical theory of superconductivity has given an enormous impetus to the study of the entire field of superconductivity in recent years. Out of this work has emerged not only the discovery and refinement of many new superconducting compounds but also the dis- covery that the magnetic field associated with a supercurrent is quantized, that is, its intensity is restricted to discrete values which depend upon the geometry of the supercon- ducting system. On the technical side, the refined studies have made it possible to construct permanent superconducting magnets which can produce magnetic fields in the vicinity of 100,000 Oersted. The superconductors used in such magnets, usually termed hard supercon- ductors, have the property that they are not physically homogeneous and are able to retain lines of magnetic force that are trapped at imperfections in a way not yet thoroughly understood. The trapped lines of magnetic force reside near the centre of vortices of super- current. Still further, there has been extensive study of the way in which conduction electrons flow from one superconducting metal to another as the spacing between the two is varied from zero to many atomic distances (tunneling effects). Such developments promise to yield an enormous amount of additional information concerning superconductivity, some of which may have very useful consequences. The methods of mathematical analysis used in the theory of superconductivity are based ‘on a combination of the methods of field theory, first developed in connection with high energy particle physics, and the methods of ‘many-body theory, developed to handle pro- blems involving the co-operative action of many particles. The success of this approach to the problem of superconductivity has opened DR. FREDERICK SEITZ a large doorway to the theoretical investigation — of many other problems of solid state science. Imperfections in Crystals. The concept of the ideally perfect crystal in which the lattice array is entirely unblemished is an abstraction normally realized only on a quite microscopic scale within a larger specimen. All real crystals contain varying degrees of imperfection. It was recognized very early in the history of the development of crystal science that imper- fections are present in typical specimens. Indeed many irregularities could be seen with the naked eye, under the microscope, or dis- cerned indirectly by chemical analysis. It was also recognized very early that imperfections must play a significant role in affecting the physical and chemical properties of specimens since the properties could be made to vary by altering the imperfections. On the technological side, the control of accidental or intentional additions or structural features has always been an important part of the practical lore in fields such as ceramics and metallurgy. Practical studies showed, in fact, that imper- fections may be relatively inert in some cases ; whereas they may have profound effects upon the properties in others, such. as im” the ‘case of additions of carbon in iron. To give another example, the entire field of crystalline luminescence underwent a_ vast development in the first quarter of the present century in the hands of the chemists, who studied the influence of various foreign additions on the luminescent properties of salts when irradiated with ultraviolet light, X-rays, or ionizing particles. Along similar lines, it was noted that the semi-conducting behaviour of many substances such as selenium, tellurium, and lead sulphide is critically dependent upon the presence of foreign atoms. Still further, it was found that the ductility of relatively plastic crystals such as metals and salts could be influenced enormously by changing the state of perfection of the specimens. Following 1925 there was a strenuous attempt to catalog the possible imperfections that could occur in crystals and to sort out the influence which they have upon the physical and chemical behaviour of such solids. This work actually did not come to complete fruition until after World War II, when the subject received international attention on the massive scale which the postwar support of science made possible. It was then realized that the types of imperfections which can occur in solids are rather small in number. The great diversity of effects arising from the imperfections is to a CURKENT DRENDS IN SOLID STATE SCIENCE considerable degree a result of the complex interactions between imperfections which can occur. Basically there are three families of imper- fections, namely: point imperfections, such as foreign atoms present in the lattice either substitutionally or interstitially, or vacant lattice sites produced by removing atoms from the lattice (vacancies) ; electronic imperfections such as additional free electrons in an otherwise insulating matrix, generated, for example, by adding an atom with a loosely bound electron to the lattice; line imperfections, generally termed dislocations, such as may be produced by permitting the atoms on opposite sides of a planar area within the crystal bounded by. a line or curve to slide past one another by one cellular distance in such a way as to cause a pattern of disregistry along the bounding line. Each of these three basic types of imper- fections can not only interact with imperfec- tions of the same type but can also interact in various ways with the other two tvpes to produce a wide variety of effects. It has been demonstrated, for example, that the plastic properties of simple crystals are closely associ- ated with the ability of the linear dislocations described above to move through the lattice when it is placed under shearing stress. The interaction of dislocations with one another and with foreign atoms provides an explanation of the sensitivity of such plastic flow to cold work (extensive deformation) and to foreign atoms. Although a large part of the research carried out in the field of solid state science between 1945 and 1960 was devoted to the clarification of the influence of imperfections on the pro- perties of solids, the field still provides an enormously fruitful area for further research, particularly as new techniques for investigation are developed. Moreover, there are a number of facts which are not at all well understood. It is known, for example, that special crystals, such as zinc and cadmium sulphide, undergo a special type luminescence (electroluminescence) when placed in an oscillatory electric field. Investigations show that the emitted radiation probably originates near imperfections ; never- theless the nature of the interaction between the applied field, the luminescent centers, and the imperfections is not at all clearly under- stood at the present time. Surface Properties. Every real crystal is bounded by a surface. Such surfaces have been studied systematically over many decades 201 in an attempt to evolve systematic knowledge of the surface properties. The initiating investigations, in areas which still continue to be productive, were carried out by chemists concerned with such phenomena as_ surface adsorption and surface catalysis. In close relation to this, chemists and miuneralogists studied the nature of crystalline layers formed by depositing one compound on the surface of another (e.g., epitaxy). : In a similar way, metallurgists have studied the influence of intercrystalline boundaries in polycrystalline materials (grain boundary etlects): Since 1945, several new types of studies have given added impetus to the investigation of surfaces. For example, Professor Mueller showed that one could obtain very interesting information about the atomic arrangements of the base material and deposited materials in the outer layers of point electrodes which were placed in electric fields sufficiently strong to induce field emission of electrons. I have been pleased to see important extensions of this work in the CSIRO laboratories in Mel- bourne. While this work has been rather specialized in the sense that it is focused on the use of a few metals, it has given a wealth of information concerning the influence of the underlying crystalline arrangement on foreign layers on the surface of such metals. Soon after the war, John Bardeen pointed out that the conductivity of thin semi-con- ducting layers or filaments could be greatly influenced by the nature and condition of the surface. He emphasized that surface atoms had their own characteristic electronic energy levels, and that these levels could influence the number of conduction electrons present in a region near the surface. Since the pattern of surface atoms can be influenced in turn by adsorption, it follows that under proper circum- stances there can be a correlation between volume conduction and surface conditions. Still more recently, a number of investigators have developed techniques for studying dif- fraction of electrons of very low energy by crystalline surfaces. Such electrons, having energies near 100 electron volts, do not penetrate the specimen by more than a few atomic distances, so that the diffraction pattern 1s characteristic of the outer layers. Many indi- viduals place high hopes on the promise of this new method of study for obtaining pro- found information on a wide diversity of surfaces. This approach to the study of surfaces 202 has been featured at the recent Melbourne Conference on Diffraction. In spite of the progress that has been made over the decades in the study of crystalline surfaces, one must admit that the field is unfolding relatively slowly. Although there presumably will come a day when there is as much understanding of the surface properties of solids as we have at present of the volume properties, it does appear that a whole new regime of development will be needed to achieve that goal. My own involvement in the science of solids now goes back somewhat over 30 years beginning with the early development of the theory of electron bands in solids. It is interesting to contemplate that a very major fraction of the quantitative and qualitative knowledge of solids which we possess at present has been developed over that span, in spite of the fact that the field is, in itself, several hundred years old. If I attempt to analyze my own experiences over this period, I find that one of the most remarkable features, apart from the advance in understanding, has been the fact that the interest in detailed facts has grown so much. In the 1930's, it seemed quite reasonable for one person to be familiar with © practically all of the available literature con- cerning solids and much of the implication of the work. Now a typical good investigator may devote a number of years to one highly specialized facet of a given family of compounds and have relatively little knowledge of a topic which, although fairly closely related to his DR. FREDERICK SEITZ interest, is not immediately tied to it. Coupled with this increasing concern about detail has been a vast growth in the number of highly competent scientists working in the field and in the range of knowledge which has direct applied interest. From the detailed study of properties, there has been spawned families of devices including a large array of transistors, a spectrum of magnetic materials for trans- formers and recording devices, luminescent screens of varied use, superconducting magnets and crystalline lasers. One might reasonably ask whether the field of solid state science is in its infancy or its old age. It clearly is not in its infancy for we now have far too much accumulated knowledge of the properties of a wide family of solids to assume that the field is not mature. Moreover, there are very few outstanding mysteries extant at present, as was true when I entered the field some 30 years ago. On the other hand, I cannot help but feel that there is still a vast amount of valuable “ ore”’ left in the study of solids. The realization of that ore in the future will depend upon the careful and systematic study of detailed properties of many compounds, using all the battery of physical and chemical techniques which are now available and can be devised in the future. In a sense, the field can be looked upon henceforth as somewhat in the nature of a very sophisticated branch of chemistry, which will persistently yield signi- ficant new discoveries if a host of competent investigators continue to pursue a wide varietv of investigations. Journal and Proceedings, Royal Society of New South Wales, Vol. 98, pp. 203-214, 1966 On Lepidopteris madagascariensis Carpentier (Peltaspermaceae) JoHN A. TOWNROW (Botany Department, University of Tasmania) (Communicated by C. T. McErroy) ApstTrRact—The pteriodosperm leaf Lepidopteris madagascariensis Carpentier, hitherto very little known, is redescribed from material coming mainly from the Gosford Formation of the Narrabeen Group (Lower Triassic) of New South Wales. The distinction between L. madagas- caviensis and L. stormbergensis (Seward) Townrow is discussed, and some specimens reclassified. Evolution in Lepidopteris is considered and its stratigraphical range discussed. Introduction The leaf Lepidopteris Schimper belongs to the small pteridosperm family, the Peltaspermaceae Thomas (1933), recently discussed and extended by Townrow (1960). In that discussion, two leaf species could be little utilised, they were too ill known, L. stutigardiensis (Jaeg.) Schimper, the Type, from the German Upper Triassic, and L. madagascariensis Carpentier, from the Triassic of Madagascar. L. madagascariensis has been somewhat eclipsed by the commoner L. storm- bergensis (Seward) Townrow, but proves to be a useful and well characterised species. It is, in part, Lower Triassic in age, and serves to tie in the Permian L. martinsi (Kurtze) Town- row more closely with the rest of the Family. It may also prove to be useful stratigraphically. Nothing is known of the reproductive structures of L. madagascariensis. Descriptions FAMILY PELTASPERMACEAE Thomas (Pteridosperms) GENUS LEPIDOPTERIS Schimper Lepidopteris madagascariensis Carpen- tier et Figs. 1-4 1907 Alethopteris nov. sp. Dun p. 155. Mention in bore log. Material here re-examined. ? 1908 Thinnfeldia sphenopterordes Seward, pp. 94-95 ; pl. 4, fig. 2 only ; Uppermost Beaufort, S. Africa., pl. 5, fig. 2 is distinct. 1927 Lepidopteris stutigardiensis du Toit, non Jaeger, pp. 400-401, pl. 28, from the uppermost Beaufort. "2 1927 Callipteridium africanum du Toit, p- 404, pl. 27. From the uppermost Beaufort ; unusually large leaf. PI. 26, figs. 2, 3 are distinct. Lepidopteris madagascariensis Carpen- tier, p. 14, pl. 3, figs. 3-5, pl. 5, figs. 4 and ? 6, from the Sakamena Group, Madagascar. Lepidopteris madagascariensis Carpen- tier: Carpentier, p. 9, pl. 5, fig. 4 and ? 5-7, from the Sakamena Group, Madagascar. Lepidopteris stormbergensis. ‘Townrow, non Seward, p. 23, text figs. 2A, H; 3B; 6 A, B. Brookvale, N.S.W., Hawkesbury Sandstone. Lepidopteris madagascariensis Carpen- tier: Townrow, p. 339. Note only. Holotype: Carpentier, 1935, pl. 3, figs. 3 and 4. Locus typicus: Amboriky, Madagas- car; Sakamena Group, Lower Triassic. 1935 1936 ? 1956 1960 Diagnosis emended. Leaf bipinnate up to 28 cms. long, with about 15 pinnae, emerging at 90° or more, at base of leaf, angle diminishing to about 60° at apex. Pinnae 0-75-1-5 cms. apart, margins usually not touching. Pinnules from 2°5mm.x1-°:25mm. to 6mm.x3 mm.; normally not overlapping one another, often slightly separated, usually entire, or with slightly lobed margins, obtuse apex, and margins usually parallel over nearly all the length of the pinnule. Venation extremely obscure, consisting of a midrib and laterals arising at an angle of about 45° to the midrib every 0:75mm. approximately. Zwischer- fiedern arising on or near the lower (abaxial) rachis surface, two or three between pinnae, somewhat rhomboidal, apex very obtuse, 1-3 mm. long and same wide. 204 JOHN A. TOWNROW Substance of leaf thick ; margins not scarious and is, on the usual scheme of dating, upper- nor thickened. Cuticle thick, 3u and more (measured here, and subsequently, in folds), showing more or less equidimensional four to six sided cells set in no order or arrangement, and unmodified at margin. Stomata scattered in about equal numbers over both surfaces of leaf. Veins not or scarcely marked in cuticle either by cells modified in shape, or by non-stomatiferous zones. Epidermal cells having outlines 1-5y-6u thick, not or only slightly sinuous, sinuosities formed by pits though cell outline with swollen parts of the outline between them. Cells about 23u across (15u-38y). General cuticle surface flat or showing low solid papillae ; sometimes thin areas of cuticle or a system of radiating fine lines present over each cell. Stomata monocyclic, showing no preferred orientation, subsidiary cells consisting of a ring of four to seven (usually five) subsidiary cells with strongly thickened radial cell outlines, and often whole ring of cells forming very strongly cutinised unit. Guard cells very weakly cutinised, sunken in a pit formed by the overhanging subsidiary cells. Each subsidiary cell bearing solid cutin lappet on its dorsal surface very close to stomatal pit. Lappets varying much in size, usually directed somewhat upward and also forward over (often about closing) stomatal pit. Rachis showing wide lumps, up to 2mm. in diameter, sometimes paired, a pair occupying whole width of rachis. Lumps low showing only two or three rows of compressed cells round their margins, and (probably) never overhanging one another. Trichomes (as in other species) present but rare. Description. The material examined consists of 12694 (Part and counterpart) Geological Survey N.S.W. from the Balmain Shaft, Sydney ; other leaves collected by Mr. R. Helby and myself at Turrimetta Head, one mile North of Narrabeen, N.S.W., now deposited in the University of Sydney, Department of Geology ; and further more fragmentary but more abundant material collected by my wife and me at Turrimetta Head on a_ subsequent occasion. Figured material of this collecting along with material collected at Coal Cliff, N.S.W., is in the Australian Museum. The Turrimetta Head material comes from the Upper Narrabeen (Raggatt in McElroy, 1962), most Lower Triassic. No leaf is complete, Fi12694 (ply ae tie) 1) is the most nearly so, and none show the base. However, as in other species of Lepidopteris, the pinnae and pinnules are borne close to one surface of the rachises, sometimes being over- lapped at their bases by the compressed rachis (figs. 2a, b). In L. stormbergensis where there were leaf bases available, the pinnae are borne on or near the upper (adaxial) rachis surface, and it is by analogy with L. stormbergensis that the leaves of L. madagascariensis are orientated. This question is of importance in the matter of stomatal distribution and possible ecology. Observed directly, the rachis shows wide but low lumps, varying greatly in size. At one extreme (fig. 2a) the lumps each occupy about half the width of the rachis, and their compressed edges stand out: at the other the rachis may be nearly smooth, and the lumps seen only with difficulty, for they are obscured by longi- tudinal compression folds. This situation is seen on the pinna rachis. On the parts of two leaves (Colls. of Sydney University), the lumps are paired, or sometimes paired, each pair apparently being connected below. This point is of interest for comparison with L. martinsit. Though there is fairly good evidence that the lumps on the rachis originate beneath a trichome, there is no evidence as to what caused the paired arrangement of the original trichomes, and whether paired or not, the lumps, so far as can be seen, are of the same sort (pl. 1, fig. 3; fig. 3e, and Townrow, 1960, fig. 2). The paired arrangement might be merely accidental—there is no room for more than two on one side of the rachis. On the rachis cuticle the somewhat concentric pattern of cells seen on the other species is present, and in a few places the trichome beneath which the lumps form (fig. 3e¢ and see Townrow, 1960, pp. 336-340). When compressed, however, the lumps contrast strongly with those of L. ottonis (Goepp.) Schimp., for only a few cells at their margins are crushed (compare pl. J, fig. 3 and Antevs, 1914, pl. 1, fig. 5). This confirms that by comparison with L. ottonis, the lumps are small. On one leaf (fig. 2b) the lower rachis surface shows the remains of tufts of pinnules, which pass into the zwischerfiedern. On F12694 such tufts are definitely absent, on F51729 they may be present, but the rachis is broken and the situation obscure. On all leaves showing the zwischerfiedern clearly the basiscopic one arose on, or nearly on, the lower (abaxial) leaf surface, WOURNAL ROYAL SOCIETY N.S.W. TOWNROW PLATE 1 Explanation of Plate PLaTE I—L. madagascariensis Fic. 1.—The most complete leaf available, F12694, x0Q-75. Fic. 2.—Lower cuticle, showing cell and stomatal arrangements (note, veins not visible). F51726, x25. Fic. 3.—Part of a rachis and adjacent pinnule, showing compressed edges of the lumps. F51726, x 25. aoe ON LEPIDOPTERIS MADAGASCARIENSIS CARPENTIER 205 Explanation to Figures TEXT-FIG. 1 Lepidopteris madagascariensis, form of leaf and venation. A. F51726. B. University of Sydney. C. F51728, Turrimetta. D. F51730, Coal Cliff, x2. E. University of Sydney. F. F51729. G. F51727, Turrimetta, xX 1. 206 JOHN A. TOWNROW By Sy LIP OE es “ eat TEXT-FIG. 2 L. madagascariensis, A-C: Thinnfeldia callipteroides, D. A. Adaxial rachis and pinna rachis surface, showing torm of lumps. University of Sydney, x10. B. Abaxial rachis surface, showing insertion of zwischer- fiedern, and remains of a tuft of pinnules on the rachis surface. University of Sydney, x10. C. A stoma from the rachis with large cutin lappets and an irregularly dicyclic stoma. F51731, x650. D. A stoma and surrounding cells note cutinisation round stomatal pit, and border to cell outlines. Oakdale State Colliery, Burragorong Valley, x 650. ON LEPIDOPTERIS MADAGASCARIENSIS CARPENTIER 207 TEXT-FIG. 3 L. madagascariensis, A, C-F: L. stormbergensis, B. A., C., F. cuticle (F lower leaf surface) showing arrange- ment of cells and stomata, in A including margin. A. F51729, C. University of Sydney, F. F51731, x 100. B. cuticle at pinnule margin, note narrow cells at margin, and vein at top, and bottom of fig. F378 (377), x80. D. Stoma closed by cutin lappets, and with whole apparatus heavily cutinised, A.M. 6399, x 490. E. trichome from rachis, and slight profileration of cells round it, in a more or less radial pattern. Uni- versity of Sydney, x 490. 208 JOHN A. TOWNROW TEXT-FIG. 4 L. madagascariensis, B-E; L. stormbergensis, A. A. somewhat open stoma, irregularly dicyclic, with hollow papillae over stomatal pit, sinuous cell outlines, and low papillae. F378 (377), x840. B. stoma com- pressed partly sideways, showing orientation of lappets, possibly as in life. University of Sydney, x 490. C., E. rather open stomata showing (c) sinous cell outlines only rarely seen in L. madagascariensis. F51730, F12694, x 490. : D. a stoma, showing holes in more or less straight cell outlines, solid (?) upward pointing cutin papillae and lack of encircling cells. University of Sydney, x 840. ON LEPIDOPTERIS MADAGASCARIENSIS CARPENTIER 209 while the acroscopic one arose on the upper (adaxial) leaf surface. The lowest pinnule on a pinna was decurrent onto the main rachis (fig. 1e). The form of the pinnules and variation is given in the diagnosis and shown in pl. 1, fig. 1 and figs. la-g. Since the veins do not show in the cuticle, and are only seen with much difficulty on a few hand specimens, they can scarcely have projected in life. There are two alternative explanations. Either the leaves were thick, or the veins very small. There is no suggestion that the leaves were succulent, but I think it is quite probable that they were thick and leathery, for beside the evidence from the veins (as it is interpreted), the margin shows no modified cells, but there may be wrinklings in the cuticle, suggesting the compression of a rather thick organ. The absence of special marginal cells suggests that the leaf maintained the same thickness to the edge (fig. 3a). The distribution of stomata is of considerable interest. In general, there is little difference between the two leaf surfaces in stomatal number (density and stomatal index). However in F12694 the cuticles are of different thick- nesses, 3u. and 1-5u, and the thinner cuticle is attached to the lower rachis surface (determined as above). Here, it is the thinner cuticle that has the more stomata (60/mm.?: 40/mm.?, S.I. 13-2: 8-3). On another leaf, however, Colls. of Sydney University, orientated in the same way, it is the upper surface that shows more stomata (58/mm.?: 69/mm.?, S.I. 8-0: 10-0). The cuticle is shown in pl. 1, fig. 2 and figs. 3a, c, f. The cell outlines are usually straight, or with only the minutest projections, however, some specimens show what appear to be sinuous cell outlines. Examined under high magnification, the cell outlines show numerous narrow perforations, complete or nearly so, between which the outline swells out (fig. 4d). In this plant, therefore, the middle lamella is not sinuous. In the present material the veins are quite invisible on the cuticle ; however, in one leaf now identified with L. madagascariensis (V/32106, see below) the veins do show as obscure rows of narrower cells (Townrow, 1956, ag. 3B). Most stomata look like those figured in figs. 2c; 4d, e. The lappets do not show an area within themselves of lighter shade (cf. Townrow, 1956, fig. 4), and so are solid. In some specimens they project upwards, as seen by focussing. In most they probably projected upwards for fig. 4b shows a stoma compressed partly laterally, in which the lappets point upwards at about 45°; but stomata on this leaf com- pressed dorsi-ventrally appear to project only over the stomatal pit, which they largely close. With the orientation suggested for them, it is hard to see how the cutin lappets can have had much effect on transpiration. A few stomata in this as in the other species, lack lappets, their places being taken by a narrow rim of cutin (see Townrow, 1956, fig. 6B and fig. 4C). Certain stomata (fig. 4d) show thick cutin bulges out onto the dorsal guard cell surface, _the bulges corresponding to the edges of the subsidiary cells. In these, presumably, the dorsal wall of the guard cell, that it shares with the subsidiary cells, is more or less strongly cutinised. In other stomata, especially on those leaves with a thick cuticle, the whole area round the stoma is densely cutinised (fig. 3d). This cutin, from focussing, appears to extend far down the radial cell walls, so that there is an apparent interruption between the out- ward outline of the subsidiary cell, and the outlines of the other epidermal cells. As in L. stormbergensis, there is normally thickening on the subsidiary cells on the cuticle surface (Townrow, 1956, fig. 4 E, F). One or two leaves (Colls. of Sydney University) show internally brown more or less circular masses, which do not dissolve in alkali. They may be resin. Discussion of the specimens referred to L. madagascariensis. The material now identified as LL. madagascariensis includes one leaf (V/32106) coming from Brookvale previously (Townrow, 1956) placed in L. stormbergensis. This leaf was recognised as unusual for L. stormbergensis having small pinnules, a thick cuticle showing straight or nearly straight cell outlines and only low (or no) papillae on the epidermal cells. It is not normal for L. madagascariensis either. It shows the course of the veins on the cuticle by files of elongated cells, and generally shows hollow papillae, not solid lappets over the stomatal pit. With hesitation this leaf is now reclassified as L. madagascariensis, since I think it diverges less from it than from L. stormbergensis. It is now probable that the Queensland material referred by me (Townrow, 1960, p. 343) to L. stormbergensis should be reclassified. The specimen regarded as a pollen sac group of Antevsia extans (Fren uelli) comes from the 210 uppermost Beaufort Series, and so probably does not belong with L. stormbergensis, which as far as is known comes from the Molteno Group only (see du Port, 1927. ple 29 ies and Townrow, 1960, p. 352). However, this affects neither the nomenclature nor the ascrip- tion of other material to A. extans. The nature of du Toit’s specimen is now left open. Carpentier’s (1935, 1936) material lacked a cuticle, but it shows a rachis having wide but low lumps, either paired (1935, pl. 3, fig. 4) or paired and alternate (1936, pl. 5, fig. 4), rather well separated pinnae and parallel sided obtuse pinnules. Thus it agrees with the commonest sort of leaf in my material and differs from JL. stormbergensis. Carpentier (1936, p. 11) says that his material is perhaps identical (“‘est peut-étre la méme’’) with L. stuttgardiensis of Zeiller from Madagascar. This is highly probable, but Zeiller’s material has never been figured. Du Toit’s (1927) Lepidopteris stutigardiensis is removed from that species, as it has only small lumps on the rachis. In gross form and size it agrees closely with the present material. There is no cuticle. No definite opinion is expressed on du Toit’s Callipteridium africanum (1927, pl. 27) from the uppermost Beaufort Series, nor on Seward’s (1908, pl. 4, fig. 2) leaf called Thinnfeldia sphenopteroides Seward. This material is all poorly preserved, and atypical in one way or another, for example it is unusually large. However, should Seward’s leaf finally prove to be identical his name will have priority. The leaves shown by du Toit (1927, pl. 26) are much too large and are excluded. There are a number of old records of Alethopteris (none figured) from lower in the Narrabeen Group (listed by Raggatt in McElroy, 1962, p. 13), especially from the Balmain Shaft. Much material from Balmain is in the Geological and Mining Museum, but I have failed to find L. stormbergensts . Thin leaf substance More or less pointed pinnules . Irregularly placed lumps on the rachis . Distinctly sinuous cell outlines, unpierced by holes 5. Irregularly dicyclic stomata, the stomatal pit being (mostly) overhung by hollow papillae 6. Leaf margin thin, epidermal cells over margin elongated. mothe JOHN A. TOWNROW these particular specimens. However, L. madagascariensis does occur in the Lower Narrabeen Group. Figs. 1d, 2c, 3f, 4e show specimens collected at the base of the cliffs North of Coal Cliff beach, and occurring in a shale some 15 feet below the conglomerate layers marking the base of the Bulgo Sandstone ; they thus lie at the top of the Stanwell Park Shale (see Hanlon, Osborne and Raggatt, 1953). The material is variable, and fragmentary, but it corresponds with the younger leaves at every available point: the only possible difference being that the stomatal pit may overhang the guard cells less than in the Turrimetta Head leaves. There does not seem to be any reason why the Stanwell Park material should not be identified. When in fragments, L. madagascariensis could be confused with the leaf Thinnfeldia callipteroides Carpentier (1935) with which it is sometimes associated. Indeed, I think this has happened and that some of the “ Alethopteris ”’ of the older records is T. callipteroides. Given complete leaves, there need be no confusion, T. callipteroides branches several times in a rather irregular way (see Carpentier, 1935, pl. 3, fig. 1) and, as far as known, the rachis of T. callipteroides is smooth. The cuticles are superficially similar, but (i) T. callipteroides has a thicker cuticle, 10 or more in folds; (ii) the cell outlines are thick and often show a sort of border absent in Lepidopteris (fig. 2d), and (iii) the stomatal pit is bounded by a massive cutin structure, recalling the cutin rim of some species of Ctenozamites Nathorst (Harris, 1964, p. 89), which is sometimes produced into. (probably upward pointing) papillae, (fig. 2d). The further delimitation and affinities of T. callipteroides are left entirely open for the present. Comparison of the species of Lepidopteris. The two Southern Hemisphere species, L. stormbergensis and L. madagascariensis can be distinguished as follows (see Townrow, 1956, 1960) : L. madagascariensis Thick leaf substance Mostly obtuse pinnules Lumps on rachis often (not always) paired Cell outlines straight, or minutely sinuous, often: pierced by holes Stomata monocyclic, the stomatal pit being: (mostly) overhung by solid cutin lappets Leaf margin unmodified. ON LEPIDOPTERIS MADAGASCARIENSIS CARPENTIER The three Northern species are unequally known and so rather difficult to treat. The Type species L. stutigardiensis (see Townrow, 1956, for further references) from the Schilff- sandstein of the German Keuper is only known as casts lacking detail. In outline the leaf is like L. madagascariensis, but shows the imprints of large to very large irregularly placed lumps on the rachis. JL. ottonis (see Antevs, 1914, Harris, 1932) has a thick leaf substance, but more or less pointed pinnules, large to very large irregularly placed lumps on the rachis, and on the cuticle the veins are generally visible as files of elongated cells. L. martinsi (see Townrow, 1960) comes close to L. madagas- cariensis, but can be distinguished because it is often tripinnate, the lumps on the rachis are large and it lacks perforated cell outlines. It must be emphasised, however, that the five species of Lefidopteris form a very close knit group. The difference just discussed will separate most specimens (about nine out of ten), but there is intergrading and will probably always be specimens whose classification is doubtful, especially among poorly preserved material. Discussion 1. The possible ecology of Lepidopteris and its evolution. There is some evidence that Lepidopteris belonged to an herbaceous plant. A cutinised, hence primary, stem has been ascribed, on evidence of association and anato- mical resemblance, to L. ottonis (Harris, 1932) and L. stormbergensis (Townrow, 1960). In addition, in L. stormbergensis it was found (Townrow, 1960, pp. 343-344) that some leaves showed more stomata on the upper leaf surface than on the lower; while other leaves had the opposite stomatal distribution. It was also found that in some waterside herbs (but not -usually thick 211 in trees) a similar pattern of stomatal distri- bution was present. Those leaves with more stomata on the upper leaf surface come from the lower nodes, those with more stomata on the lower leaf surface came from the upper nodes. It is now found (above p. 209) that some leaves of L. madagascariensis have a stomatal distribution like L. stormbergensis. Against these facts, which seem to point towards an herbaceous plant, there are two which point towards a woody plant. In L. ottonis there is not the stomatal distribution just discussed for L. stormbergensis. The lower leaf surface, apparently generally, shows the majority of stomata. The cuticles of Lepidopteris are (3u.): this can be matched among plants growing in wet places today, especially in the Ericaceae and Epacridaceae, but these plants are woody, though often of low stature. The force of this analogy is open to some question, and I think the points suggesting an herbaceous habit are the more impressive. Those facts bearing on the relationships of the Peltaspermaceae, whose leaf is Lefidopieris, have been discussed earlier (Townrow, 1960, pp. 358-359). The information now available for L. madagascariensis adds nothing to that discussion. However, L. madagascariensis serves to tie in to the Upper Permian L. martinsi1 much more closely with the rest of the Family. L. martinsw and L. madagascariensis resemble one another, and together differ from the other species, in having paired lumps on the rachis, lateral veins in the pinnules that are (usually) unforked, and a stomatal structure that appears indistinguish- able to me. The ages of the Lepidopieris leaves are as follows (see also Townrow, 1960) : L. martiunsu Upper Permian Northern Hemisphere L. madagascariensis Lower to Middle Triassic Southern 5 L. stormbergensis Middle and Upper Triassic Southern . L. stuttgardiensis Keuper Northern os L. ottonis Rhaetic Northern ys The lumps on the rachis probably arise by The tufts of pinnules on the rachis lower proliferation of the sub-epidermal cells beneath a trichome (Townrow, 1960, pp. 340). In L. martinsit the lumps so formed are large and often paired. In the two Southern species the lumps are small, sometimes absent in L. stormbergensis but L. madagascariensis may retain the paired arrangement. In the two Triassic Northern species the lumps are large but irregular. surface, seen in L. martinsit are retained in both Southern species (at least on some leaves) : they are not seen on L. ottonis, while in L. stutigardiensis the preservation is too poor to Say with assurance that they are absent, but none of the figures suggests their presence. The stomatal structure of L. martinsu and L. madagascariensis is very close (fig. 4d and Townrow, 1960, fig. 35). L. stormbergensis 212 shows hollow papillae, but L. ottonis retains the solid cutin lappet. However, it generally lies not on the dorsal cell surface, projecting upwards, but on the edge of the stomatal pit, and projects (usually) horizontally (Harris, 1932). Finally, L. stormbergensis unlike the other species (L. stutigardiensis 1s unknown) has a rather thin leaf. One explanation of the information just summarised is that there was parallel evolution in the Northern and Southern Triassic species of leaf; sometimes one group of species retaining a feature of the earliest L. martinsziz, sometimes the other. This is of considerable interest for it suggests that: while the Family was Northern in origin, and reached the Southern continents in the Lower Triassic (like a good many other sorts of plant as Balme, 1963, shows), once established in each Hemisphere, the groups of species in each evolved with little (or no) reference to the other. That is, that migration from one to other Hemisphere was not maintained in the later Triassic. If, with Roselt (1962), we regard Calliptertanthus anhardtit Roselt as allied to the peltasperms, a similar conclusion emerges from the pollen organs. More information is needed to carry this speculation any further, or to decide whether the sort of behaviour suggested is found in other groups of plants. 2. Southern Triassic floras containing Lepidopteris. Lepidopteris stormbergensis 1s known from the Molteno Group of South Africa, and from the Hawkesbury Sandstone of New South Wales (Townrow, 1960, text fig. 5G). The Molteno Group has been dated as Middle Triassic, but the discovery of sauropods in it (Dr. J. Cosgriff pers. com.) places it in the Upper Triassic. The Brookvale shale lens lying near the top of the Hawkesbury Sand- stone, is dated as Middle Triassic on its fishes by Wade (1935). No Lepidopteris has yet been found in the Rhaeto-Liassic (Dettmann, 1961) of South Australia or Tasmania: neither is it found in the Ipswich Coal Measures, though these are dated by Jones and de Jersey (1947) and de Jersey (1962) as Middle to Upper Triassic. It does, however, occur in the Esk Beds, whose top is equivalent to the base of the Ipswich Coal Measures. Provisionally therefore, L. stormbergensis is called a Middle and partly Upper Triassic species. It does not, on present evidence, reach the Rhaetic, and may not enter the equivalent of the Norinic. JOHN A. TOWNROW The Lepidopteris from the Hawkesbury Sandstone, though small in amount is very interesting. The leaf from the Brookvale shale lens has already been discussed (p. 6), since it comes intermediate between L. stormbergensis and L. madagascariensis. There is other similar material in the Geological and Mining Museum coming many years ago from a shale lens at Woolloomoolloo, also towards the top of the Hawkesbury Sandstone. Though all the specimens are given one number (F 388), there is so much variation that I think it likely that at least two leaves were originally present (M 426 and 429: M 411, 428, 377 and 378). These specimens too are intermediate between L. stormbergensis and L. madagascariensis. They show mostly papillate cells, many sinuous cell outlines, files of elongated cells over the veins and (in some) a thin leaf margin, and mostly hollow papillae over the stomatal pit (figs. 3b, 4a), characters of L. stormbergensis. However, they also show thick cuticles (5u or more in folds), and in M 429 with M 426 the thin leaf margin is missing and at least half the stomata show solid lappets, and these are features of L. madagascariensis. Three out of the four specimens from the Hawkesbury Sandstone are atypical and inter- mediate between L. madagascariensis and L. stormbergensis, and though one, V 32972 has typical characters of L. stormbergensis, none have typical characters of L. madagascariensis. This rules out the possibility that we are dealing with a mixture of the two species. Perhaps at this horizon L. madagascariensis is evolving into L. stormbergensis, or we may be dealing with a population distinct from either. With present knowledge, to describe it as a new species would merely confuse the taxonomy of Lepidopterts. L. madagascariensis occurs in, and helps tie together, two Lower Triassic floras. One flora, ‘with abundant Dicroidium and other forking leaves, is well seen in du Toit’s (1927) South African flora from Brown’s River. It is also seen in Walkom’s (1925) flora from Turrimetta Head, towards the top of the Narrabeen Group. The Brown’s River flora occurs in sandstone at the top of the Cynognathus zone of the Karroo tetrapod zones, and is thus uppermost Lower Triassic. The Narrabeen flora cannot be extrinsically dated, but is usually given also as uppermost Lower Triassic. The other flora is seen in Carpentier’s (1935, 1936) Sakamena flora, the Sakamena being placed by Lehman (1952, pp. 190-196; 1961, pp. 151-152) at the base of the Triassic. In ON LEPIDOPTERIS MADAGASCARIENSIS CARPENTIER this flora Dicrotdium is almost or quite absent. In Australia a flora showing much in common with Carpentier’s appears in the roof shales of the Bulli Seam, also lacking Dicroidium, also basal Triassic (Hennelly, 1958). Lepidopteris is not known from the Bulli flora. The oldest record of L. madagascariensis is the one referred to above from the Stanwell Park Shales (upper Lower Narrabeen Group). Here it occurs with Thinnfeldia callipteroides Carpentier—common in the Bulli roof shales—and leaf fragments with a Dicroidium-like cuticle. This statement ignores even older records that may be of Lepidopteris, but in absence of figures or material, and in view of the fact that the concept of all the species involved has altered since the records were made, one must ignore these records. The interesting fact thus emerges that in New South Wales, and Madagascar, there is a basal Triassic flora which, unlike floras from the later Triassic, is not dominated by the Corystospermaceae. By the top of the lower Triassic, however, the Corystospermaceae had become dominant, as at Turrimetta Head and Brown’s River. It is not possible to say yet when one flora changed into the other, and this information is much to be desired. The discovery of Dicroidium-like fragments in the Stanweil Park Shales suggests that the basal Triassic flora without Dicroidium did not last long. Contrary to Walkom (1925) but in agreement with Hennelly (1958) and Balme (1963) I can see very little of a Glossopteris flora in Carpen- tier’s basal Triassic flora, or in material from the Bulli roof shales. It is conceded that the occasional specimen of Glossopteris Brongniart or Phyllotheca Brongniart may be found, and Schizoneura Schimper and Mougeot is common to both. But the whole appearance of the flora, with its abundant conifers, Thinnfeldia callipterovdes and (in Madagascar), Lepidopteris is quite unlike a Glossopteris flora. Acknowledgements I am much indebted to Mr. H. O. Fletcher and Miss D. Jones (Australian Museum), Dr. John Pickett (Geological and Mining Museum) and Dr. G. Packham (University of Sydney) for much help and for the permission to examine their material. I thank Mr. R. Helby (Geological Survey of New South Wales) for taking me to the Turrimetta Heads locality. To Drs. J. Cosgriff (Tasmania), A. Carter and C. T. McElroy B 213 (New South Wales) and, especially Professor T. M. Harris F.R.S. (Reading), I am grateful for much useful criticism. References ANTEvs, E., 1914. ‘“‘ Lepidopteris ottonis (Gopp.) Schimp. and Antholithus zeilleri Nath.”’ ie Svensk. Vet.-Akad. Handl., 51 (7): 1-18. BatME, B. E., 1963. ‘‘ Plant microfossils from the Lower Triassic of Western Australia’’. Palaeont- ology, ©: 12-40. CARPENTIER, A., 1935. ‘‘ Etudes paléobotaniques sur le groupe de la Sakoa et le groupe de la Sakamena (Madagascar) ’’. Ann. geol. serv. Mins. Govt. gen. Madagascar. 5: 7-82. CARPENTIER, A., 1936. ‘‘ Additions a l'étude de la flore du groupe de la Sakamena’’. Ibid., 6: 7-11. DETTMANN, M. E., 1961. ‘“‘ Lower Mesozoic mega- spores from Tasmania and South Australia ’’. Micropalaeontol., 7: 71-86. Dun, W. S., 1907. “Sydney Harbour Colliery: section of Strata’’. Ann. vep. Dep. Mins. N.S.W., 1907: 154-161. pu Toit, A. L., 1927. “ The fossil flora of the Upper Karroo beds’’. Ann. S. Afr. Mus., 22: 289-420. FLorin, R., 1940. ‘“‘ The Tertiary fossil conifers of South Chile and their phytogeographical signi- ficance’’. K. Svensk. vet.-Akad. Handl., (3) 19 (2): 1-107. Harris, T. M., 1932. ‘‘ The fossil floras of Scoresby Sound, E. Greenland’’. Part 2. Description of seed plants incertae sedis. Meddl. Gvronland, 85 (3): 1-112. Harris, T. M., 1964. ‘“ The Yorkshire Jurassic Flova’’ Il. Caytoniales, Cycadales and Pteri- dosperms, 191+ -viii. Brit; Muss “(nat. hist.) London. Hanton, F. N., OSBORNE, G. D., AND RaGGatTtT, H. G., 1953. ‘‘ Narrabeen Group: its sub-divisions and correlations between the South Coast and Narrabeen—Wyong districts’’. Proc. roy. Soc. N.S.W., 87: 106-120. HENNELLY, J. B. F., 1958. ‘‘ Spores and pollens from a Permian-Triassic transition, New South Wales ’’. Proc. Linn. Soc. N.S.W., 83: 363-369. DE JERSEY, N. J., 1962. ‘“ Triassic spores and pollen grains from the Ipswich coalfield’’. Qld. Dep. Min. Pubdl., 307: 1-18. Jonus, ©. As and De ersny, IN J tote “dhe flora of the Ipswich Measures—morphology and floral succession’’. Pap. Dep. Geol. Univ. Qld., n.s., 3: 1-88. . LEHMAN, J. P., 1952. ‘‘ Etude complementaire des poissons de lEotrias de Madagascar ’’. i¢ Svensk. vet.-Akad. Handl., 4 (2) @: 1-201. Leuman, J. P., 1961. ‘‘ Les Stégocephales du Trias de Madagascar’’. Ann. Paleont., 47: 1-47. McEtroy, C. T., 1962. ‘1: 250,000 Geological Series Maps. Explanatory notes. Sydney, N.S.W.”’ Bur. min. Res. Geol., 1-48, Canberra. RosEtt, G., 1962. ‘‘ Untersuchungen zur Gattung Calliperis ii. Callipterianthus anhardtii n.g.n. sp. die erste durch Zusammenhang erwiesene Callip- tevis Fruktifikation’”’. Freiburg. Forsch., C131: 29-38. 214 JOHN A. TOWNROW SEWARD, A. C., 1908. ‘‘ Fossil plants from South Townrow, J. A., 1960. ‘‘ The Peltaspermaceae, a— Africa’’. Quart. J. geol. Soc. Lond., 44: 83-108. pteridosperm Family of Lower Mesozoic age’’. Tuomas, H. HamsHaw, 1933. ‘‘On some pterido- Palaeontology, 3: 333-361. spermous plants from the Mesozoic rocks of Wabe, R. T., 1935. ‘‘ The Triassic fishes of Brookvale, South Africa”. Phil. Trans. ‘voy. Soc: Lond., New South Wales’’, 98+-viii, Brit. Mus. (nat. B 222: 193-256. hist.) London. Townrow, J. A., 1956. ‘The genus Lepidopieris Watkom, A. B., 1925. ‘“‘ Fossil plants from the and its Southern Hemisphere species’’. Norsk. Narrabeen Stage of the Hawkesbury Series ’.’ Vid.-Akad. Oslo. Mat.-naturv., K1., 1956: 1-28. Pyoc. Linn: Soc. N.S.W., 50>, 214-224. Journal and Proceedings, Royal Society of New South Wales, Vol. 98, pp. 215-219, 1966 The Big Hole near Braidwood, New South Wales J. N. JENNINGS Australian National University, Canberra (Received 20th December, 1965) ABSTRACT—A survey and observations of the Big Hole are regarded as supporting the view that it is a subjacent karst doline due to solution of inferred Silurian limestone lying uncon- formably beneath the ridge of Devonian sandstone and conglomerate in which it lies. Its combination of large size and a high depth width/ratio is exceptional for the landform type and a structural cause is invoked since it is probable that the hmestone would occur as a narrow, steeply dipping strike belt. Sudden collapse of a cave roof in the limestone explains the Big Hole’s characteristics better than gradual stoping of the sandstone through solution at the top of the limestone. The inference that the solution must have been deep phreatic in nature presents a problem for the formation of the large cave involved. The Big Hole is a deep pit which abruptly interrupts the wooded north-eastern flank of a ridge about half a mile east of the Shoalhaven River 20 miles south-south-west of Braidwood in the Southern Tablelands. Recent descents by the Canberra Speleological Society have been made the occasion of measuring its dimensions and making other observations which bear on the origin of this remarkable feature. General Description It is a pit of angular plan with a maximum diameter of 175 feet and a minimum of 100 feet at right angles.! Since the hillslope in which it is set is steep, there is a difference of about 50 feet between the highest south-western part of the lip of the pit and the lowest north-eastern part. The depth from the highest lip to the lowest part of the pit is 360 feet whereas the depth from the lowest lip to the floor beneath is 240 feet. Although the Big Hole opens near the top of the ridge, its bottom reaches a level some 80 feet below the gently inclined and marshy valley floor to the east. Most of the way down, the walls are nearly vertical to slightly overhanging, with occasional small ledges and overhangs in the bedding planes. Below the eastern corner there is a vegetated slope about 100 to 120 feet down. Near the bottom greater overhangs have developed on the north-eastern side and, most of all, on the south-western side where there 1The rough dimensions given by Trickett (1900) tally very well with these measurements whereas those on the face of the relevant map in Carne and Jones (1919) depart substantially from them. is a large recess some 60 feet deep and 80 feet high. The maximum and minimum diameters at the base are 240 and 120 feet respectively. Parts of the walls appear from weathering stains on the surfaces to be in a fairly stable condition ; this is notably so on part of the south-western wall where the safest descents can be made. From fresh rock surfaces and opened joints, other parts of the walls appear to be undergoing active rockfall and along about 20 feet of the north-eastern wall, fissuring a few feet back from the lip indicates that a large mass will break away before long. How- ever, a number of eucalypts up to 18 inches in diameter are growing so closely to the walls at various points round the perimeter as to bear witness to stability since they began to grow. The floor consists entirely of a rubble pile some 80 feet high, with a more gently sloping upper part at angles of 20-25° and a longer steeper slope at about 35° beneath the south- western overhang. The total depth of rubble is unknown. The blocks are larger towards the sides were they reach to four feet in length. In the south-west, boulders are jammed against the wall to form a small cave about 20 feet long. At the lowest part of this south-western corner there is standing water, which on 14 May, 1961, was up to six feet deep, and fine silt on the rocks around indicated it had recently been as much as five feet deeper. The rubble pile is elongated more or less parallel to the longer axis of the hole but eccentrically disposed away from the higher southern walls. A cover of tree ferns about six feet high of the top of the pile confirms the inference that there has not been a major fall from the walls for many years. 216 J. N. JENNINGS FoF FAULT —— MARGIN AT SURFACE — — MARGIN AT BASE —— SURFACE CONTOURS —-— CONTOURS OF RUBBLE PILE +100 - A FAULT PLANE anaieonneee de VISIBLE IN te 8s FAR WALL LADDER PITCH 288FT FROM FOOT OF TREE Ls = e: RUBBLE PILE WITH COARSER BLOCKS TO f FLANKS FAULT 6%9:° ““WATER AMONG ROCKS - 300 “=; DEVONIAN SANDSTONE SURFACE AND UNDERGROUND SURVEY *35¢ DEVONIAN CONGLOMERATE CANBERRA SPELEOLOGICAL SOCIETY KM | Fre, Plan and cross-sections of The Big Hole near Braidwood, New South Wales. Note that the cross-sections are at a smaller scale than the plan. The datum for heights 1s arbitrary. THE BIG HOLE NEAR BRAIDWOOD, NEW SOUTH WALES Geological Features The surrounding hill and the Big Hole from top to bottom consist entirely of Devonian rocks; most of the walls are quartzitic sand- stone, mainly very thick-bedded, but the lowest part of the south-western wall is conglomeratic. The attitude of the beds seems to be nearly horizontal in general but there is a gentle roll over the hole, to be seen most clearly in the south-eastern wall. Two nearly vertical faults, throwing a few feet only, occur in the hole, one in the backwall of the north- eastern overhang and the other coinciding with part of the south-western wall and clearly visible in the full height of the north-western wall. Narrow brecciated zones up to four feet thick mark the faults and major joints are parallel of them. Discussion Though the data given above do not prove, they give support to the contention that the Big Hole is a feature of subjacent? karst development (“‘wnterirdische Karstphinomen’’ of Penck, 1924); solutional removal of a more soluble rock below has caused a_ surface depression through subsidence of overlying insoluble? rock. Other hypotheses fit the known facts less well or require less probable postulates about the underlying geological structure. Volcanic explosions and meteoritic impacts produce craters of bowl-like form quite unlike the cavity in question. Also its compact horizontal combined with pronounced vertical develop- ment is out of keeping with a tectonic origin ; if faulting produces a surface cavity, it is of fissure type and there are usually associated surface manifestations of faulting not found here. Subsidence depressions can be caused by oxidation of sulphide ore bodies (Wisser, 1927) and the forms produced are more akin to the features under discussion. However, the regional geology offers no support for postulating such bodies. Features broadly similar to the Big Hole are known to be due to various subjacent karst rocks—gypsum and highly soluble evaporites such as rocksalt and potash as well as the more widespread carbonate rocks, dolomite and lime- 2 “Subjacent’’ (cf. Martin, 1965) is used in preference to “‘covered‘’ since the latter term is more closely associated with thin covers of superficial deposits and/or soils. The cover rocks are, of course, not completely “insoluble” but this slight lack of precision is thought preferable to the use of such terms as ‘‘non-karst’”’ or ‘“‘unkarstifiable’’. 217 stone. However, evaporites are not known from the Palaeozoic rocks of the area and the nearest dolomites are in the Buchan area of Eastern Victoria. Although no limestone is found in the Big Hole, the occurrence of Silurian limestone unconformably beneath basal Devonian conglomerate at Wyanbene five miles south-south-east and recurring at Marble Arch and Cheitmore in the same line of strike passing two miles east of the Big Hole points to lime- stone being the karst rock responsible for the latter. Carne and Jones (1919) had no hesitation in assuming this to be the case, even though it does leave some geomorphological difficulties which will be discussed below. The structural difficulty that a second strike belt of limestone, additional to the one which outcrops on a line to the east, must be involved in the formation of the Big Hole makes little demand in this context of closely folded lower Palaeozoic rocks ; Silurian limestones in parallel strike belts only a few miles apart are known elsewhere in the Southern Tablelands. As a subjacent karst doline, the Big Hole is far from rare. Nevertheless on the basis of some of the more readily available relevant literature (Bennett, 1908; Cramer, 1941; Fisher, 1859; Hare, 1947; Laurence, 1937 ; Lee, 1926; Stockdale, 1936; Thomas, 1959, 1963), it is an exceptional case in its combination of considerable absolute size with pronounced vertical development. The depth/width ratio is 2: 1 on the basis of the maximum surface diameter and 3:5: 1 on the minimum. The examples discussed by Fisher (1859) and Hare (1947) are shallow (40-60 feet deep) and basin- or funnel-shaped rather than _pit-like, with D/W ratios between 1: 18 and 1: 3:°5. Both authors deal with areas where thin Tertiary beds overlie Cretaceous Chalk in south-east England. However, the thinness of overlying rocks cannot be expected to limit depth in relation to width because there is no structural reason why the surface depression in the insoluble rocks should not be continued downwards into the underlying karst rock. Moreover recent discussions by Thomas (1959, 1963) of solution subsidence phenomena in Carmarthenshire and Breconshire in Wales suggest that thickness of cover rocks has little control of doline shape. Here dolines tend to be larger and steeper in the overlying Millstone Grit than in the exposed parts of the under- lying Carboniferous Limestone. But depths remain rather small—up to 60 feet and D/W ratios low, even though the Grit reaches thicknesses of 450-550 feet. The dolines do 218 not change in character as the Grit gets thicker. One figure (Thomas, 1959) shows a very steep- sided doline 75 feet across and 45 feet deep, giving a D/W ratio of 1: 1-7 however. Greater thicknesses still of covering rocks are recorded from the Cumberland Plateau in Tennessee in U.S.A. where up to 800 feet of sandstone and shale overlie thick Mississippian limestone (Laurence, 1937, ,>tockdale, 1936): hie largest doline described here is elliptical in shape, 390 by 250 feet, with a probable depth of 230 feet (Stockdale, 1936). These dimensions give ratios of 1: 1:6 and1: 1-1, approaching more closely to the Big Hole values. The vertical rock walls and talus slopes up to 130 feet high of this doline surround a deep lake, Montlake. The presence of this lake suggests that depth to water rest levels is not a critical factor governing the shape of dolines any more than the thickness of the cover rocks. Of all the authors consulted, Cramer (1941) alone records subsidence dolines with D/W ratios exceeding those of the Big Hole. A shatt near Gotha in central Germany opened up suddenly in the Muschelkalk to become 3-4 m. diameter and more than 37m. deep (D/W> 12-3: 1) andasimilar subsidence near Zimmern in Thuringia produced a shaft 3-4 m. wide and 38-40 m. deep (D/W 13:3: 1). However, not only are these examples smaller than the Big Hole, they are also not fully comparable on other grounds. The measurements were made at the time of subsidence when long-term stability had not been achieved. Thus the Zimmern example four years later on is described as remaining shaft-like below but having become a steep funnel shape above. Also older subsi- dences near Gotha were much wider with 1: 2 to 1: 3 ratios. Moreover, these occurrences were due to solution of the salt and gypsum beds of the Zechstein series and different effects can be expected from these more soluble rocks. The Big Hole therefore appears to be an extreme case in its form. A structural cause seems possible because in all the examples cited above the limestones as well as the cover rocks were not far from horizontally disposed, whereas in the case of the Big Hole it is reasonable to infer from the regional geology that the lime- stone involved would be steeply dipping or vertical in attitude and so of great depth but in a strike belt of little width. In the former cases subterranean solution would not be con- fined laterally and might tend to remove extensive but shallow bodies of limestone, inducing basin-like depressions. In the latter case solution might be concentrated in horizontal J. N. JENNINGS dimensions but able to work in great depth. | Sharply confined but deeper subsidence could be the consequence. The presence of the two faults in the Devonian rocks above, crossing the probable line of strike of the limestone at an angle, might localise and facilitate the subsidence. In his general review of dolines, Cramer (1941) discusses those involving the subsidence of overlying insoluble rocks in two categories, respectively named Frdfdlle (sink holes) and Schwunddolinen (swallow holes) or Nachsackungs- dolinen (subsidence dolines). The first category is attributed to sudden collapse into a cave in the underlying karst rock and resemblance to collapse dolines (Einsturzdolinen) in outcropping karst rocks is close. In thick resistant cover rocks, deep pits may be produced by subsidence into large caves and these may retain steep walls for decades, until weathering eventually produces first a funnel and then a basin shape. The second category is described as due to gradual subsidence or to cumulative effects of subsidence at intervals through progressive subcutaneous solution. The solution in this category is thought to take place at the top of the karst rock, inducing more or less con- tinuous stoping of the cover rock but without the development of large cavities. The resemblance therefore is to the solution dolines (Lésungsdolinen) of outcropping karst rocks. Greater opportunities for weathering should result in the second category becoming more regularly shaped dolines with less steep sides earlier in their history than in the first category. Moreover their sides may become composite in nature, reflecting several phases of develop- ment rather than one catastrophic event more or less instantaneous in a geological time scale. The angularity of plan of the Big Hole, together with its great D/W ratio and uniformly steep walls from top to bottom, constitutes a strong case for placing it in the first category. This ascription must be recognised as demanding the formation of a very large chamber in the limestone, much larger than any known in the neighbouring exposed karsts. Major subsidence would not, however, produce the smooth shape and size sorting of the debris pile in the Big Hole. This must be due to subsequent small-scale accretion from the walls of the pit. Bouncing of fragments from the walls in the long descent would account for the absence of a raised rim around the debris pile at the foot of the walls such as is often found in shallower dolines, and also for the fact that the top of the pile is displaced away from the THE BIG HOLE NEAR BRAIDWOOD, NEW SOUTH WALES higher southern walls, which can be expected to have supplied the greater volumes of material. The flatter top of the pile with slopes lower than the angle of rest for talus is probably due to the scatter resulting from ricochet. From the presence of standing water at the bottom, the limestone solution regarded as causing the doline must have taken place below the present groundwater level. Further- more it is difficult to envisage how past water levels can have been significantly lower than at present, even though the vicinity of the Big Hole has not been affected by the coastal slope rejuvenation, which is now lowering water levels in the limestone at Marble Arch and Cheitmore not far to the east. The valleys around the Big Hole ridge drain to the upland plain of the Shoalhaven, part of the Newer Peneplain of Tertiary age of Craft (1932). There is no great aggradation in this plain near the Big Hole to allow of former lower groundwater levels. The hidden limestone mass beneath the ridge is likely to have been small, below the level of nearby surface drainage and barred round by impervious rocks. In these circumstances the solution below the Big Hole must have been phreatic in nature and true phreatic rather than epiphreatic or shallow phreatic. The volume of the Big Hole is of the order of 3,200,000 cubic feet but as the loss of sand- stone from the system seems unlikely in view of the previous discussion, the volume of limestone removed in solution to accommodate the shattered subsided rock with its voids must have been significantly larger by a margin which is difficult to estimate. The recent tendency in _ speleological theory, both in Europe and North America, has _ trended against attributing large caves to deep phreatic solution. Bretz’s interpretation of Carlsbad Cavern with its exceptionally large Big Room as of deep phreatic origin has not been contro- verted yet, however, even though the occurrence of several horizontally developed levels in that system appear to be a difficulty for it. The amount of deep phreatic solution demanded by the interpretation of the Big Holes’ origin supported here remains a difficulty for this view. Even if we accept a single catastrophic subsidence as the mode of origin of the Big Hole, it is still difficult to ascribe an age to it. Historical knowledge of it and the inferences from the vegetation around and within the hole mean that it is at least a century old. Beyond that, its freshness of form implies 219 great youth geologically but datings of analogous dolines are not available to translate this freshness into so many centuries or millennia. The fact that part of limestone shafts such as Padirac in France can be regarded as surviving from the Lower Tertiary (Cavaille, 1963) is a warning against uncontrolled speculation in this matter. Acknowledgements This note could not have been written without the help of various members of the Canberra Speleological Society in gathering the data on which it is based. In particular I am very much indebted to Dr. R. W. Galloway, not only for free use of the observations he made on the 1961 descent, but also for critical comments from which the manuscript has benefited much. Responsibility for the inferences from the data is mine, however. References BENNETT, F. J., 1908. Solution-subsidence valleys and swallow-holes within the Hythe Beds area of West Malling and Maidstone. Geogrl. Jf. 32: 277-288. Bretz, J. H., 1949. Carlsbad Caverns and other caves of the Guadalupe block, New Mexico. J. Geol., 57: 447-463. CARNE, J. E., AND JONES, L. J., 1919. deposits of New South Wales. Surv. New South Wales, 25. CavAILLE, A., 1963. L’age des grottes du Quercy. Third Int. Cong. Speleology, 2 (1): 153-166. CraFt, F. A., 1932. The physiography of the Shoal- haven River Valley. VI. Conclusions. Pvroc. Linn. Soc. New South Wales, 57: 245-260. CRAMER, H., 1941. Die Systematik der Karstdolinen. N. Jahrb. Min. Geol. Pal., B 85: 293-382. FISHER, O., 1859. On some natural pits on the heaths of Dorsetshire. Quart. J. Geol. Soc., 15: 187-8. Hare, F. K., 1947. The geomorphology of a part of the middle Thames. Pyoc. Geol. Ass; 38: 294-339. LAURENCE, R. A., 1937. Sinkholes of the Cumberland Plateau. J. Geol., 45: 214-215. LEE, W. T., 1925. Erosion by solution and fill. U.S. Geol. Surv. Bull., 760 C: 107-122. The limestone Min. Res. Geol. Martin, J., 1965. Quelques types de dépressions karstiques du Moyen Atlas central. Rev. Géogr. Maroc., 7: 95-106. Penck, A., 1924. Das unterirdische Karstphanomen. In Zbornik Radova Posvecen Jovanu Cuvijicu, ed. P. Vujevic, Belgrade, p. 175-197. STOCKDALE, P. B., 1936. Montlake—an amazing sinkhole. J. Geol., 44: 515-522. Tuomas, T. M., 1959. The geomorphology of Breck- nock. Brycheiniog., 5: 129-136. Tuomas, T. M., 1963. Solution subsidence in south- east Carmarthenshire and south-west Breconshire. Trans. Inst. Brit. Geographers, 33: 45-60. TRICKETT, O., 1900. In Annual Report of Department of Mines for 1899. Sydney. WIssER, E., 1927. Oxidation subsidence at Bisbee, Arizona. Econ. Geol., 22: 761-790. ‘NM ie 6 ne Journal and Proceedings, Royal Society of New South Wales, Vol. 98, pp. 221-237, 1966 Petrography of Some Permian Sediments from the Lower Hunter Valley of New South Wales J. D. HAMILTON Division of Building Research, Commonwealth Scientific and Industrial Research Organization, Melbourne, Australia ABSTRACT—The non-coal detrital sediments of the Tomago and Newcastle Coal Measures in the Lower Hunter Valley comprise a homogeneous lithological suite ranging from fine-grained rudite to claystone. Lacustrine conglomerates and fluvial sandstones are moderately well-sorted lithic (volcomictic) types, with recrystallized mixed-layer mica-montmorillonite/kaolinite matrix- cements. For the rudite-siltstone range, the ratio rock fragments: quartz/feldspar appears to be a direct function of average grainsize. Reworked deltaic arenites (e.g. Waratah Sandstones) have comparable compositions, but are typically better-sorted and more compact than their fluvial counterparts. The marine Ravensfield and Cessnock Sandstones and their siltstone variants are well-sorted, compact rocks, which contain less lithic detritus and correspondingly more quartz and feldspar than the coal measures arenites. Textural characteristics suggest a possible genetic link between the massive clayey siltstones and interlaminated siltstone/claystone lithologies of the deltaic environments. Montmorillonite and kaolinite are the chief constituents of the marine claystones studied. Clay rocks of the Tomago and Newcastle Coal Measures may have similar clay mineralogies, but more commonly contain mixed-layer mica-montmorillonites in heu of montmorillonite. eisai glacial and volcanic debris occur in some claystones. Bentonites from the Tomago and Newcastle Coal Measures are highly montmorillonitic. Variable particle-size and plasticity characteristics of these materials reflect differences in the physical properties of the clay mineral constituents. Introduction Earlier studies on the geology of the Permian System of the Hunter River Valley, New South Wales (David, 1907; Raggatt, 1938; Jones, 1939) in general have included little detailed petrological and mineralogical information per- taining to the non-coal sediments. Booker, Bursill and McElroy (1953) have described the petrographic properties of the rocks outcropping in the Singleton-Muswellbrook region, and in a later work Booker (1960) has provided minera- logical data for some Permian bentonite deposits of the Newcastle area. A wider mineralogical survey of the Permian economic clay deposits of the Hunter Valley has been made by Loughnan (1960). Specific aspects of clay mineralogy have also been covered in subsequent papers (Loughnan and See, 1959; Loughnan and Craig, 1960). The heavy mineral suites of the coarser clastic lithologies of the Hunter Valley succession have been studied in detail by Culey (1938) and Carrol (1940). The work reported herein represents part of a comprehensive lithological study recently carried out by the author on sediments from the Lower Hunter Permian type succession. Materials from the Tomago and Newcastle Coal Measures have been examined in detail and are here compared with some typical lithologies of the associated marine groups. Geological Setting and Stratigraphy Outcrops of Permian sediments along the northern margin of the Sydney Basin are confined to the floors of the Hunter and Goulburn River Valleys (Fig. 1). To the south the gently dipping succession is overlain conformably by sediments of the Triassic Narrabeen Group, and to the north is separated from the deformed Palaeozoic “ Central Complex ”’ region (Voisey, 1959) by the Hunter-Mooki Thrust System (Osborne, 1950). The Permian depositional environments of the Lower Hunter have been described by Booker (1960) as “marginal geosynclinal lacustrine and barred estuarine ’’, representing accumulations under glacial, effusive and ex- plosive volcanic, as well as normal fluvial/ deltaic and paludal swamp conditions. In the Maitland-Cessnock-Newcastle region a type stratigraphic section, 14,000 feet in thickness, is exposed in and adjacent to the deeply eroded Lochinvar Anticline (Fig. 2). A recent reclassification of the succession by 229 J. D. HAMILTON SS \) Cie Vi GA We SYONEY BASIN —— eWILLIAMTOWN = ——~ ~ o_ LEGEND TERTIARY TO RECENT (44) TRIASSIC PERMIAN (UNDIFFERENTIATED ) [TI] NEWCASTLE COAL MEASURES = TOMAGO COAL MEASURES [5] MAITLAND GROUP PERMIAN (SHOWING MUREE HORIZON) MMA GRETA COAL MEASURES REI DALWOOD GROUP F XN eo FAULT Nee FAULT XK pruna AXIS S99) PRE= PERMIAN PTGsyed Geological map of the Lower Hunter River Valley region (after Jones, 1939). Legend from Booker (1960). PETROGRAPHY OF SOME PERMIAN SEDIMENTS Booker (1960) defines five stratigraphic groups, representing two major alternations of marine and freshwater deposition (Table 1). Dis- crimination between the Tomago and Newcastle units is based primarily upon distributional and lithological contrasts. (a) Dalwood Group Six thousand feet of Dalwood Group sediments are exposed in the core of the Lochinvar Anti- cline. The lower formations contain abundant andesitic tuffs and basalt flows, locally associated with tuffaceous arenites, claystones and boulder beds containing occasional horizons of glacial erratics. The upper formations contain finer, and better-sorted quartzose sediments (e.g. Ravensfield Sandstone), and are generally poorer in volcanic materials. (b) Greta Coal Measures The succeeding Greta Coal Measures consist of a succession of coals, rudites and arenites, (Clay < 1/256 m.m.) Sand Sit ()Yig mm) (« Yig > Y256 mm) 223 100-300 feet in thickness. in the sequence: Claystones are rare (c) Maitland Group The lower units of the marine Maitland Group are generally conformable with the underlying Greta succession. However, trans- gressional overlaps between the upper and lower Maitland beds, on the flanks of the Lochinvar Anticline, clearly mark the inception of Permian folding in the region. Booker (1960) has divided the Maitland sequence into two major subunits—the Branxton Subgroup (lower) and Mulbring Subgroup (upper). Four lith- ological subdivisions of the Branxton Subgroup are defined—viz. the basal Elderslie Formation (1,500 feet) comprising a sequence of pre- dominantly arenaceous and conglomeratic rocks, associated with fossiliferous sandy lutites, con- taining glacial erratics; the succeeding Fenestella Shale (20-100 feet), constitutes a marker in the Lower useful stratigraphic pe (b) nN (d) (fF) iG 2 Lithological classification of the Lower Hunter Permian sediments. (a) Lithological classification (modified after Trefethan, 1950) 1—Claystone ; la—Sandy claystone ; silty claystone. 2—Sandstone ; 2a—Silty sandstone ; clayey sandstone. 3—Siltstone ; 3a—Clayey siltstone ; sandy siltstone. @ Dalwood Group. A Maitland Group. Tomago Coal Measures, pure lithologies. Newcastle Coal Measures, pure lithologies. 16b—Silty sandy claystone; Ic—Silty claystone; l1d—Sandy 2b—Clayey silty sandstone; 2c—Clayey sandstone ; 2d—Silty 3b—Sandy clayey siltstone; 38c—Sandy siltstone; 3d—Clayey (0) (c) . (d) Tomago Coal Measures, interlaminated lithologies. (e) (f ) Newcastle Coal Measures, interlaminated lithologies. J. D. HAMILTON TABLE 1 Permian Stratigraphic Succession of the Lower Hunter Valley 224 System Group Subgroup TRIASSIC Narrabeen Clifton Subgroup 1,300” Moon Island Beach ea: (250’) Boolaroo Subgroup (800—600’) Newcastle? : Coal Measures ow Subgroup (500’) Lambton Subgroup (200-300’) PERMIAN} Tomago® Coal Measures < (1,200’) Mulbring Subgroup Maitland4 (1,500-3,000’) Group (4,500-6,000’) Branxton Subgroup Greta Coal4 Measures (100-3007) Dalwood4# Group (6,000’) 1 Major stratigraphic classification after Booker (1960). 2 Subdivided by Hanlon, e¢ ali (1953). Formation Munmorah Formation® (500’) with Wallarah Tuff Member Wallarah Seam Catherine Hill Bay Formation Great Northern Seam Eleebana Formation Fassifern Seam Croudace Bay Formation Upper Pilot Seam a Mistake Formation Lower Pilot Seam brite ee Bay Formation Hartley Hill Seam Mount Hutton Formation Australasian Seam Tickhole Formation Montrose Seam ahibah Formation Wave Hill Seam Fern Valley Seam otara Formation Victoria Tunnel Seam Shepherd’s Hill Formation Nobby’s Seam Bar Beach Formation Dudley Seam Bogey Hole Formation Yard Seam Tighe’s Hill Formation Borehole Seam Waratah Sandstone (100’) ( Hexham Formation | (with Sandgate Seams) j Four Mile Creek Formation 1x | Highfields Formation ie (with Buttai Seams, Donaldson’s Seam, Big Ben Seam Tomago Thin Seam) Wallis Creek Formation (with Scotch Derry Seam, Rathluba Seams, Morpeth Seam) ( Muree Formation Belford Formation 4 Fenestella Shale | Elderslie Formation Rutherford Formation Allandale Formation | Lochinvar Formation | Farley Formation 3 Subdivided by R. A. Britten (N.S.W. Joint Coal Board) and P. J. Mackenzie (The Broken Hill Pty. Co. Ltd.). 4 Subdivided by Booker (1960). 5 Subdivided by J. B. Robinson (N.S.W. Joint Coal Board). PETROGRAPHY OF SOME PERMIAN SEDIMENTS Hunter Region; the Belford Formation (1,500 feet), which is less arenaceous than the Elderslie unit, but otherwise similar in lithology; and the Muree Formation, a thin, but persistent horizon of glacial materials, ranging from tillites to clay-shales. The Mulbring Subgroup is represented by 1,500-3,000 feet of mainly soft argillaceous sediments which, in the lower levels, contain sparse glacial erratics. (2d) Tomago Coal Measures Contemporary tectonic activity greatly influenced the sedimentation patterns of the Tomago Group in the Lower Hunter region. Maintenance of shallow-water deltaic conditions along the eastern flank of the rising Lochinvar structure is reflected in the accumulation of 800-1,200 feet of coals and _ thinly-bedded silt/clay sediments, containing arenaceous channel deposits. Contemporary deeper water environments to the east of the Maitland WEIGHT (%) WEIGHT (%) 225 Coalfield (the Dempsey Beds of David, 1907), are represented by a thick (2,000 feet+) succession of carbonaceous sediments containing little coal. A recent subclassification of the Group by J. B. Robinson (private communi- cation) defines three formations. The _ basal Wallis Creek Formation is characterized by the predominance of silt/clay lithologies over sand- stones. The succeeding Four Mile Creek Formation is distinctly more arenaceous, but like the Wallis Creek unit, contains a number of important coal horizons. The Hexham Formation consists mainly of argillaceous and silty sediments and, except for the two thin Sandgate Seams near the top, lacks coal deposits of economic significance. (e) Newcastle Coal Measures The Newcastle Coal Measures outcropping in the Newcastle-Lake Macquarie region comprise 1,500 feet or more of thick lacustrine conglo- Ga Sue Fic. 3 Cumulative curves and frequency histograms for the particle-size distributions of some Permian arenites. c) d) Lithic arenite, 2nd (d) should be (f) a) Quartzose arenite, Maitland Group, Cessnock, N.S.W. b) Lithic arenite, Tomago Coal Measures, Thornton, N.S.W. Lithic arenite, Tomago Coal Measures, Thornton, N.S.W. Newcastle Coal Measures, Wallsend, N.S.W. e) Lithic arenite, Newcastle Coal Measures, Waratah, NESW. f) Lithic arenite, Newcastle Coal Measures, Waratah, N.S.W. 226 J. D. HAMILTON WEIGHT (%) WEIGHT (%) Fic. 4 Cumulative curves and frequency histograms for the particle-size distributions of some Permian silt rocks. (a) Silt-shale, Newcastle Coal Measures, Waratah, N.S.W. b) Clayey siltstone, Tomago Coal Measures, E. Maitland, N.S.W. c) Clayey silt-shale, Newcastle Coal Measures, Warner’s Bay, N.S.W. e) Interlaminated clayey, sandy siltstone/silty clay-shale, Tomago Coal Measures, Thornton, N.S.W. f) Interlaminated clayey siltstone/silty clay-shale, Newcastle Coal Measures, Wallsend, N.S.W. ( ( (d) Interlaminated sandy, clayey siltstone/silty clay-shale, Tomago Coal Measures, E. Maitland, N.S.W. ( ( merates and arenites, interbedded with minor deposits of finer silty and argillaceous sediments, and associated with abundant coal seams and tuff accumulations. R. A. Britten (New South Wales Joint Coal Board) and P. J. Mackenzie (The Broken Hill Pty. Co. Ltd.) have suggested a stratigraphic subdivision of the Group, based on “coal seam’’ and composite “ inter-seam ”’ formations (Table 1) to accommodate the inherent complexities of the succession (J. B. Robinson, New South Wales Joint Coal Board, private comm.). Four major Subgroups are defined above the distinctive basal Waratah Sandstone unit—viz. Lambton (bottom), Cardiff, Boolaroo and Moon Island Beach (top). The non-coal lithologies of the Lambton Subgroup are mainly arenaceous and argillaceous. Conglo- merates are of minor importance. Tuffs are not common but may form useful stratigraphic marker units (e.g. Nobby’s Tuff Member). The Cardiff Subgroup is characterized by abundant developments of thick lenticular fanglomerates interbedded with sequences of delta arenite. Tuff deposits are common, but are usually found in the coal seam sections. The Boolaroo Subgroup represents a period of poor; coal development. The thin Hartley Hill and Pilot Seams are interbedded with abundant vitric tuff and clayey arenites. Thick conglomerates are developed locally. The Moon Island Beach Subgroup is lithologically similar to the Cardiff unit, massive conglomerates, tuffs and coals constituting a high proportion of the sequence. The rudite units are generally lenticular and restricted in lateral extent, but some of the thicker deposits (e.g. Teralba Conglomerate Member) may be persistent. Procedures in Examination of Materials Some 130 samples, representing full ranges of Tomago and Newcastle Coal Measures lithologies PETROGRAPHY OF SOME PERMIAN SEDIMENTS WEIGHT (%) WEIGHT (%) 227 Fic. 5 Cumulative curves and frequency histograms for the particle-size distributions of some Permian claystones and tuffs. (a) Silty clay-shale, Newcastle Coal Measures, Warner’s Bay, N.S.W. and a more limited selection of Maitland and Dalwood Group materials, have been examined. Basic textural and mineralogical data have been derived from studies of hand specimens and thin sections supplemented by complete grainsize distribution analyses of all samples and detailed X-ray, differential thermal analysis, chemical, cation exchange, and electron microscopic investigations of their clay-size matrix fractions. Estimates of mineralogical modes for repre- sentative sandstone and siltstone types have been made on the basis of counts per 200 to 300 points, in linear microscope traverses across thin sections. Fifty to sixty gram samples were used for particle size analysis. The materials were easily disaggregated by soaking in dilute (0-1%) Calgon solution and gentle crushing. Dispersion was subsequently effected by stirring for about five minutes in a high-speed mixer. The resulting suspension was passed through a 200 mesh ) Silty claystone, Newcastle Coal Measures, Swansea, N.S.W. c) Silty claystone, Maitland Group, Kurri-Kurri, N.S.W. d) Sandy, silty claystone, Dalwood Group, Cessnock, N.S.W. e) Altered vitric-tuff, Newcastle Coal Measures, Swansea, N.S.W. f) Altered vitric tuff, Newcastle Coal Measures, Swansea, N.S.W. (B.S.S.) steve, collected in a one litre measuring cylinder and set aside for more detailed analysis. Material retained on the sieve was dried, weighed and passed through a sieve stack containing units of 2 mm., 1 mm., 0:5 mm., 0:25 mm. and 0-125 mm. opening size to ascertain the weight percentages (on an oven dry basis) of the Wentworth “very coarse sand’’, “‘ coarse sand’”’, “‘medium sand” and “fine sand” grades respectively (Wentworth, 1922). From the residual suspension containing the minus 200 mesh material, two points (at about 20 microns and four microns) on the particle size distribution curve were determined using the hydrometer method of Day (1950). Finally, the percentage of particles finer than 0-5 micron was estimated on the basis of pipette samples taken from the suspension during settling under controlled conditions. For purposes of discussion, the — size distribution data are presented as cumulative 228 percentage curve and frequency histograms (Figs 3-5). The system of lithological nomen- clature adopted is based on the Wentworth definitions for sand (>1/16mm.), silt (<1/16 >1/256 mm.) and clay (<1/256mm.). The scheme is essentially similar to that of Trefethan (1950), but, in providing for a more detailed subdivision of the transition categories, has the added advantage of emphasizing the relative importances of the subdominant size grades. Separate plots of data for “ uniform’ and “interlaminated ”’ types of Tomago and New- castle sediments (Fig. 2 (c)-(f)) are made to facilitate textural comparisons. Ihe cumulative curves and frequency polygons of Figures 2—4 illustrate graphically some important features of the various textures. Minus 2 micron fractions required for clay mineral analysis were obtained by settling and siphon extraction methods from the above- mentioned suspension of minus 200 mesh material. A Philips PW1010 X-ray generator and wide-range goniometer were used in the X-ray diffraction analysis of these fractions. Glass-mounted flake aggregates were used to study the basal diffraction characteristics of the layer-silicate components under air-dried, glyco- lated and heat-treated conditions. The general diffraction patterns were obtained from random- ageregate specimens, packed in aluminium goniometer cells. Differential thermal curves for the minus two micron fractions were derived using apparatus developed by Carthew and Cole (1953). The micro method described by Mackenzie (1951) was utilized for the deter- mination of cation exchange capacities of both whole sample and clay fraction materials. Morphological studies of the submicroscopic constituents of the matrix fractions were carried out using Siemens electron microscope units. Shadowing techniques were used in most specimen preparations. (a) Petrography (i) Rudites Rudites of the Newcastle Group conform essentially to a single lithological type, viz a fine to medium-grained lithic material, occurring as thick discontinuous lensoid masses, inter- bedded with other coarsely arenaceous units. Rock structure is typically anisotropic, bedding being clearly defined by sequential variations in grain size, and interbedding of fluvial sand lenses. The Merewether Conglomerate Member (Kotara Formation) which is well exposed in J. D. HAMILTON the gravel quarries at Merewether, three miles south from Newcastle, has been examined in detail. The rock is textually heterogeneous. Bands containing pebbles up to 100mm. in diameter are abundantly developed through the main aggregate of 10mm. average grain- size. Most of the constituent fragments are moderately well-rounded. Voids created by the open contact packing of the coarse detritus are filled with sand-size material, and the whole is bonded by a relatively pure cement of secondary clay mineral. The rock is heavily stained by iron oxide throughout the exposed pit section. Volcanic rock fragments constitute 90° or more of the pebble suites. The majority are fine-grained or divitrified glassy acid types (dacites, rhyolites), which have been tentatively identified, using staining techniques (Bailey and Stevens, 1960). Some types are transected by numerous thin veins of quartz associated with minor chalcedony, white mica and, less frequently, chlorite. Small spherulites and larger irregular segregations of silica minerals may be associated with the veins. Chalcedonic spherules exhibit typical radiating fibrous textures ; the quartz patches form inter-locking granular mosaics. Many of the quartz-aggregate grains appear to be derivatives of these quart- zose volcanic rocks; others may be derived from granitic and metamorphic sources. Pheno- crysts of embayed quartz and prismatic feldspar are not commonly observed, but pyroclastic shards and crystal fragments may be abundant in some rock types. Andesitic and basaltic varieties are rare in the pebble suites. The inter-pebble sand-size constituents are also predominantly lithic. Accessory types include subrounded quartz, angular plagioclase feldspar and rare flakes of leached muscovite. Detrital clays appear to be absent from the matrix. In most cases, the interstices are filled with mosaic aggregates of pure, finely vermi- cular kaolinite. The texture is typically authigenic, but there is no evidence (eg, replacements of pebble and sand fragments) to confirm such an origin. Patchy developments of montmorillonite in some samples are probably related to a phase of epigenetic mineralization, which has produced changes in and adjacent to principal joint sets, traversing the rock unit. The montmorillonite occurs in the conglomerate as irregular colloform masses and veins of fine, ragged flakes, penetrating along grain margins and producing random replacements of both detrital and primary cementitious constituents. PETROGRAPHY OF SOME PERMIAN SEDIMENTS (ii) Aventtes Argillaceous arenites are widely distributed both laterally and vertically throughout the Lower Hunter Permian succession. Three principal types are recognized—viz. fine-grained quartz-feldspar sandstones forming laterally persistent sequences in the Dalwood and Maitland Groups; soft argillaceous lithic arenites constituting the abundant fluvial deposits of the Tomago and Newcastle Coal Measures ; and the tough even-grained lithic sandstones of the Newcastle Group, typified by the Waratah Sandstone. The quartz-feldspar sandstones, constituting the basal units of the Farley Formation (Dalwood Group) and Elderslie Formation (Maitland Group) in the Maitland-Cessnock region, are light grey to buff-coloured, fine-grained, massive, compact rocks containing sparsely disseminated coarse sand grains and granules up to 3mm. in diameter. The latter (Cessnock Sandstone) consists of closely packed, angular to subrounded fragments of quartz (up to 60%), with associated minor amounts of feldspar rock detritus, sand-size mica flakes, and carbonized plant debris, embedded in a matrix of fine white clay mica (PI. 1(a)). Modal analysis (Table 2, spec. 133) indicates that the rock fragment and feldspar accessories are represented in approximately equal abundance. Grain shape varies from equant to elongate —sphericities as low as 0:45 on the Rittenhouse scale (Rittenhouse, 1943) have been recorded. The outlines of quartz grains are frequently modified through pressure solution and repre- cipitation processes. Sutural contacts so 229 developed frequently entrap matrix clay materials. Indications of original grain outlines are rare. Thus, it is usually difficult to assess the extent of the silica outgrowths. The quartz grains contain only limited quantities of mineral inclusions (especially zircon, muscovite and tourmaline), but fluid inclusions forming fine trails, or occasional larger individual blebs, may be abundant. Sand-size feldspar components include moderately well-rounded, turbid grains, and fresh, multiply-twinned, prismatic cleavage fragments of sodic plagioclase (albite-oligoclase). Potassic types are represented by rare abraded grains of microcline, showing characteristic “ erid”’ twinning. The rock fragment suites contain predominant massive and banded, glassy or fine-grained acid volcanic varieties. Chloritized basic rocks and quartz-mica sedimentary materials are present in minor proportions. The constituent biotite flakes are invariably leached and oxidized and may be partially replaced by fine-grained secondary hydrous micas. Muscovites, too, are usually leached and altered to aggregates of wispy clay. Exten- sive compactional distortion of the origina, flakes may be evident in thin section. In some instances, larger flakes may be completely macerated by crushing between adjacent grains Of ‘quartz, etc. Illitic mica and partially ordered 70: 30 to 60: 40 mixed-layer mica-montmorillonite pre- dominate over kaolinite in the matrix suites of the quartzose arenites (Table 2). Quartz is a consistent though minor accessory constituent. TABLE 2 Modal Analyses for Typical Arenite and Coarse Siltstone Lithologies from the Permian of the Lower Hunter River Valley Matrix Composition in parts per tent : n fe) 455 s E - a: 5 z S S e. F E a 2 Whee a 04 (| oe , 5 mc = w S = O oOo Vat O77 aa! 17-0 8-1] 2-5 2-0 0-0 7S 7 3°5 0°5 4-5 0:5 1-5 Abie. 099 45-9 17-1 Tig 0-0 6-0 0:0 23-8 33 0:5 4 slates oy 0:5 056 56:1 9-7 7:0 0-7 22, 0:0 24-3 3 ] 4 = 1-5 ] 063 56:1 14-4 4-8 1-0 3:1 0-0 20-8 3 — 5:5 — 1-5 alr 186 64-9 9-8 3-1 1-7 7-1 0-0 13-4 3:5 l 3 ass 2-5 aire 133 11-1 59-4 13-2 1-7 O-7 0:0 14-0 2-5 0:5 4 == 3: — 1 Matrix composition estimated from X-ray, cation exchange and chemical data. 230 The average fluvial sandstone is a friable, fine- to medium-grained material, similar in texture and mineralogy to the argillaceous arenites from the Singleton Coal Measures, described by Booker, Bursill and McElroy (1953). The rock type consists essentially of subangular, to moderately well-rounded fragments of rock, quartz, feldspar and mica, embedded in a matrix/cement of fine-grained clay mica and vermicular kaolinite. Rock fragments pre- dominate in the clastic fractions and in the coarsest sediments may be present almost to the complete exclusion of quartz and feldspar. In the finer rock types the ratio rock fragments : quartz-+feldspar is of the order of 3 or 4: 1. Volcanic rock types predominate in the lithic suites of the fluvial arenites. Quartzophyric and feldsparophyric dacites, banded and spherulitic rhyolites and altered micaceous tuffs are generally represented, and are associated with minor quantities of granite, granophyre grey- wacke and quartz/feldspar/mica hornfels detritus. Many of the quartz detritals are evidently volcanic derivatives, having smooth, rounded and often deeply embayed outlines (Pl. 1(d)), similar in form to the quartz pheno- crysts of the lithic constituents. Other more angular, inclusion-riddled fragments, which commonly show evidence of mechanical strain, are comparable with the quartzes of the granitic fragments. Plagioclase feldspars predominate over potassic types (almost to the exclusion of the latter). Iwo general conditions of the plagioclase are recognized, viz. fresh, unabraded prismatic cleavage fragments, showing well-developed multiple twinning; and moderately rounded kaolinized and sericitized individuals. Coarse mica flakes are common minor constituents of the soft lithic sandstones, which do not exceed a maximum of about 5% con- centration. Marked decrease in double refraction and bloating of the crystallites in a direction perpendicular to the basal cleavage, indicates progressive degradation and hydration of the materials 1m situ (Pl. 1(c)). Ultimate breakdown of the wispy hydrous mica products to kaolinite is frequently evident (Pl, 1(@)). Tuffaceous variants of the lithic arenites occur in the upper levels of the Catherine Hill Bay Formation (Moon Island Beach Subgroup) and in the Triassic Wallarah Volcanic Member overlying the Wallarah Seam. These materials, which are associated with the vitric ash sequences, either as thin interbeds or as thicker adjacent units, typically contain abundant broken, angular, often wedge-shaped splinters JD. HAMTEM@N of quartz and feldspar, in association with moderately well-rounded lithic detritus, quartz, CLC: Kaolinite and _partially-ordered mixed-layer mica-montmorillonites varying widely in relative abundance (ratio 0-5 to 2) are the chief constituents of the matrix/cements of the soft lithic arenites. Quartz is a consistent though minor (<5%) accessory of the minus two micron fractions. Secondary carbonate replacements of the clay mineral and other chemically reactive consti- tuents (e.g. feldspar, glassy rock) occur sporadi- cally in the Tomago and Newcastle Group arenites. Booker, Bursill and McElroy (1953) have observed similar features in the Tomago sediments from Singleton-Muswellbrook region. Calcium and iron varieties may be associated in these replacements, which range in scale from small patchy granular developments along grain boundaries, to complete carbonate cements (Pl. 1(e)). More intense impregnation is generally restricted to narrow bands or thicker discon- tinuous lensoid zones in the clay-cemented rock units. Hydrated ferric oxides may also extensively replace the clay mineral and secondary carbonate matrix components, especially in zones of iron enrichment in weathering profiles. The compact, even-grained arenites of the Waratah Sandstone unit and the lower part of the succeeding Lambton Subgroup, are similar in composition to the soft fluvial arenites. The fresh rock is grey-green in colour and exceedingly tough. Weathered materials, too, are generally hard and only slightly friable. This characteristic toughness is attributed not only to inherent high textural density, but to developments of thin grain boundary cements of ferrous carbonate (PI. 1(f)). Tight packing of the constituent rock, quartz and feldspar is evident in thin section (PI. 1(f)). Although often highly deformed by squeezing between the compacted fragments, the larger flakes of mica and carbonized plant material may retain preferred orientation roughly parallel to the bedding direction in the aggregate. Chlorite, as small mossy green aggregates, is a distinctive minor (<5%) detrital consti- tuent of the Waratah Sandstone (Table 2, spec. 077). Other heavy minerals, including zircon, ilmenite (largely replaced by anatase and hydrous ferric oxides), tourmaline, rutile, apatite, chromite and picotite, are also important accessory constituents. Most commonly these are evenly disseminated through the rock HOWRNAL ROYAL SOCIETY N.S.W. HAMILTON PLATE I PLATE | Quartzose sandstone from the Maitland Group (HVC132), showing its closely packed texture. Quartz is the dominant sand-size component ; rock fragments and plagioclase feldspar in subequal proportions are the chief accessories. The sparse matrix consists mainly of kaolinite and degraded mica—crossed nicols— X36. Fluvial lithic arenite from the Tomago Coal Measures (HVM072), showing the variety of shapes exhibited by the quartz constituents—crossed nicols—X36. Micas from a Newcastle arenite (HVN118), showing effects of intrastratal degradation. Muscovite flake at lower left is virtually unaltered, while the others are leached and bloated. Flake at lower right is partially replaced by vermicular kaolinite—crossed nicols—X58. Degraded mica (muscovite ?) flake from a Tomago lithic arenite. Thin remnant layers of highly birefringent material are interleaved with the leached and hydrated mass at left. On the right the flake is replaced by aggregates of weakly birefringent kaolinite—crossed nicols—X143. Secondary iron carbonate replacements in a Tomago arenite (HVM194). The carbonate (very high relief) occurs interstitially, and as replacements of the more susceptible clastic units. The feldspar prism at the lower left is almost completely pseudomorphed—plain light—X22. - Waratah Sandstone (HVN076), showing the typical close-packed texture, with the clastics clearly outlined by thin surface layers of finely granular siderite—plain light—X58. JOURNAL (ROY AE SOCTE TNGAN SM. HAMILTON Weiler PLATES2 Tomago clayey siltstone (HVM049) consisting of fine to coarse silt-size particles dispersed uniformly :n an abundant clay matrix—crossed nicols—X22. Partially reworked banded texture of a Tomago lutite (HVM052), possibly representing a stage in the development of the uniform texture shown in (a)—crossed nicols—X22. Interlaminated siltstone-claystone from the Tomago Coal Measures (HVM067)—crossed nicols—X22. Tuffaceous claystone (HVM189) from the Tomago Coal Measures. Angular fragments of rock, quartz, mica and feldspar are embedded in an abundant matrix of fine clay and carbonaceous material. Much of the coarse detritus is probably of pyroclastic origin—plain light—X57. Vitroclastic texture of the Wallarah tuff (HVN116) from Swansea. Sparse quartz grains occur through the aggregate which is composed predominantly of montmorillonite. Silica may be present in significant amounts in the fine matrix material—crossed nicols—X57. Lithic tuff (HVN105) from the Mount Hutton Formation of the Newcastle Coal Measures. The fragments of vitric tuff are embedded in a matrix of ragged montmorillonite clay particles—crossed nicols—X29. JOURNAL ROYAL SOCIETY N.S.W. AMVETS ON Se eaves Sal PLATE 3 (a) Electron micrograph of a bentonitic clay from the Newcastle Coal Measures, showing filmy, sheet-like crystals of aluminous montmorillonite. Most units are exceedingly thin and flexible and have resisted disintegration during mechanical dispersion. (b) Electron micrograph of bentonitic clay from a thin tuff band in the Scotch Derry Seam (Tomago Coal Measures), showing the fine particle-sizes of the constituent minerals. Platey montmorillonite anhedra contrast strongly with the associated thicker, hexagonal kaolinite units. wy PETROGRAPHY OF SOME PERMIAN SEDIMENTS aggregate ; more rarely they may be concen- trated in thin segregation “ streaks’ through the mass. From “hydraulic equivalence ”’ considerations (Rubey, 1933; Rittenhouse, 1943) high concentrations of heavy minerals are to be expected in fine-grained arenites. However, their segregation from the lighter constituents, in the present instance, seems to imply that the deposits have been subjected to some degree of post-depositional reworking. Such a concept would certainly accord with the well-graded particle-size characteristics of the Waratah arenites. (11) Lutites Siltstones and silt-shales are the most common lithologies of the Tomago and Newcastle Coal Measures and possibly of the Permian succession generally. Significant deposits of relatively pure silt rocks appear to be limited in occurrence to the thick arenite sequences of the stratigraphic successions. Materials containing less than 20% total clay and sand occur in the Newcastle Coal Measures as textural variants of the massive Waratah Sandstone. The matrix of this silt rock typically constitutes about 10% of the total aggregate, while fine sand may be present in concentrations of 5 to 10%. Fresh materials are grey to blue-grey in colour, very compact and hard. ‘Textures are usually massive, but the inclusion of richly carbonaceous bands may frequently impart distinct fissility to the rock. The mineralogy of the Waratah silts parallels that of the associated arenite lithologies (Table 2, compare 077 and 099). Tightly packed, sub- angular to subrounded fragments of rock, quartz and feldspar are associated with minor quantities of detrital muscovite, biotite and chlorite in a finely vermicular clay matrix/ cement. The massive rock types contain only sparse, disseminated plant detritus. Shaley equivalents contain higher proportions, usually concentrated in discrete bands. Silt variants, containing as little as 8% matrix clay, are also associated with the marine Cessnock Sandstone. In the more prevalent lutaceous delta facies, relatively pure silt rocks are represented as lithological variants of channel sand sequences, or more commonly, as thin stringers and laminae in thinly-banded clay/silt materials. The textural heterogeneity of the banded rocks is very evident in hand specimen. Layers of light-coloured massive siltstone up to 2 cm. thick contrast strongly with the carbon- pigmented and strongly laminated clay-rich 231 horizons. Fresh materials are soft to moderately hard, friability being directly related to the proportion of silt layers present. The sharply defined bedding planes are usualiy undulose and disturbed. Interpenetration contacts be- tween adjacent and coarse elements reflect turbulent conditions of deposition for the silt materials. The general textural and compositional characteristics of these silt layers imply genetic interrelationships with the arenaceous sediments of the fluvial channel units which are interbedded with the banded rocks. The typical aggregate is composed of fine-grained lithic fragments, quartz, feldspar and leached mica, embedded in a matrix of recrystallized clay mica and secondary kaolinite. The materials are mode- rately well-packed and particle sizes seldom exceed a maximum of 0-1 mm. Extensive sequences of the banded silt-clay rocks may include thick persistent interbeds of massive lutite materials, which are moderately carbonaceous, and usually contain high pro- portions of silt and fine sand. Plate 2(a) illustrates the texture, in which an abundant fine sand-silt fraction of quartz, feldspar, mica and macerated plant detritus is dispersed in a matrix of degraded clay mica. The matrix may constitute between 20 and 40% of the rock. The general physical attributes of the massive rocks are clearly intermediate between those of the purer silts and clays, which suggests that they may in fact represent homogenized products of banded silt-clay rocks (PI. 2(c)). This inference is certainly substantiated by occurrences of partially reworked disrupted banding (PI. 2(0)) in many of the uniform clayey silt units. Permian claystones and clay-shales contain high proportions (>70%) of clay particles, but none examined contain the minimum quantity (>80%,) requisite for classification as a “ pure ”’ claystone. Silt is the chief contaminant. Sand- size components seldom exceed 10% concen- tration. Four distinct claystone types have been identified in the studied stratigraphic sections. Carbonaceous claystones and clay-shales are most commonly developed as the floor and roof rocks of the coal seams in the Tomago and Newcastle Groups. Even textures, fineness of grain and high carbon contents reflect conditions of stable quiescent deposition which ultimately contributed to the accumulation of the coal materials. Colour and texture of these claystones are governed by the abundance and degree of comminution of the carbonaceous components. 232 Highly carbonaceous types are dark grey or brown in colour with strong fissility induced by planar concentrations of coarse leafy detritus. Sediments containing only disseminated fine carbon particles are lighter in colour and lack any pronounced bedding fissility. Non-clay and non-organic clastics are of minor importance. Fine quartz particles up to 0:05 mm. in diameter, and partially leached flakes of muscovite and biotite associated with particles of volcanic and sedimentary rock, rarely constitute more than 5% of the aggregate. The principal matrix components of the carbonaceous claystones are invariably kaolinite, and randomly interstratified mica-mont- morillonite in varying relative proportions. (Tables 2 and 3, specs. 108, 090). Massive, medium to dark grey szlty claystones of marine origin (Maitland Group) are exposed in the open cut working of the Hunter Valley Stoneware. Pipe Co,» at.Kurrn’ Kurr. ; The material is extremely plastic when wet and shrinks markedly on drying. In thin section the rock appears as a uniform mass of very fine shred-like clay crystals, enclosing rare interspersed silt-size quartz and feldspar particles. Patchy ferric oxide staining is related to weathering in zones adjacent to shrinkage fractures. Preferred orientation of the flaky elements, which is lacking in the fresh rock material, may be developed in these narrow weathered zones, as a_ result of recrystallization. Montmorillonite is the dominant individual mineral constituent (Table 3, spec. 130), but kaolinite and quartz in approximately equal proportions together constitute more than half of the aggregate. The minus two micron clay fraction of the sediment is enriched in mont- morillonite (60%). Kaolinite (30%) is an important accessory, while quartz is represented in’ minor quantities only (<= 5%). Ferruginous silty claystones of Dalwood age from the Forest Reserve pit of Cessnock Potteries Ltd. are soft to moderately hard, grey or pink, fine-grained massive rocks. Pronounced grittiness is due to the inclusion of quantities of fine sand and silt in the clay. Patchy red colouration results from the partial replacement of the clay matrix by secondary hematite/goethite. Nodular clay ironstone is the ultimate replacement product in some zones. The iron oxide-free sediment consists essentially of fine sand to coarse silt-size fragments of rock, quartz, feldspar and mica, dispersed through an abundant matrix of clay J. D. HAMILTON minerals and very fine quartz silt. Rhyolitic— and dacitic volcanic fragments comprise the bulk of the rock detritus. Granitic, granophyric, pelitic metasedimentary and quartzose frag- ments are also represented as accessory con- stituents of the suite. , The detrital quartz grains are mainly ‘metamorphic’ types, crowded with dusty inclusions, trails of fine fluid inclusions and occasionally, identifiable crystalline inclusions (especially muscovite and tourmaline). The strained and fractured condition of these quartz crystals readily distinguishes them from “volcanic ’’ derivatives which are typically unstrained and inclusion-free. Grains of untwinned, slghtly kaolinized perthitic potash feldspar are much less abundant than the plagioclase (oligoclase) types, which occur as fresh, twinned anhedra or prismatic cleavage fragments. The detrital mica group includes muscovite and biotite, showing evidence of severe leaching and hydration (im situ). Sparse fragments of finely macerated plant material are evenly disseminated through the rock. In some cases where the tissue structures have been preserved, intergrowths of secondary clay mica and vermicular kaolinite fill the open cell voids. Montmorillonite and kaolinite in subequal proportions are the principal constituents of the rock matrix, representing up to 50% of the rock aggregate (Table 3, spec. 137). Iron- enriched rock types show varying degrees of replacement of the clay matrix by aggregates of fine blood-red to orange red hematite/ goethite platelets. Tuffaceous claystone is represented in the section of Tomago sediments exposed in the Waterloo Firebrick Co. pit at Thornton. It is pale brown-pink to medium grey-brown, depending upon the organic carbon content. The more richly carbonaceous layers are slightly fissile, but generally the rock is quite massive and breaks with a conchoidal fracture. Sporadic textural heterogeneities in the form of. thin bands or lenticles of silt and sand-size clastic particles are evident on close examination. In thin section these fragmentary constituents are revealed as rock, quartz, mica, and feldspar in that order of abundance. Although con- centrated in thin zones, the particles are well dispersed in the abundant fine-grained clay matrix (Pl. 2(d)). The coarse clastics are poorly sorted (estimated size-range 0-02 to 0:80 mm.), and of diverse ‘ PETROGRAPHY OF SOME PERMIAN SEDIMENTS 233 TABLE 3 Mineralogical Composition of Fine Siltstones, Claystones and Tuffs from the Permian Deposits of the Lower Hunter River Valley Palts pet tem ve wt Spec. Rock Type 8 Seam . No. 5 N 3 = = = = et a oo f tee | ie ee emo eae, Pierce ae eae Se See Ss wee Se See Se OO fF SS F&F Ze FS OC |HO & O PERMIAN Newcastle Coal Measures 118 Clayey Siltstone — 3 Tr — 2 —_—- — Tr — Tr 095 Clayey Silt-shale . ae —.: 3 creas 0-5 3 — 13. Fel 090 Carbonaceous Silty Clay- -shale .. --- 4 0-5 3:5 0:5 1:5 — — Tr — 0:2 108 Carbonaceous Silty Clay-shale . — 2:5 0-5 4 — 3 —-— — Tr — 3:0 iG Altered Vitric Luft — 4 — 1 —_ — 58 — Tr — Ol 120 Altered Volcanic Breccia _ 4 —- — 2 —- — 4 — {1:0 — Tr 097 Weathered Interlaminated Clayey Silt- stone/Silty Clay-shale .. — 3 0-5 3 1:5 1:5 — 0-5] Tr — Tr Tomago Coal Measures 058 Clayey Sandy Siltstone — 3 0-5 I> O0-d 5 —- — }0°5 — 1:1 060 Sandy Clayey Siltstone .. —- 2:5 0-5 1:5 0-5 4 0-5 180 Interlaminated Clayey Siltstone/Siltstone —- 3 0-5 2 0-5 4 —_—-— — Tr — 0:2 Note Clayey siltstone .. —- 2 0-5 1:5 0-5 — 4:5 — | 0-2 — 0-1 195 Interlaminated Clayey ‘Siltstone/Silty- Clay-shale .. --- 3 0-5 2 0-5 — 4 — —- — 0:5 061 Interlaminated Sandy Clayey Siltstone/ Silty Clay-shale. — + 0-5 3 1 2 0-5 181 Interlaminated Clayey _Siltstone/Silty Clay-shale = BO oir 2 1 3:5 — — Tr — 0O-l 17 6 Interlaminated Clayey Siltstone/Silty Clay-shale _— 3 Da. od 1 4-5 — — Tr — 0:8 182 Interlaminated Clayey Siltstone/silty Clay-shale : : — + — 2:5 Tr 38 —- — —- — Ol 054 Carbonaceous Clayey Silt-shale_ (Micaceous) = 2-5 lr. 5:01 5 ees) 052 Interlaminated Clayey Siltstone/Silty Clay-shale : — 3°75 0-5 I 1 — 4:5 0-3 089 Tuffaceous Silty Claystone . Sparse eithic Frags. 3°5 — 2 1 35 — — —- — 0:3 068 Tuffaceous Clayey Siltstone (Micaceous) Altered Volcanic Rock 0-5 Tr 5:5 0-5 3:5 — — Tr — 0:8 069 Bentonitic Clay (Pyritic) . Altered Pumice 0:5 — 2:5 — — 7 --= Ir. 3:0 “022 059 Weathered Silty Claystone _— 2-5 0-5 1-5 1 4-5 — — —_ — 0-2 Maitland and mateeod Groups 130 Silty Claystone : a 3 dB es! — — — — Tr 137 Ferruginous Sandy Silty ‘Claystone — 3 O- be 2 —_—- — 3 — | 2:5 — 0:4 1 Determined by X-ray, cation exchange 2 Determined by chemical analysis. 3 Determined by heavy mineral analysis. and chemical analysis. 234 shapes. Quartz occurs as highly angular frag- ments, arcuate and wedge-shaped splinters, or even as well-rounded and embayed grains. The rock fragments including sedimentary and metamorphic, as well as acid volcanic varieties, typically show moderate rounding. However, some volcanic fragments may possess highly angular outlines. The larger detrital mica flakes in general show evidence of extensive leaching and hydration. Clay minerals constitute at least 80-90% of the rock matrix. Hydrous mica and mixed- layer mica-montmorillonites predominate, and are associated with kaolinite in approximately 2: 1 proportions (Table 3, spec. 189). The remaining 10-20% of the matrix comprises comminuted plant detritus distributed fairly uniformly through the clay aggregate. The genesis of this rock type is obscure. While some features, especially those related to the nature and distribution of the erratic silt and sand components, would imply a partly pyroclastic origin at least, others would indicate a normal detrital source. Certainly the occurrence of mixed-layer minerals rather than montmorillonite in the clay grades, suggests a closer relationship to the non-volcanic sediments than to the tutis. Adjacent to pyritic coal seams the tuffaceous claystones are extensively leached and _ re- crystallized. Mixed-layer micaceous components are largely converted to kaolinite, which may constitute up to 75% of the clay fraction. The original heterogeneous texture of the rock is usually well preserved. The more susceptible constituents (rock fragments, feldspar, mica) are at least partially replaced by aggregates of secondary vermicular kaolinite and finely granular ferrous carbonate. The carbonate is restricted mainly to the coarse-grained bands and is consistently associated with carbonized plant materials. One occurrence of such leached material in the Thornton Fire and Building Brick Co. pit at Thornton (PI. 2(d)) contains numerous small rods and prisms of apatite up to 0-1 mm. in length, concentrated mainly in the coarser-grained laminae. The fresh euhedral and unabraded subhedral con- dition of the crystals and the inclusion of sparse fluid-filled cavities suggests a primary pyro- clastic origin for this constituent. (iv) Tuffs Tuffs are more prevalent in the Newcastle than in the Tomago Coal Measures successions. Bentonitic deposits of the Tomago Group are typically thin, but are often laterally persistent, J. D. HAMILTON especially as bands in coal seams. Similar types of deposits occur in the Newcastle sequence, but are usually associated with other thicker units, which may be of very limited lateral extent. Soft, waxy or plastic clays largely replace the original components of the coal seam tuff bands. Textural characteristics of the original pyroclastic products are retained to varying degrees in the clay aggregates. The thickest band from the Scotch Derry Seam (Tomago Group) at Thornton retains only a few relict features indicative of original rock character. This clay is light grey to white in colour, often stained yellow by free sulphur from the coal, and flecked with black, due to included carbonaceous material and secondary pyrite crystal aggregates. The dry clay is soft and friable ; when wet it is extremely plastic. The coarse pyroclasts have been largely replaced by clay aggregates, but some quartz, feldspar and lithic fragments are _ still identifiable. Relict outlines indicate original particle diameters ranging up to 1mm. and averaging about 0-5mm. The grains were evidently angular, ovoid and less frequently, splinter-shaped. Two principal phases are represented in the secondary clay suites. Dioctahedral mont- morillonite, as colourless to pale yellow aggregates of fine ragged crystals, replaces the greater part of the original matrix material and embedded pyroclasts. The subordinate colourless vermicular kaolinite component occurs mainly as pseudomorphs of other coarse clastic units. The constituent clay particles, as a rule, lack preferred orientation, but may show small degrees of aggregate alignment adjacent to, and parallel with, the margins of the replaced fragments. Radial orientation patterns are sometimes developed in clay aggregates, re- placing the bubble walls of pumice particles. Tuffs of the Newcastle Coal Measures are typically more “ rock-like’”’ in the unweathered condition. Fresh materials from a_ thick (30 ft.+) sequence of the Wallarah Tuff Member (subunit of the Munmorah Conglomerate), exposed in the Belmont Stoneware Pipe Quarry at Swansea, are hard, brown to grey-brown clay rocks, somewhat ~~ chert-like * in appearance, and have a distinct waxy lustre. Variations in carbon content accentuate the bedding and reveal developments of small-scale sedimentary structures—especially current bedding. The hardness of the rock possibly reflects a moderate degree of silicification. PETROGRAPHY OF SOME PERMIAN SEDIMENTS A high silica content is certainly indicated by the bulk rock composition (Table 3, spec. 116). The Wallarah tuff (Pl. 2(e)) has a_ well- developed vitroclastic texture (Williams, Turner and Gilbert, 1954, p. 154). However, much of the original glassy ash and lithic components have been replaced by secondary montmoril- lonite. Leached mica flakes and splinters of quartz and plagioclase, up to 0-2mm. in diameter, are the chief accessory constituents of the aggregates. Welding is not apparent. The textures of vesicular pumice fragments are often pseudomorphed by aggregates of radially- disposed clay scales, which replace the bubble walls as sequences of concentric shells. The original textures of most other lithic pyroclasts are recognisable only where clay replacements are incomplete. Very fine-grained vermicular kaolinite is probably the dominant matrix component. Secondary iron oxides and carbonate are minor accessory constituents, especially in zones adjacent to iron-enriched bedding horizons and joint fissures. Tuff from the Kotara Formation (Cardiff Subgroup) exposed in Wardley’s Clay pit at Hillsborough, is distinctly more lithic. In this section (Pl. 2(/)) fragments of vitric tuff and tuffaceous lava are visible in an abundant matrix of montmorillonite and kaolinite clay particles. Small deposits of coarser lithic ejectamenta occur in the Wallarah Tuff Member at Swansea. In the section exposed in the Belmont Stone- ware Pipe Co. pit, the Wallarah Seam rests directly upon a six to eight inch band of volcanic breccia, consisting of lithic and crystal frag- ments up to 3 cm. in diameter (average 3 mm.), embedded in a massive matrix of extremely plastic montmorillonite/kaolinite clay (Table 3, spec. 120). The material has a streaky pink- white colour due to patchy iron staining. The clastic fraction, which may constitute 70-80% of the aggregate, includes fragments of heavily iron-stained dacitic and rhyolitic rocks with fine-grained or glassy textures; crystal tufis, containing abundant ill-sorted angular particles of quartz, feldspar and flakes of mica; and tuffs, showing vitroclastic and vesicular textures, pseudomorphed by clay minerals. Coal frag- ments occur sporadically in the aggregates. Larger quartz and feldspar grains up to 0:2 mm. in diameter are minor constituents only. The quartz pyroclasts have well-rounded and em- bayed outlines, are commonly fractured, and contain inclusions of ferric oxide. Kaolinized 235 cleavage fragments of albite/oligoclase are the dominant feldspar components. Fresh sanidine crystals may also occur rarely. (b) Grainsize Distributions (i) Avenites Arenites from the Lower Hunter Permian succession are well-sorted to moderately well- sorted sediments. The distributions of quartzose sandstones from the Dalwood and Maitland Groups (Fig. 3(a)) typically show small devia- tions (g'=1-5—2-0) about well-defined modes in the fine to very fine sand grades (o?=2-4). Lithic arenites of the Tomago and Newcastle Groups are on the average less well-sorted (og=2:-5-3-5). These higher deviations in most cases, are attributable to the inherent bimodality of the distributions for the traction grades of the aggregates. Figure 3 demonstrates the range of textural variation in these coal measures rocks. From the plots it is clear that both open deltaic products of the Waratah Sandstone type ((d)--(f)) and the more prevalent channel sand deposits ((0), (c)) show wide variations in silt content. The extensive “tails ’’ usually developed in the clay range (o>7) of the arenite size distributions are not primary textural phenomena, but are reflections of the particle-size and dispersion characteristics of the secondary matrix components. (11) Lutites The lutites of the Tomago and Newcastle Coal Measures comprise a complete lithological suite linking the arenite and claystone textural extremes. From Fig. 2(c), (e) it is evident that, within the sandstone/clayey siltstone range, particle-size variations are related primarily to changes in sand content, the ratio silt: clay remaining virtually constant. For Tomago Coal Measures sediments an average ratio of 3: 1isindicated; for Newcastle Coal Measures materials the value appears to be higher— about 4: 1. Analyses of the thinly banded siltstone/claystone sediments plot mainly within the “clayey siltstone’ region of the triangular diagram (Fig. 2(d), (f)). The evident mechanical similarity of the banded rocks and other homo- geneous clayey siltstones may well be significant, especially in the light of earlier inferences concerning the origin of the latter type. For coal measures sediments containing less than about 10% sand, the silt: clay ratio decreases progressively towards an observed minimum of 1 Deviation measure proposed by Inman (1950). 2=-log,d where “d’’ is particle diameter in millimetres. 236 approximately 0-25. Corresponding sediments from the marine successions may be even more clay rich. In general, the grain-size distributions of the silts are negatively skewed about single, prominent modes in the size range g=—4-6. The size distributions of the claystones are more diverse in character. Poor grading is typical. Principal modes are ill-defined (e.g. Fig. 5(b) (c)) or virtually lacking (Fig. 5(a)). The, “sand,” “mode in Vig. 5(@) is due, to: an admixture of glacial erratic material in the claystone. (111) Duffs Particle-size analyses of tuffs from the upper coal-bearing successions do not reflect primary textural characteristics so much as the morph- ological conditions of the secondary clay mineral constituents. | Electron micrographs of the minus two micron fractions of two montmoril- lonitic bentonites from Swansea (PI. 3(a)) and Thornton (PI. 3(0)) demonstrate the contrasting natures of the principal mineral components of these materials under normally dispersed con- ditions. On this basis the marked differences in particle size distribution (Fig. 5(e), (f)) of the parent clays may be readily appreciated. Summary and Conclusions Although largely restricted to a consideration of the Tomago and Newcastle Coal Measures the present study has served to demonstrate the broad compositional uniformity of the Permian sediments of the Lower Hunter region. Petrographic evidence has indicated that at least two major source environments contributed to the development of the wide range of epi- clastic lithologies represented in the successions —one predominantly volcanic and unmeta- morphosed—the other of deformed granitic and metamorphic character. ‘The: «closely, comparable sedimentary suites of the Tomago and Newcastle Coal Measures are dominated by detrital volcanic components ; those of the associated Dalwood and Maitland (marine) Groups received more or less equal contributions from the volcanic and metamorphic sources. Contemporaneous volcanic ash _ deposits, especially abundant in the Newcastle sequence, are largely altered to montmorillonite/kaolinite clays. Parallelism of textural trends in the Tomago and Newcastle sedimentary suites is confirmed by the grain-size distribution data. The unique stratigraphic, textural and mineralogical attributes of the Waratah Sand- J. D. HAMILTON stone unit set it in marked contrast to the fluvial sands of the Tomago and Newcastle sequences. Lateral persistence and lithological uniformity especially suggest development under unusually widespread, active sedimentary con- ditions—possibly in an open lacustrine environ- ment—providing opportunity for extensive re- working and sorting of the materials. The genetic interrelationships of the various lutite lithologies are fairly clear. The silt rocks of the Waratah Sandstone are unique. Like their arenite counterparts they are well-sorted and highly consolidated. The more typical deltaic interfluvial deposits include rock types ranging from thinly interlaminated siltstone/ claystones, to massive clayey _ siltstones. Observed field and textural relationships imply a genetic link between these seemingly diverse lithologies. The evidence suggests that the laminated textures, which appear to be funda- mental to the interfluvial environments, have been locally reworked to form the massive (but mechanically identical) clayey siltstone units. Poor sorting in the claystone rock types may be at least partly due to hybridisation. Thus, secondary modal concentrations in the coarse grades of some materials are nearly certainly primary detrital features, representing admix- tures of flakey detritus (e.g. mica, plant frag- ments), or even erratic materials of volcanic or glacial origin (e.g. Fig. 5(d)). Other features of the distributions, especially those related to the clay grades probably reflect the degrees of dispersion more than the original micellar distribution characteristics of the component minerals and thus lack any real geological significance. The particle-size distributions of the altered tuffs too, are probably functions of dispersion and are virtually unrelated to the original pyroclastic textures of the materials. Acknowledgements The author wishes to express his appreciation to Professor C. E. Marshall for his supervision in this work, which was carried out in the Department of Geology and Geophysics, Uni- versity of Sydney. Sincere thanks are also due to the managements of the clay products industries of the Maitland-Cessnock-Newcastle region for their help and co-operation in the collection of field samples, and to Dr. Drummond of the Electron Microscope Unit of the Uni- versity of Sydney, and Dr. J. Sanders of the C.S.I.R.O. Division of Tribophysics, who pro- duced the electron micrographs. PETROGRAPHY OF SOME PERMIAN SEDIMENTS References BAILEY, E. H., AND STEVENS, R. E., 1960. Selective staining of K-feldspar and plagioclase on rock slabs and thin sections. Amer. Min., 45: 1020-1021. BOOKER, F. W.:, BURSILL, C., AND McELroy, C. T.., 1953. Sedimentation of the Tomago Coal Meas- sures in the Singleton-Muswellbrook Coalfield : an introductory study. J. Proc. Roy. Soc. N.S.W.., 87: 137-151. Booker, F. W., 1960. Studies in Permian sedimenta- tion in the Sydney Basin. Tech. Rep. N.S.W. Dep. Mines for 1957, 5: 10-62. CaRROL, D., 1940. Possibilities of heavy mineral correlation of some Permian sedimentary rocks of New South Wales. Bull. Amer. Ass. Petrol. Geol., 24: 636-648. CuLEey, A. G., 1938. The heavy mineral assemblages of the Upper Coal Measures and Upper Marine Series of the Kamilaroi System, N.S.W. J. Proc. moy. Soc. N.S.W., 72: - 15-105. Davin, Eb: W.'E., 1907. Ihe geology of the Hunter River Coal Measures. Geol. Surv. N.S.W. Mem., G. 4. Day. P. K., '9b0. Physical basis of particle-size analysis by the hydrometer method. Sozl Scz., 70: 363-374. HaAnton, F. N., OSBORNE, G. D., AND RaaGGatTtT, H. G., 19538. Narrabeen Group: its subdivisions and correlations between the South Coast and Narrabeen—Wyong Districts. J. Proc. Roy. Soc. N.S.W., 87: 106-120. InMAN, D. L., 1952. Methods for describing the size distributions of sediments. J. Sediment Petrol., 22: 125-145. Jones, L. J., 1939. The coal resources of the southern portion of the Maitland-Cessnock-Greta coal district (northern coalfield). Geol. Surv. N.S.W. Min. Res., 37. 237 LouGunan, F. C., 1960. The origin, mineralogy and some physical properties of commercial clays of INS. W. Geol Series 2 (Univ.“of N-S:W., School of Mining Eng. and Appl. Geol.). LouGHNAN, F. C., aND CraiG, D. C., 1960. Occurrence of fully-hydrated halloysite at Muswellbrook, N.S.W. Amer. Min., 45: 783-790. LOUGHNAN, F. C., AND SEE, G. T., 1959. Bentonites and. Pullers arth “deposits of N.S: Wes: Occurrence, mineralogy and physical properties. Proc. Aust. Inst. Min. Metail., 190: 85-103. MACKENZIE, R. C., 1951. A micro-method for determi- nation of cation-exchange capacity of clay. /f. Colloid Sct., 6: 219-222. OsBORNE, G. D., 1950. The structural evolution of the Hunter-Manning-Myall Province, N.S.W., Roy. Soc. N.S.W., Monograph No. 1. RaGGaTT, H. G., 1938. Evolution of the Permo- Triassic Basin of east-central N.S.W. D.Sc. ‘Thesis, University of Sydney. RITTENHOUSE, G., 1943. A visual method of estimating two-dimensional sphericity. J. Sediment. Petyrol., 13: 79-81. RITTENHOUSE, G., 1943. The transportation and deposition of heavy minerals. Bull. geol. Soc. Amer., 54: 1725-1780. RuBEy, W. W., 1933. The size distribution of heavy minerals within a _water-laid sandstone. /. Sediment Petrol., 3: 3-29. TREFETHAN, J. M., 1950. Classification of sediments. Amer. J. Sct., 248: 55-62. VolisEy, A. H., 1959. eastern N.S.W., Australia. N.S.W., 92: 191-208. WENTWORTH, C. K., 1922. class terms for clastic 30: 377-392. WILLIAMS, H., TURNER, F. J., AND GILBERT, C. M., 1954. Petrography. Freeman and Co.: San Francisco. Tectonic evolution of north- Je Proc. Wey. .50e: A scale of grade and Sediments: | J. saab. Journal and Proceedings, Royal Society of New South Wales, Vol. 98, pp. 239-262, 1966 The Geology of Mandurama-—Panuara R. E. SMITH ABSTRACT—Investigation of an area between Mandurama and Panuara, approximately 30 miles south of Orange, New South Wales, has resulted in more detailed knowledge of the stratigraphy and petrology of the Ordovician and Silurian formations as defined by Stevens (1952 and 1954), and Bruce and Langley (1949). There is a lateral facies change in the Angullong Tuff from lavas, tuffs and breccias in the west to a volcanic labile greywacke suite together with subordinate lavas in the east. This confirms the presence of a north-south trending Ordovician volcanic island ridge which passed through the west of the Area associated with the Molong Geanticline as described by Packham (1958). The alteration of the Ordovician formations correlates with the prehnite— pumpellyite metagreywacke facies of Coombs (1960). The graptolite assemblages investigated indicate a Darriwilian age (zones D2-D3) for patt of the Ordovician Malongulli Formation, and a Melbournian age for part of the Silurian Panuara Formation. Introduction The Area described in this paper lies approximately 30 miles south of Orange between Mandurama and Canowindra, see Fig. 1. The lithologies present in the Area studied represent sedimentation and vulcanism from pre-Middle Ordovician time (as represented by the Walli and Mount Pleasant Andesites) through Middle Ordovician and Upper Ordovician times (re- presented by the Cliefden Caves Limestone, Malongulli Formation, and the Angullong Tuff). A structural gap exists in the history between the Upper Ordovician Angullong Tuff and the Upper Silurian section of the Panuara Torma- tion. Zoning of graptolites was obtained by reference to Thomas’ paper (1960), “ The Zonal Distribution of Australian Graptolites’”’. Field locations of points of interest are given using the standard Military grid for the Blayney and Canowindra one inch to the mile sheets. The subscripts ‘2’ and ‘8’ as shown on the map, Fig. 6, have been omitted in the text for simplicity. The five figure numbers of specimens refer to rock thin sections catalogued in the University of Sydney. The Ordovician formations, namely, the Angullong Tuff, Malongulli Formation, Mount Pleasant and Walli Andesites, have undergone alteration of a regional extent, presumably due to burial. The mineralogical adjustments are extensive and hence the rocks are said to have undergone a low grade of metamorphism. The original textures of the rocks are usually visible and schistosity is generally absent. The rocks have been deformed by simple concentric folding. This paper follows the regional investigations of Stevens in his Ph.D. thesis (University of Sydney, 1954), and his papers of 1952 and 1953. Owing to the scale of the map, Fig. 6, detail of field mapping could not always be included, G eeait (is ——-—7 Ryall aa CANOWINDRA Ww, : ay —., Stern High Highway Baihorsn=ce 6 Miles Fig. 1 240 and imterested readers are referred “to. the original thesis at the University of Sydney, where a detailed map at the scale of one inch = approximately 800 feet is available. The quality of outcrop in the Area is generally good, in places it 1s excellent, “as, for example, along Swallow and Cadiangullong Creeks and the Belubula River. There is an area south of “Millamolong’ Station, where outcrop is poor and the lithology can only be inferred from the soil) characteristics, the structure’. being obscure. Stratigraphy and Petrology WALLI ANDESITE Defimtion. Stevens (1954): “The Walli Andesite (after Walli, a locality north of Woodstock) is the name given to volcanic RK. Ee Svilir rocks which make up the oldest Ordovician formation exposed. The type area lies between Walli and Limestone Creek, and the best outcrops are along the creeks which flow north into the Belubula River . . 7 J) Aem@edded members are infrequent, the thickness of the formation can only be estimated; however, there appears to be at least 4,000 feet of sequence in the Davy’s Creek Anticlne; “Oursee ihe Area studied, the formation outcrops in a belt five miles wide, extending south to Woodstock, but the base of the formation is not known to outcrop. The Walli Andesite dips to the north-east on the east limb of the Davy’s Creek Anticline, named by Stevens, 1954, and is conformably overlain by the Cliefden Caves Limestone. Good exposures of Walli Andesite are offered Generalized Stratigraphic Sequence West part of the Area Tertiary Basalt Panuara Formation SILURIAN Angullong Tuff Malongulli Formation Gisbornian Z < = > O a) oa O Walli Andesite Key to the Dominant Lithologies Shale & siltstone Arenite Limestone Cliefden CavesLimestone East part of the Area x 1000 ft Angullong Tuff Malongulli Formation Mount Pleasant Andesite Greywacke conglomerate Lava, tuff & breccia Andesite & basalt THE GEOLOGY OF MANDURAMA-PANUARA in the Limestone Creek section, between grid references (880400) and (882430). The Walli Andesite consists predominantly of porphyritic andesites and_ fine-grained vesicular basalts, associated with subordinate volcanic breccia and tuff. Excellent pillow lava structures are exposed along Limestone Creek, for example at grid reference (882418) where pillow lava grades downward into non- pillowed amygdaloidal lava. The pillows range from four feet to eight feet in diameter, frequently with subspherical upper surfaces. Adjacent pillows tend to mould upon one another, and are separated by thin dark-green chilled selvages + to 4 inch across. Bands of breccia, usually less than one inch across, may occur between the chilled selvages. Amygdules often show concentric elongation near the margins of pillows, however, other amygdules may show radial elongation. The basalts are fine-grained hypocrystalline with intersertal to microlitic textures. Pheno- crysts are not abundant in the basalts, however, when present they tend to form clusters resulting in glomero-porphyritic textures. The phenocrysts consist of albite, augite, and pseudomorphs after both pyroxene and olivine, in that order of abundance. The olivine is always pseudomorphed, and is only recognised by its euhedral outline. The pyroxene shows valious stages of replacement by secondary minerals but in many cases relic augite remains. Growth of the secondary minerals quartz, albite, chlorite, prehnite, epidote, carbonate, and pumpellyite has somewhat modified the textures. The andesites are porphyritic with large phenocrysts up to 8mm in length of albite, sometimes in association with phenocrysts of hornblende or augite. The groundmass may be trachytic, having microlites of albite with interstitial chlorite, epidote, granular opaques and sphene; or may be a felt of albite laths, chlorite, epidote, opaques and sphene. Acicular Opaques are widespread accessory minerals in the Walli Andesite. The lavas and breccias of the Walli Andesite show various stages of low grade metamorphic alteration with the formation of the following authigenic minerals: albite, chlorite, epidote, prehnite, pumpellyite, quartz, carbonate, and sphene. The same minerals occur as amygdule fillings. Such a mineral assemblage indicates a grade of metamorphism similar to the prehnite- pumpellyite-metagreywacke facies of Coombs, (1960). The widespread occurrence of Cliefden Caves and equivalent limestones overlying the Walli 241 and Cargo Andesites indicated general marine conditions followed the extrusion of the ande- sites. Limestone at grid reference (875400) lies within Walli Andesite. In addition the frequent occurrence of pillow lavas suggests an underwater environment. On the above evidence, it appears that much of the Walli Andesite was probably extruded under marine conditions. No other indication of environ- ment was obtained. Mount PLEASANT ANDESITE The formation was named by Bruce and Langley (1949) after Mount Pleasant, grid reference (008430) where the rocks form a prominent outcrop. The Mount Pleasant Andesite outcrops in the south-east corner of the Area, and is con- formably overlain by cherty shales, siltstones and arenites of the Malongulli Formation, at grid reference (985420). Porphyritic andesites and basalts are interbedded with thin beds of volcanic labile arenite and siltstone. The formation appears to be 1,600 feet or more in thickness at Mandurama Ponds Creek. As both the Walli Andesite and the Mount Pleasant Andesite are the first volcanic formations below the Malongulli Formation, they are considered equivalent formations. The Cliefden Caves Limestone which separates the Malongulli Formation from the Walli Andesite at Lime- stone Creek is absent from the sequence at Mandurama Ponds Creek. Although no fossils have been found in this formation, it is known to be pre-Darriwil in age as Darriwilian graptolites have been found in the Malongulli Formation, see location CO.1/40, 41, 42, 43, this paper. Darriwilian graptolites were also found by Stevens (1954) in the Malonguli Formation above the Mount Pleasant Andesite in Mandurama Ponds Creek, at grid reference (990428). Pillow lavas are exposed in Mandurama Ponds Creek at grid reference (987416), 300 feet below the upper contact of the formation. The largest pillows are 8 feet in diameter, and are separated by a thin silty interpillow matrix varying from 4 to 1 inch in thickness. The porphyritic basalts have phenocrysts of albite and pale green augite ; the augite being in various stages of replacement by tremolite- actinolite. The groundmass is felty consisting of albite laths, interstitial chlorite, and ragged acicular secondary tremolite-actinolite, with granular epidote, sphene, and opaques. 242 A representative andesite, slide 23070, has phenocrysts of green-brown primary hornblende in addition to the albite phenocrysts. The groundmass is felsitic, and there is only a trace of opaques. The thin sections of the Mount Pleasant Andesite show alteration to albite, epidote, tremolite-actinolite, pumpellyite, carbonate, and sphene. The alteration could be due to hydro- thermal activity related to an igneous body, such as the Prince of Wales Diorite, or perhaps more probable, be due to low grade meta- morphism of a regional nature. If the latter be the case, the Mount Pleasant Andesite can be correlated with the higher zone of Coombs’ prehnite-pumpellyite-metagreywacke facies of metamorphism. Some of the basaltic and andesitic pillow lavas of the Mount Pleasant Andesite may have been sill-like bodies intruded into semi- consolidated marine sediments. An extrusive lava may cause partly intrusive relations with the overlying sediments by ploughing into semiconsolidated muds. CLIEFDEN CAVES LIMESTONE Defimtion. Stevens 1954: “The Cliefden Caves Limestone takes its name from the caves which are situated in the upper part of the formation on the south side of the Belubula River, 10 miles north of Woodstock ... The formation consists chiefly of light-grey massive limestone ; at some places thinly-bedded fossili- ferous limestones are present at the base. The maximum thickness is about 2,000 feet, east of the Cliefden Caves ”’. The Chefden Caves Limestone conformably overlies the Walli Andesite and conformably underlies the Malongulli Formation near Lime- stone Creek, grid reference (881421), but is absent from the sequence at Mandurama Ponds Creek where the Malongulli Formation con- formably overlies the Mount Pleasant Andesite, grid reference (988420). At Limestone Creek, large brachiopods and corals are common in the bedded limestone which forms the lower member, however, there is a vertical change to massive grey limestone with occasional chert nodules. Fossil fragments do not form a conspicuous part of the massive limestone, but organic remains are sometimes visible in thin section; one such slide contained part of a bryozoan, slide 23096. One mile to the north-west of Limestone Creek, at grid reference (875435), the structure R. E. SMITH is simple and the Cliefden Caves Limestone is seen to be approximately 800 feet in thickness. Just how far the limestone continued eastward from its outcrop at Limestone Creek is not known, as the top of the Walli Andesite-Mount Pleasant Andesite is not exposed between this creek and Mandurama Ponds Creek. However, it is apparent, due to the absence of the Cliefden Caves Limestone at Mandurama Ponds Creek, that the limestone has undergone a facies change. The cherty shales and siltstones, which form much of the Malongulli Formation at Mandu- rama Ponds Creek, probably represent deposi- tion in a bathyal environment. The distribution of the Cliefden Caves—and equivalent—Lime- stones represents part of the paleogeographical neritic environment which was. associated with the structural ridge, the Molong Geanticline. The conclusion is that, during Middle Ordovician times, there was a general deepening of the sea eastwards, away from the meridional geanti- clinal ridge, the axis of which lay close to the west margin of the Area. Moors (1963), working in the area immediately to the west of Limestone Creek, states that part of the Clefden Caves Limestone is definitely Gisbornian in age and may extend down into the Darriwil. MALONGULLI FORMATION About one-third of the Area shows outcropping Malongulli Formation. This formation forms most of the central portion. of the Area. A complete sequence of the Malongulli Formation is exposed along Mandurama Ponds Creek and part of the Belubula River, as is described below. There appears to be a major anticlinal structure in the centre of the Area, causing the formation to show a wide outcrop. Defintion. Stevens 1954: The Malongulli Formation . . . “is named after the Parish of Malongulli, north of Woodstock. The type area is between Malongulli Trigonometrical Station and the Belubula River near ‘ Kalimna’.. . Two distinct facies are present ; a calcareous facies in which most of the sediments are laminated calcareous siltstones or impure lime- stones (spiculites), and a siltstone-arenite facies, in which the sediments are feldspathic siltstone interbedded with arenites, tuffs and some lava flows. “The calcareous facies is developed in the type sakedea. The siltstone-arenite facies of the Malongulli Formation is developed in a broad arc east, north and south-east of Cliefden Caves. ”’ THE GEOLOGY OF MANDURAMA-PANUARA The occurrences of the Malongulli Formation described in this paper should, therefore, lie in Stevens’ siltstone-arenite facies. It is apparent, however, that this division of the Malongulli Formation into separate facies is a generaliza- tion and, in fact, most of this formation in the west and central portions of the Area are transitional between the two facies of Stevens. The Malongulli Formation in the east at Mandu- rama Ponds Creek can be placed in the siltstone arenite facies. Mandurama Ponds Creek Section Between Junction Reefs and the Mandurama —Canowindra Road, beds of the Malongulli Formation outcrop. They strike north-east and dip gently north-west at 25° to 30°. The upper boundary of the formation has been mapped against the overlying Angullong Tuff, grid reference (946462), about a mile north of Junction Reefs. The lowest unit of the Malon- gulli Formation conformably overlies andesitic lavas and volcanic labile arenites of the Mount Pleasant Andesite at grid reference (988421). Several east-west trending faults outcrop along the Belubula River at Junction Reefs, grid reference (967436), the total displacement of the series of faults has been calculated by Henderson (1953) as being 600 feet, south block down, causing repetition of the ore beds either side of the river. A total thickness of 5,500 feet (corrected for the fault displacement) of Malon- gulli Formation is exposed in sequence at Mandurama Ponds Creek ; the accuracy of the total thickness is expected to be + 500 feet. In this sequence the Malongulli Formation can be divided into three dominant lithologies : (i) Cherty shales and siltstones, which form 75° of the formation. (ii) Labile arenites, which form 20°, of the formation. (iii) Andesites, which form 5% of the forma- tion. (i) The shales and siltstones vary from light-grey to black in colour, and have a con- choidal fracture when fresh. The rocks are well bedded with bedding planes separated at intervals of 2 inches down to less than + of an inch. The weathered rock is hard, light- grey to buff and sometimes leached in outcrop. The fresh rock is often pyritic, calcareous, and exceedingly hard to split along bedding planes. The detritus consists of feldspar (mainly plagioclase), quartz (usually less than 25% of the rock), and carbonate, in a cryptocrystalline 243 matrix of reorganised mud. The coarsest material is usually less than oT mm in diameter. Some of the opaque granules are detrital. Detrital grains of altered ilmenite in crystallographic intergrowths with an opaque mineral are present in trace amounts. Sphene granules may form up to 5% of the mode. The chief authigenic or secondary effects are the recrystallisation of carbonate, albitisation of plagioclase, patchy development of prehnite, and the general development of chlorite and granular pyrite. (ii) The labile arenites at the base of the Malongulli Formation, grid reference (988421), show a moderate quartz content of 15°, which is in contrast with the usual Angullong Tuff labile greywackes where quartz is lacking or absent. Of the rock fragments, porphyritic andesites are the most frequent, sometimes forming 45°, of the mode. However, fragments of dacite and rhyodacite are conspicuous and form 10% to 15% of the mode. Of the crystal detritus, plagioclase predominates. Pale green augite occurs in minor amounts. The frame- work of the arenites has been somewhat con- densed during burial and deformation of individual grains is sometimes apparent where neighbouring grains meet. Twin lamellae of plagioclase crystals are at times bent, and some quartz grains have fractured. A microcrystalline chloritic matrix occurs as a thin filling between grains. The detrital grains are angular to subangular, the size sorting 1s moderate. Rock fragments range from less than 0:2 mm up to 2mm. By increase in the size of rock fragments, the arenites grade into labile conglomerates which have fragments up to 5 mm in diameter. The arenites higher in the Malongulli Forma- tion, grid reference (970430), have a lower percentage of detrital quartz, typically 1% to 5%, and are finer grained than the arenites at the base of the formation. Crystal detritus, chiefly plagioclase and pyroxene, is dominant over andesitic rock fragments. The sorting for size is fair. The cement is generally chloritic, although patches 1mm across may be seen where the cement is calcareous and in other cases feruginous. (iii) The andesites as exposed at grid reference (970428), in the middle of the Malongulli Formation, are either lavas or sill-like intrusives. Typically the andesites have phenocrysts of hornblende, augite, and less commonly, plagio- clase, set in a felty groundmass of plagioclase microlites, interstitial chlorite, granular opaques and sphene. Other Occurrences In the centre of the Area, three north trending limestone conglomerates can be traced for three or four miles. They cross the Belubula River at the junction of Flyers Creek, grid reference (943495). The conglomerates contain rock fragments of andesite, basalt, shale, siltstone and limestone, reaching a maximum diameter of 1 inch. The conglomerates are often uniform in thickness over considerable outcrop, but may gradually increase in thickness from 10 feet to 100 feet. Between Swallow and Cadiangullong Creeks, the conglomerates are folded into a northward plunging syncline and are joined by six or more conglomerates of similar nature. Interbedded with the conglomerates are hard grey to black shales and siltstones. Malongulli Formation outcrops over a large area on the east and west slopes leading down to Cadiangullong Creek. Numerous gullies offer good exposures. The outcrops south of the junction of Rodds Creek, grid reference (940535), show a complicated structure due to the develop- ment of concentric folding on a mesoscopic and macroscopic scale. The lithologies south of Rodds Creek are dominantly shales and silt- stones, at times calcareous, with thin horizons of labile arenite. North of Rodds Creek the lithologies are similar but the structure is simpler with the beds dipping uniformly to the north-east. Approximately 2,000 feet of Malongulli Formation outcrops between Rodds Creek and the overlying Angullong Tuff. The complete section of Malongulli Formation is not exposed. The black shales are frequently fossiliferous, especially in the vicinity of grid reference (937546) ; graptolites are the most abundant fauna, occurring with = small brachiopods (see locations CO.1/40, 41, 42, 43). Truncated sedimentary structures and current scours indicate intermittent turbulence. Shale, siltstone, and minor calcareous sand- stone of the Malongulli Formation outcrop along the lower part of Swallow Creek, upstream of the Narambon Fault. The sandstones are usually less than 5 feet thick and weather to a porous crumbly rock often containing small articulate brachiopods, as at grid reference (917530). The structure along this part of swallow Creek is complicated, due to the presence “of \;several” faults sand) \ isolated occurrences of intense, concentric™ ‘folding: Intrusion of the diorite body at grid reference (918525), and its associated dykes, has further complicated the relationships. Hard grey siltstones of the Malongulli Forma- tion outcrop east of the Rowland Syncline RE Serre underlying the Angullong Tuff, at grid reference (910470). The rocks, although porous due to leaching, are still sufficiently compact to preserve graptolites in fair detail. These grey siltstones are probably the equivalent to the black pyritic siltstones seen elsewhere in the Area. Limestone conglomerates, interbedded with blue-grey to black shale and siltstone and bearmg limestone pebbles” up: to,se simone. im. diameter, outcrop in the west limb of the Rowland Syncline, at grid reference (892453). The conglomerates are 600 feet to 1,000 feet below the overlying Angullong Tuff. Provenance The source area for the lower arenites at Mandurama Ponds Creek was volcanic in nature, containing andesite, dacite, and rhyo- dacite volcanic rocks. The abundant quartz, some of which is vein quartz, can be assigned to such a source. There were no rock fragments or crystal detritus characteristic of a meta- morphic source. The distance of transport of the detritus of the lower labile arenites was not very great, as concluded by their im- maturity of mineral components and texture. The source area for the middle arenites con- tained intermediate to basic volcanics, probably hornblende-pyroxene andesites. The source for these arenites contrasts with that of the lower andesites in that there are no fragments of dacites or rhyodacites amongst the detritus, and that quartz is less common. The quartz and feldspar of the shales and siltstones probably came from the volcanic source during quieter periods of sedimentation. The calcareous detritus is of intraformational origin, much of it being fragments of organic TESTS: The presence of hornblende-augite basalt 400 feet from the base of the Angullong Tuff at grid reference (936553) indicates volcanic activity of a basic nature nearby. The Malongulli Formation represents generally quiet sedimentation with occasional periods of rapid sedimentation, under somewhat euxinic conditions. It is inferred that a neritic environ- ment existed in the west of the Area probably extending into the east where, as suggested by the very fine grained cherty lithologies, there may have been alternations with a bathyal environment. Deposition was in a subsiding basin, probably at the edge of a eugeosyncline during a quiet period of tectonic activity. THE GEOLOGY OF MANDURAMA-PANUARA ANGULLONG TUFF Conformably overlying the Malongulli Forma- tion, the Angullong Tuff consists of a thick sequence of intermediate to basic volcanic rocks and their associated sediments. Defimtion. Stevens (1954): “ The Angullong Tuff, named after ‘ Angullong’ Station (Estate) north of Cliefden Caves, is the uppermost Ordovician formation in the region. It con- formably overlies the Malongulli Formation and at some places there is a lateral gradation at the formation boundary. The type area is along the Belubula River downstream from “Kalimna’ and the formation extends north and east towards Cadia and Junction Reefs respectively. It is not known whether all the formation is exposed in the type area where it is unconformably overlain by Devonian sedi- ments. The maximum thickness is estimated to be at about 1,500 feet, an approximate figure due to complex structures and lack of a well-exposed sequence. “The section exposed along the Belubula River downstream from ‘ Kalimna’ shows siltstones and tuffs at the base, followed by andesitic tuffs, andesites, felspathic sandstone and siltstone. ”’ The formation is at least 8,000 feet in thick- ness at Cadiangullong Creek ; 5,000 feet within the Area studied, plus a further 3,000 feet immediately to the north (Offenberg, 1963). The volcanic rocks consist of basalts and andesites with tuff and volcanic breccia. Volcanic labile greywacke and greywacke con- glomerate predominate in the eastern portion of the Area. There is an overall lateral facies change from a dominantly marine greywacke suite with a small percentage of lavas in the east to a volcanic suite of breccia, tuff and lava in the west. Superimposed on this is a vertical facies change in the west, at ‘ Angullong ’ and ‘ Millamolong’ Stations, where the base of the formation is represented by texturally sorted volcanic arenite and limestone conglo- merate indicating a neritic environment. These lithologies give way vertically to devitrified glassy tuffs and coarse volcanic breccia con- taining rock fragments up to 18 inches in diameter. In Rodds Creek, at erid reference (955554), a thin coral reef containing in situ halysitids and favisitellids, outcrops for about 20 feet along strike. Cadiangullong Creek Section An excellent exposure of the lowest 5,000 feet of Angullong Tuff is offered in Cadi- anguilong Creek between the Errowanbang- D 245 Panuara Road, grid reference (948570), and the upper contact of the Malongulli Formation at grid reference (943553). The sequence consists predominantly of volcanic labile rudites and arenites, with subordinate lavas and minor lutite beds. The epiclastic rocks show sedi- mentary structures characteristic of the Grey- wacke Suite (Packham, 1954). The beds dip uniformly at 50° to 60° to the north-east. Soft sediment deformation is seen in the shales and siltstones about 12 feet below the boundary of the Angullong Tuff at grid reference (943553). The style of folds and their relations with the overlying beds are not like those of a slump structure. Formational gliding of the Angullong Tuff over the semiconsolidated Malongulli Formation could cause the observed style of deformation. If so, rising connate water squeezed out of the semiconsolidated muds and silts of the Malongulli Formation owing to superimcumbent load of the Angullong Tuff, could provide the necessary lubricant. (1) Redites. The rudites are greywacke conglomerates consisting essentially of fragments of igneous and sedimentary rocks in a greywacke matrix. The rock fragments are commonly angular to subangular with low sphericity. A small percentage of the rudites shows more rounded grains. Angular fragments sometimes reach 6 inches to 8 inches across. The rudites typically form bold outcrops. The rock frag- ments are of the following types :— a. Porphyritic basalts and andesites. These can be matched with the volcanics of the sequence. There are three main _ varieties, spilitised albite-augite basalt, albite andesite, and hornblende-augite andesite. b. Shale and siltstone. Fragments of shale and siltstone may be subordinate to the volcanic rock fragments as in most of the greywacke conglomerates, or they may be the only rock fragments as in the intraformational conglo- merate or breccias. c. Limestone fragments. Locally, frag- ments of limestone occur in the conglomerates ; generally they are less than 4 inch in diameter. The framework of the greywacke conglo- merates is frequently partially or completely disrupted (Pettijohn, 1957), that is, the boulders and pebbles or phenoclasts are not always in mutual contact, but are frequently scattered and isolated throughout the matrix. In such instances the framework on its own would be unstable in the gravitational field, but is supported by the matrix. It seems, therefore, 246 that the framework and the matrix were deposited simultaneously ; such deposition can be explained by mud flows, or turbidity currents. The greywacke conglomerates, by decrease in size of the rock fragments, may grade upwards into labile greywackes. One greywacke conglo- merate, at grid reference (945554), contains rock fragments of 2 inches in diameter at its base, but the size of the fragments decreases to less than 5mm at a height of about 2 feet from the base. Finally, after 12 feet of thickness, the rock grades into labile greywacke with a grain size of about }mm. The style of graded bedding of this specimen is typical of that produced by differential settling from a turbidity flow (Pettijohn, 1957, p. 171; Menard, 1951, p. 9), in contrast to that produced by a waning current. Horizons of intraformational breccias occur in places throughout the column. The fragments are of shale or siltstone, similar to the shale and siltstone of the formation, and are dis- tributed throughout greywacke or greywacke- siltstone. Most of the fragments are tabular with subrounded corners, while others are well rounded. One example, at grid reference (945556), shows an intraformational breccia arising from the upper section of a slump structure. The fact that the breccias are within labile greywackes and greywacke siltstones suggests that they are due to subaqueous processes. Such processes can be caused by turbidity currents which cause pull aparts, and slumping. Evidence for turbidity current action and slumping has been seen elsewhere in the sequence. Shoaling can also cause fragmentation of the mud and silty layers leading to intraformational breccias. (11) Aventes. As mentioned above, the greywacke conglo- merates, by decrease in size of rock fragments, may grade upwards into greywackes. However, as most greywacke units are of granule or coarse sand size at their base, the grading leads only to finer greywacke. Unless outcrop is good, it is often difficult to determine widths of individual greywacke units. Throughout the sequence, the relationship of increase in width of beds to increase in grain size is apparent. The bedding units less than 1cm in width have silt-sized particles as their coarsest detritus. The greywackes are greenish-grey in hand specimens. The fresh rock is hard, compact, with little or no porosity, and has an uneven fracture. Specks of sulphide minerals some- times may be seen. The crystal detritus is RE SMITE usually of sand size. It is rare to detect any detrital quartz with the hand lens. In thin section, the greywackes show a fairly consistent composition. There is some variation in the proportions of the components, but this is mainly a function of grain size, the coarser varieties being richer in rock fragments. The essential components are subrounded to angular grains of plagioclase, clinopyroxene and horn- blende with varying proportions of rounded to angular rock fragments, in a silty clay matrix. The detrital quartz content is noticeably low, seldom exceeding 5%. The rock fragments are of the same types as those of the greywacke conglomerates (see above), andesites and por- phyritic basalts predominating over the shale and siltstone fragments. At least 70% and probably more than 90% of the detritus is volcanic in origin. An advanced state of authigenic alteration has, in many slides, made percentage estimates difficult, due to reorganisation of the matrix and infringement of the matrix minerals into the detrital grains. However, the greywackes all lie within the labile greywacke field of the M.L.Q. diagram of Packham (1954) (see Fig. 3), M = matrix, L = labiles, unstable minerals and. rock fragments, O = quartz plus ‘chert: |. /1t seems appropriate to qualify the term ‘labile greywacke’ with the addition of the word “volcanic ’, volcanic labile greywacke has specific genetic implications. Gi) Shale and Sultstones. Well-bedded shale and siltstone form only 15% of the column. Their occurrence is random throughout the sequence. The maximum. M Labile Yreywacke Fig. 3 THE GEOLOGY OF MANDURAMA-PANUARA thickness of any one sequence is 150 feet. The greywacke siltstones plot between the labile greywackes and the pelite field on the M.L.Q. diagram. As the grain size increases, the bedding planes become more widely spaced. The shales and finer siltstones show better sorting than the greywacke siltstones, both in grain size and in recognisable mineral content. Fine siltstones show a quartz content of 10% or 15%, feldspar 20°, in a brownish mud matrix containing opaque material, some of which may be organic in origin. Slumping may be seen in the shale and silt- stone beds. The slumped beds range from 9 inches to 2 feet in thickness. At grid reference (945557), the slumps are truncated by erosion of their upper surfaces, indicating that slumping took place prior to or during deposition of the overlying bed. (iv) Pvroclastics. In the Cadiangullong Creek sequence, pyro- clastic tuffs are not common. Most specimens examined could be classified as being either epiclastic or igneous, rather than pyroclastic. It was not possible in the case of two of the slides examined (two out of 40) to decide on an epiclastic or pyroclastic origin. One slide (23128) shows a framework composed almost entirely of devitrified glass shards, with some plagioclase and _ clinopyroxene fragments cemented by interstitial carbonate, chlorite, prehnite, and ? clay minerals. The delicate Shapes of the angular shards are preserved. There is neither evidence of flattening nor of plastic flow after emplacement. The rock, possibly a pyroclastic, may represent volcanic fallout into water as the rock overlies a pillow lava. It could also be a transported tuff, if so, the mechanism of transport was_ sufficiently gentle so as not to destroy the delicate shards. (v) Lavas. Lavas form 10% of the stratigraphic column at Cadiangullong Creek. They are intermediate to basic in composition, and all have porphyritic textures. Three different lava types have been recognised, spilitised albite-augite basalt, horn- blende-augite andesite, and albite andesite. Spilitised albite-augite basalt forms the major pillow lava which outcrops over a distance of 24 miles along strike from Panuara, grid reference (926578), to Cadiangullong Creek, grid reference (945555). Large euhedral pheno- crysts up to 5mm in length of light coloured plagioclase and dark pyroxene are characteristic and easily seen in outcrop. The lava is approxi- 247 mately 200 feet thick at Cadiangullong Creek. The lower 100 feet 1s massive lava and rests conformably on shale which has been indurated for about 1 inch next to the contact. In the upper part of the lava, pillow structures are developed. The pillows reach 5 feet in diameter, adjacent pillows being separated by a thin band of interpillow matrix, varying from 4 inch to 3 inches in thickness and consisting of indurated mud layers and volcanic debris. The actual chilled margin of the pillow lava is thin, being + inch to #4 inch across, and is seen as pale groundmass due to the de- velopment of authigenic chlorite and prehnite. The plagioclase phenocrysts are now albite, containing large patches of prehnite, chlorite and carbonate. Mosaics of quartz aggregates may be in part pseudomorphic after pyroxene, although pale green augite, in many cases, is free from alteration. The groundmass is hyalopilitic or pilotaxitic with sub-aligned euhedral albite laths. The mesostasis consists of chlorite, feldspar, sphene and opaque dust. The mesostasis, at times, has the appearance of devitrified glass. Some of the chlorite mesostasis may be pseudomorphic after mafics. ‘ Angullong’ Station Angullong Tuff is exposed in a broad belt extending from ‘ Angullong’ homestead to the Belubula River with a total thickness in excess of 3,500 feet. The upper part of the Angullong Tuff is transgressed by the Silurian Panuara Formation with which its boundary is either unconformable (as it is one mile to the west), or is faulted. Outcrop is only fair and the thicknesses have only been calculated off the map as dip readings are not very abundant. The formation has been folded into a series of gentle synclines and anticlines which plunge north at about 40°. Dominant amongst the lithologies are coarse fragmental rocks. Many of these are volcanic breccias, although thin sections are sometimes required to distinguish these from labile grey- wacke conglomerates. The rock fragments are almost exclusively of andesitic lavas. Shale and siltstone fragments are scarce. The Angullong Tuff on ‘ Angullong’ Station shows characteristics which contrast with those at Cadiangullong Creek Section. The sequence is composed dominantly of volcanic breccias with minor andesitic lava. Labile greywackes and greywacke conglomerates appear to be absent in the upper member, Member B, their place being taken by the coarse pyroclastics. The lower member, Member A, consists of 248 conglomerates, some of which have limestone pebbles, with subordinate shale and siltstone. Member A. The lowest 1,000 feet of Angullong Tuff consists of 60°, limestone conglomerate, and 40% shale and siltstone. The conglomerates contain limestone pebbles 1 inch to 2 inches in diameter ; the matrix is feldspathic. Limestone pods develop at grid reference (908519), where pods of limestone up to 3 feet long and 9 inches thick show a lateral facies change into impure limestone and calcareous siltstone. This calcare- ous horizon is only 5 feet in maximum thickness but can be traced laterally for about 1,000 feet. The shales and siltstones become in- creasingly scarce higher up in the sequence. They are typically black and hard when fresh, but weather to a buff colour ; some are lighter in colour and are calcareous. Member B. The upper portion of the Angullong Tuff exposed has been grouped as one member 2,500 feet or more in thickness. It consists mainly of coarse fragmental rocks. A traverse along one gully, grid reference (885515), which offered good exposure of volcanic breccia revealed only one siltstone horizon 3 feet thick occurring near the top of the exposed sequence. The coarse fragmental rocks contain andesitic fragments up to 6 inches or 10 inches in maximum diameter set in a matrix which is deeply weathered. The fragments show various states of angularity, ranging from angular to subrounded, such variations being observed within one exposure. Several andesitic bodies occur throughout the upper member ; probably all are lavas. ‘ Millamolong ’ Station East of Limestone Creek on ‘ Millamolong ’ Station, the Angullong Tuff occurs as a keel to a major syncline, the “ Rowland Syncline ’. About 1,200 feet of sequence is preserved. At the base of the sequence, medium to coarse clastic sediments overlie hard grey leached siltstones of the Malongulli Formation. The sequence shows a vertical change from sandy volcanic epiclastics at the base to pyroclastics and extrusives higher up. The lowest member is a labile arenite rich in volcanic crystal detritus and lava fragments. Rock fragments may reach 4mm in diameter. The fragments consist of hornblende-augite andesite and plagioclase-hornblende andesite. Ree SMa Shale and siltstone fragments are lacking. The crystal detritus consists of plagioclase, hornblende, augite and some detrital opaques. Above the labile arenite member is a sequence of andesitic pyroclastics and lavas. The first lithology is a fine volcanic breccia approxi- mately 60 feet thick and has andesitic fragments up to 1 inch in diameter set in a feldspathic crystal tuff matrix. The rock fragments are of one type, namely spilitised albite-hornblende andesite; the tuffaceous matrix consists essentially of the same minerals as those forming the rock fragments. This volcanic breccia is overlain by interbedded crystal tuff and more volcanic breccia of a similar nature. Metamorphism The lavas, greywackes and _ greywacke conglomerates of the Angullong Tuff all show authigenic development of some assemblage of quartz, prehnite, pumpellyite, epidote, albite, chlorite, carbonate, and _ sphene. Quartz, prehnite, epidote, chlorite, and carbonate occur as amygdule minerals in the lavas. The extent of authigenesis is more apparent in the arenites, rudites, and in some lavas than in the shales and siltstones. Within the formation, the plagioclase of all rocks examined is albite. Relic zoning of the plagioclase may be recognised in both the lavas and the greywackes by the inclusions of chlorite, prehnite, carbonate, and epidote. The occurrence of calcium bearing silicates within sodic plagioclase is strong evidence for an originally more calcic plagioclase, the calcium released by albitisation being taken up by minerals such as prehnite, pumpellyite, epidote, and carbonate. Prehmte may also develop in the matrix of the greywackes and greywacke conglomerates, at times encroaching upon rock fragments and crystal detritus. Chlorite may be seen in all slides of the sequence. Chlorite shows various stages of replacement of crystal detritus, matrix, or groundmass of the lavas. Authigenic carbonate has been produced in some cases by the albitisation of plagioclase. Some carbonate, however, was detrital as shell fragments, limestone pebbles or as calcareous matrix. The detrital carbonate frequently shows reorganisation and secondary overgrowths into the matrix. Pumpellyite occurs as a secondary mineral within the plagioclase pheno- crysts and in the mesostasis of slides 23124, 23134, 23136. Allogenic clinopyroxene, pale green augite, is often apparently metastable, and at times may THE GEOLOGY OF MANDURAMA-PANUARA 249 persist after plagioclase, hornblende and rock fragments have been extensively altered to assemblages of chlorite, prehnite, epidote, and carbonate. However, slight marginal alteration and alteration along cleavage planes of augite to either albite, prehnite, chlorite or carbonate are not uncommon. Provenance The rocks of the Angullong Tuff have essentially the same provenance. The detritus of the labile greywackes and greywacke conglo- merates at Cadiangullong Creek contain rock fragments of porphyritic basalts and andesites with subordinate fragments of shale, siltstone and limestone. Rock fragments of plutonic and metamorphic lithologies are absent. The rock fragments are therefore either of intraformational origin or are correlatable with a volcanic source of intermediate or basic nature. The crystal detritus is in agreement with such a source. There has been little or no mineralogical sorting of detritus during transport and deposition. The rocks are also texturally immature. Sub- marine mud flows, slumps and turbidity currents are believed to be the prime methods of transport. The supply of detritus must have been rapid and abundant to enable unstable minerals and rock fragments to survive. Poorly consolidated lithic tuffs could provide a source of angular fragments and such a source could be rapidly eroded. Eruptions of submarine breccias may have also been a major process for the introduction of coarse angular lava fragments into sedimentary detritus. The general instability of such a volcanic island ridge would provide opportunities for the triggering off of submarine slides, turbidity currents, and slumps. Slump structures, at grid reference (944556), 1,400 feet from the base of the Angullong Tuff indicate a down slope direction to the east. Scant field evidence suggests a direction of provenance to the west. In the Area studied, there does not seem to be any decrease in rock fragment size away from the source region. Not all the greywacke conglomerates seen in the Area show grading. Many, containing coarse material several inches in diameter, are ungraded even over outcrop thickness of 16 feet or more. These greywacke conglomerates usually have a disrupted framework. It appears that, due to the effective density and viscosity of the suspension, rock fragments were not able to settle in a graded fashion. The grading or settling is said to be a function of the solid-fluid ratio (Pettijohn, 1957), that is, the framework to matrix ratio. The framework to matrix ratio of a grevwacke conglomcrate at grid reference (943553), which shows grading of rock fragments from a maximum of 2 inches diameter to sand sized particles of 0:2mm diameter over a thickness of 12 feet, is 3 : 1. That of an un- graded greywacke conglomerate is 7: 1. An- other angraded greywacke conglomerate has a ratio of 5: 1. It is probable that these un- graded, unsorted greywacke conglomerates are the products of mud flows whose solid to fluid ratio was too high for Newtonian settling to allow grading of the components (Pettijohn, 1957, p. 591). The lower member at ‘ Millamolong ’ Station is a clean washed, shallow-water, volcanic sandstone. The textures of the overlying tuffs and volcanic breccias indicate that they were hot when deposited as seen by the plastically deformed fragments. As the water was already shallow during the deposition of the basal member of the Angullong Tuff, it seems likely that the rapid addition of 1,200 feet or more of volcanic material would exceed the rate of subsidence and consequently the deposition surface may have risen above sea-level. It is therefore hkely that much of the sequence is terrestrial, the product of direct volcanic fallout, ash flows, and fragmental lavas. The basal member of the Angullong Tuff at ‘Angullong’ Station seems to represent deposition in a shallow neritic environment as seen by the presence of corals, brachiopods, and limestone conglomerates. The rapid influx of 2,500 feet or more of tuffs, volcanic breccias and lavas no doubt also raised the deposition surface above sea-level in this domain. The presence of very coarse blocks of lava 6 inches to 10 inches in diameter in the volcanic breccias suggests a proximity to the source. Environment of Deposition Immediately prior to the rapid influx of volcanic material which marks the base of the Angullong Tuff, which is Eastonian in age (Moors, 1963), a neritic environment extended over most of the Area. A nearby region, probably near the west of the Area, was under- going uplift, resulting in widespread limestone conglomerates. The lowest beds of the Angullong Tuff are seen in the centre of the Area as marine labile greywackes at Cadi- angullong Creek and as marine labile volcanic sandstones and limestone conglomerates in the west of the Area. As deposition proceeded, the sequence at Cadiangullong Creek remained submarine. The lowest members of the 250 Angullong Tuff at ‘“Angullong’ and ‘ Milla- molong’ Stations in the west of the Area were deposited in shallow water, and as accumulation of volcanic material proceeded, the deposition surface rose above sea-level, resulting in the unsorted volcanic breccias, tuffs and lavas, which form the upper members. The absence of typical continental sediment in the Angullong Tuff indicates that there was no continental land mass nearby shedding sediment into the deposition area. An island shore line, however, did exist during deposition of the base of the Angullong Tuff. A further 12 miles to the west, the marine epiclastic Millambri Formation is equivalent to the Angullong Tuff. From east to west we obtain the lateral facies change from marine Millambri Formation through the shallow water and terrestrial Angullong Tuff at the western margin of this Area, to the marine dominantly epiclastic Angullong Tuff in the east (see Fig. 5). The Angullong Tuff was associated with a north-south trending volcanic island chain passing through the western margin of the Area. PANUARA FORMATION Defimtion. Stevens (1954): “ The Panuara Formation, which takes its name from Panuara Rivulet, an alternative name for Four Mile Creek, consists of shales, siltstones and sand- stones, with one or two limestone beds near the base. The type area is on Bridge and Bull’s Camp Creeks and on Panuara Rivulet. The total thickness in this area is about 2,000 feet. Fossiliferous Silurian rocks from Lower Llan- dovey (Lower Silurian) to upper Wenlock (Upper Silurian) are included in the forma- tion ”’. That part of the Panuara Formation exposed consists of khaki shales and siltstones with grey to red sandstones. A thin horizon of lime- stone conglomerate and associated coral fauna (including halysitids and favositids CO.1/51) outcrop halfway up the sequence at grid reference (808540). Approximately 3,000 feet of Panuara Formation intermittently outcrops. The boundary with the underlying Angullong Tuff is poorly exposed but is not concordant and may be faulted. Three miles to the north- west, in the Cobbiers Creek Syncline, the Panuara Formation unconformably overlies the Angullong Tuff. The lithologies present within the Area belong to the arkose-quartzose-sand- stone suite (Packham, 1954). The lowest 1,000 feet consists of fine grained, even textured, khaki sandstone, with thin RoE? SMI interbedded khaki siltstone and shale, over- lain by 1,200 feet of sandstone lithology with subordinate khaki shale, minor limestone conglomerate and impure calcarenite. The sandstone is further overlain by 500 feet to 1,000 feet of dominantly well-bedded khaki and buff shales and siltstones. The shales are very weathered and crumbly in outcrop with lmonite enriched layers along bedding planes and joints. Varieties of Monograpius tumescens indicate a Melbournian or Upper Silurian age, for the top of this sequence exposed, grid reference (904559), location CO.1/44. Associated with the graptolite fauna are fragments of trilobites and small brachiopods. The presence of graptolites indicates a marine environment, in addition, the presence of in situ corals indicates that at times the environ- ment was epineritic. Oxidising conditions existed as seen by the presence of abundant haematite granules in the cement, the break- down of the haematite results in the general khaki appearance in outcrop. Deposition apparently took place on the shelf margin of an open basin. Regional Metamorphism The Ordovician rocks of the Area have been subjected to low grade metamorphism leading to the formation of secondary minerals, similar to those of the prehnite-pumpellyite metagrey- wacke facies described by Coombs (1960). The metamorphism is presumably due to a rise in temperature and pressure during burial. The oldest sequence of volcanics, the Walli and Mount Pleasant Andesites, shows the assemblage of quartz, albite, epidote, prehnite, pumpellyite, chlorite, carbonate, and sphene. In addition to this assemblage, tremolite- actinolite is present in some slides from the Mount Pleasant Andesite, at grid reference (989412). The assemblages of the stratigraphi- cally higher Ordovician formation in the Area, the Angullong Tuff, is apparently the same, except that prehnite is more extensively developed and pumpellyite is scarce. The rocks, in general, show undeformed fabrics ; relic textures are usually visible despite the extensive development of secondary minerals. As a first approximation one can assume uniform thicknesses of formations over a limited area. There are, however, limitations to this assumption, as the Malongulli Formation, for example, is known to wedge above the Cliefden Caves Limestone, see Fig. 5. Five thousand THE GEOLOGY OF MANDURAMA-PANUARA Stratigraphic Columns Angullong Malongulli Walli Tuff Formation Andesite d) (b) Cadiangullong Creek “‘Angullong’ Scale x 1000 ft (Cc) ‘Millamolong’ Omf < MEL: volcanic breccia basalt andesite siltstone, shale greywacke conglomerate limestone conglomerate TEER eee ¢ t tuff limestone Pillow lava arenite RUE 251 252 feet of Angullong Tuff outcrop within the Area at Cadiangullong Creek. Added to this thickness is a further 3,000 feet or more adjoining to the north (Offenberg, 1963). The Malongulli Forma- tion at Mandurama Ponds Creek appears to be approximately 5,000 feet thick. These figures give a minimum of 13,000 feet overlying the Walli and Mount Pleasant Andesites. Added to this estimate is the sequence of Silurian rocks which, from nearby field evidence, may add a further 2,000 feet or 3,000 feet. Younger formations are markedly unconformable on the Ordovician and Silurian formations and their relation to burial is more obscure. It seems, therefore, that the maximum depth of burial of the Walli and Mount Pleasant Andesites was in excess of 16,000 feet. In southern New Zealand, Coombs (1954) shows prehnite first appearing at a depth of burial of 23,000 feet, pumpellyite first occurring higher at 16,000 feet. Calcic plagioclase had almost completely gone over to albite by a depth of 17,000 feet. Crook (1960) at Wahgi Valley, found prehnite and pumpellyite at a depth of burial of 16,000 feet to 17,000 feet, and found albitised feldspar at the top of the sequence at 13,000 feet of burial. In the Mandurama-Panuara Area, the Ordo- vician Formations belong to the _prehnite- pumpellyite metagreywacke facies. The partly unconformable Silurian formations show authi- genic albite, chlorite, but neither prehnite, pumpellyite nor epidote is present. The Silurian lithologies are somewhat different in composi- tion to the Ordovician formations which are richer in labiles. As yet the relationship of metamorphism to varying lithologies is not clear. In the Permian rocks of the South Coast of New South Wales, Raam (1964) noted the occurrence of prehnite and pumpellyite, associ- ated with laumontite, under a calculated 3,000 feet of burial. Otalora (1964) records the occurrence of prehnite-pumpellyite in his Rio Loco Formation which consists of andesitic lava flows, flow breccias, and volcanic breccias. The calculated depth of burial is again low, being no more than 6,000 feet. Intrusive Bodies PRINCE OF WALES DIORITE Fic. 6A. The Prince of Wales Diorite is an _ inter- mediate to basic, medium to fine grained intrusive which outcrops between Junction Reefs and Burnt Yards, grid reference (970470). R. E. SMITH The name is taken from the discontinued ‘Prince of Wales’ Mine at the north-east margin of the intrusive. The Prince of Wales Diorite is the largest intrusive body outcropping in the Area, being about 14 miles across at its narrowest diameter. The body has a general boss-like outcrop, with minor cupolas in the south at Junction Reefs, grid reference (960440). The lithologies are dioritic to andesitic in character, two varieties being present. A porphyritic variety forms more than 60% of the exposed body. The aphyric variety occurs as several isolated bodies located near the margins of the porphyritic variety, as shown in the map. The largest aphyric diorite body is roughly 14 miles long and 1 mile wide, outcropping about 1 mile north of Junctior. Reefs, grid reference (968454). As seen from the outcrop pattern, the porphyritic variety does not seem to be a simple marginal facies of the aphyric diorite. The two varieties may represent two different intrusive occurrences. The aphyric diorite is classified as a uralitised augite diorite or augite microdiorite and reaches a maximum grain size of 4mm. The average mode is given in Table Ia. Anhedral orthoclase is frequently subophitic with euhedral plagioclase and pyroxene. Simple zoning is shown by the plagioclase, which has cores of labradorite An;, and rims of more sodic plagioclase, oligoclase Angy. Euhedral to subhedral pale green augite is partly replaced by tremolite-actinolite. Buiotite, when present, also shows partial alteration to tremolite- actinolite. Slide 23161 shows pale green tremolite- actinolite, or uralite in various stages of replace- ment of augite, frequently the tremolite- actinolite forms a margin around relic augite, and in some cases the pyroxene has been pseudomorphed. Many uralite patches contain opaque granules, probably representing iron released during the alteration. In one instance, augite shows replacement by uralite and calcite. Minute sphene euhedra about 0-02mm in diameter accompany the uralitisation. Although at times apparently optically continuous, the tremolite-actinolite pseudomorphs are usually composed of tightly packed fibres having a common orientation. The plagioclase shows extensive alteration typically to a felty mass of white mica, and in other cases to a white mica and tremolite-actinolite. The alteration of the plagioclase shows a preference for the cores which are more calcic than the rims. The orthoclase is clear except for patches of pink-brown clay products. THE GEOLOGY OF MANDURAMA-PANUARA The average mode for the porphyritic intru- sives is given in Table Ib. The porphyritic lithologies vary in coarseness of the groundmass and have been classified as uralitised porphyritic augite microdiorites and augite andesites. The phenocrysts of plagioclase and augite reach a maximum size comparable with that of the aphyric varieties, namely 1mm to 4mm. The groundmass is either granular or felty, and contains plagioclase, oligoclase An,;, tremolite- actinolite, interstitial chlorite, granular opaques, and a trace of biotite. As the Prince of Wales Diorite outcrops in the vicinity of the Junction Reefs Goldfield, the possibility of a relationship between the intrusive (or intrusives) and the genesis of the ore bodies has been investigated. The ore bodies at Junction Reefs occur over an area intruded by minor cupolas of the Prince of Wales Diorite. Sulphide mineralisation occurs with a gangue of tremolite-actinolite and carbonite. The mineralised “ ore-beds ’’ which appear to be altered labile calcareous grey- wackes occurring with altered siltstones of the Malongulli Formation also show development of sulphides, tremolite-actinolite, and carbonate. Sulphide mineralisation occurs again at the north margin of the Prince of Wales Diorite, at the ‘ Prince of Wales’ Mine. Sulphide minerals occur among the opaques of the diorite and microdiorites, all varieties of the pluton show accessory opaques. How- ever, in the porphyritic varieties, the percentage of opaques is higher and averages about 10°%%. Possible relations between the Prince of Wales Diorite and the mineralisation which lead to the formation of the ore bodies cannot be disregarded. MINOR INTRUSIVES Bie. 6, C, D, E and-F. Several minor intermediate porphyritic intru- sive bodies outcrop in the Area, viz at grid references (925510), (918520), and (958426). All show alteration leading to the formation of secondary minerals similar to those formed in the regional alteration or metamorphism of the Ordovician formations into which the bodies have intruded, and for this reason are considered to have been intruded before or during the metamorphism. The development of patches of prehnite, chlorite, epidote, and carbonate con- tained within albite is good evidence for the albitisation of an originally more calcic plagio- clase. These minerals may also occur as alter- ation products of the mafic minerals. In slide 23167, from grid reference (925514), the amphi- 253 bole has in some examples been pseudomorphed by epidote, and to a lesser extent by chlorite. Tables Ic, d, e, gives approximate modes of the intrusives. The microdiorite body which outcrops on the eastern slopes leading down to Swallow Creek, between that creek and Cadiangullong Creek, at grid reference (918520), narrows in outcrop southwards until at a minimum width of 100 yards, then widens gradually after crossing the river. The maximum width of the body on the south side of the river is 400 yards, on the north side it is about 500 yards. Along Swallow Creek, in the vicinity of grid reference (915525), numerous dykes and minor intrusive offshoots of the main body outcrop in the creek bed and in the side gullies and cut across shale and siltstone of the Malongulli Formation. The bodies are interpreted as being meta- morphosed quartz microdiorites. Their composi- tion is similar to that of some of the plagioclase- hornblende andesites which occur in the Angullong Tuff. The dominant textural difference is the more coarse groundmass of the microdiorites. The microdiorites may be magmatically related to the plagioclase-hornblende andesites. Evrowan Svyenite Fic. 6, B. One mile north-west of ‘Errowan Park’ Station, a medium to coarse grained inter- mediate igneous body has intruded the Ordo- vician Angullong Tuff, grid reference (000550). The rock is deeply weathered over much of the outcrop. The outcrop pattern is partly obscured by an overlying unconformable series of Tertiary lavas. The rock is an oversaturated syenite or quartz syenite. The texture is hypidiomorphic- granular, with an average grain size varying from 5mm to 2mm. Eubhedral pyroxene outlines are visible, although in some cases the pyroxene is pseudomorphed by tremolite- actinolite. Relic islands of augite are some- times seen at the centres of the altered pyroxene. Alteration of the pyroxenes may produce optically continuous pseudomorphs of amphi- bole, or ragged patches of acicular tremolite- actinolite intergrown with chlorite, epidote and opaques. The plagioclase, which has _ the composition of albite Ang to Ang;, 1s peppered with alteration to tremolite-actinolite, chlorite, and minor patches of prehnite. Polysynthetic twinning is barely visible due to the alteration. Microperthitic K-feldspar occurs as anhedral patches subophitically enclosing plagioclase, 254 pyroxene and anhedral quartz. Table If gives an approximate mode for the Errowan Syenite. Weemalla Dviorite One quarter of a mile east of the Panuara- Angullong Road, and one mile north-east of ‘Angullong’ Station, a small aphyric inter- mediate igneous body outcrops, grid reference (898540). The boss-like body is less than half a square mile in area, and has intruded Silurian sediments. The rock has been classified as a medium grained allotriomorphic-granular augite- quartz microdiorite. The plagioclase occurs as simply zoned subhedral laths arranged to give a felty texture. The composition of the plagio- clase lies in the andesine class, except for the outer margin of each lath which is oligoclase. Subhedral to anhedral colourless augite tends to accumulate in aggregates. White mica and biotite occur as ragged patches throughout the rock. Chlorite occurs as a replacement of biotite, and, to a lesser extent, of augite. An approximate mode of this Weemalla Diorite is given in Table Ig. Structure Field mapping shows that the Area can be divided into two major blocks. The western block, Block I, is about 20 square miles in area, and is bounded in the east by the Narambon Fault, and in the south-east by a region of poor outcrop. The second block, Block II, consists of the eastern two-thirds of the Area, containing about 30 or 40 square miles. Block II is divided into subordinate sections by the major north-south trending Wongalong Fault. Block I. In the west of Block I, the Walli Andesite and Cliefden Caves Limestone are separated from the main section of this block by a fault trending 330°. Bedded rocks of the Cliefden Caves Limestone terminate abruptly along strike against shales and siltstones of the Malongullii Formation. The fault outcrops in a gully at grid reference (899402), one quarter of a mile north of the Mandurama-Canowindra Road, where an 800 feet wide shear zone of folded slates and phyllites outcrops. The remainder of Block I is a structurally continuous unit, except perhaps for the extreme northern section of Panuara Formation, which may be faulted against the Angullong Tuff. The Rowland Syncline outcrops in the south of Block I. The west limb, dipping at an average of 20° or 30°, has a more gentle dip Ri Esha vee than the east limb which dips at 45° to 50°. The lowermost beds of the Angullong Tuff are preserved in the keel of the syncline and conformably overlie the Malongulli Formation. The syncline shows an overall plunge of 15° to 155°. The north section of Block I shows a series of gently folded synclines and anti- clines of Angullong Tuff plunging north at angles ranging from 20° to 34°. Deformation is by concentric folding; no cleavage being developed. The folds show undulation of the hinge areas and the folds tend to die out along strike of their axes into the limbs of other folds. The Narambon Fault A subvertical dyke-like body has _ been mapped continuously from the Belubula River northward over a distance of one mile. The ‘dyke’ is 10 feet to 20 feet across and contains brecciated cherty siltstone cemented by quartz- barite mineralisation. The siltstone fragments are typically less than one inch in diameter, and are similar to siltstones of the Malongulli Formation. The ‘dyke’ forms a prominent ridge, sometimes rising 10 feet above less resistant country rock. Further northwards, the ‘dyke’ gives way to smaller ‘dykes’ of similar nature. The ‘dykes’ are mineralised Shear zones. Several other shear zones occur subparallel in strike to the main ‘dyke’. Within the ‘dykes’ minor mineralised veins 1 foot to 2 feet across, containing 60% to 90% barite, occur but are discontinuous. Bedding has been deformed in the neighbourhood of the ‘dykes’ by complicated concentric folds and small faults. Small blocks of Ordovician and Silurian formations have been isolated by zones of shearing at grid reference (910530). On the macroscopic scale, as seen on the map, Angullong Tuff and Panuara Formation have been cut sharply by the ‘dyke’ bodies, and along strike adjoin the Maiongulli Formation. It is concluded that the dyke-like bodies represent the positions of faults and are mineralised fault breccias. It appears that faulting was not restricted to a single plane of movement, but occurred over a zone 800 feet to 1,000 feet wide. The fault zone has a trend of 350°, within this zone is a series of echelon component faults with a more westerly trend of 330° to 340°. The fault zone outcrops intermittently over a distance of five miles, disappearing at either end into areas of poor outcrop. The displacement of the Narambon Fault is not known. THE GEOLOGY OF MANDURAMA-PANUARA Block II. Angullong Tuff forms a major part of Block II. In the north of Block II, beds of the Angullong Tuff strike north-west and dip at 40° to 50° to the north-east. The formation boundary with the underlying Malon- gulli Formation strikes north-west at the north-west part of this block in accordance with the strike of the beds. However, at Rodds Creek, grid reference (952550), the formation boundary swings sharply to a _ north-south direction and the Angullong Tuff cuts across the trend of the Malongulli Formation. The boundary continues with a north-south trend for six miles, during which distance the trend of the Malongulli Formation swings and becomes subparallel to the trend of the formation boundary. Two miles north of Junction Reefs, grid reference (947462), the Angullong Tuff/ Malongulli Formation boundary turns again and takes a north-west trend again. The Wongalong Fault The discordant relationship of the Angullong Tuff to the Malongulli Formation during the north-south trend of the formation contact mentioned above is due to faulting along the contact. The boundary of the two formations between grid reference (946463) and (952550), is frequently sheared over a zone varying from 10 feet to 70 feet. Shearing is exposed at the Belubula River, grid reference (948477), where several minor faults are exposed in the river bed. Following the formation boundary north- ward, shearing can be seen in most of the side gullies of Cadiangullong Creek where the gullies cross the boundary. Tight concentric folding and shearing can be seen over a zone of 400 feet in width at Rodds Creek, grid reference (952550). The zone of shearing con- tinues northward along Rodds Creek. More evidence of this fault is seen at grid reference (947520) where the lowest beds of the Angullong Tuff end abruptly westwards along strike against north-south trending beds of the Malongulli Formation. It is concluded that a fault separates the Angullong Tuff and the Malongulli Formation between grid reference (952550) at Rodds Creek in the north, to grid reference (947462) south of the Belubula River. The fault is named the Wongalong Fault. This fault possibly continues northward along the shear zone in Rodds Creek and may join a north-south trending fault of Offenberg (1963) at grid reference (959600), however, outcrop between these two regions is not good. It is possible that the Wongalong Fault continues to the south and may join or be 255 associated with the Marangulla Fault at grid reference (955440). Minor Faulting Small scale faults are numerous along Swallow Creek. One fault can be traced intermittently northward from grid reference (920533). A series of limestone conglomerates and greywacke conglomerates, probably representing the base of the Angullong Tuff, are faulted against the Malongulli Formation at grid reference (923539). The fault has a shear zone 5 feet to 10 feet across and contains brecciated shale and sheared greywacke. The shear zone weathers mcre rapidly than the unsheared rock, and consequently the creek tends to follow the fault. Intense flexural slip folding of the bedded Malongulli Formation at grid reference (920534) occurs in the regions local to the fault. The main fault either bificates or is associated with several minor faults. Regional Setting A major volcanic arc dominated sedimenta- tion in the east of Victoria and central New South Wales during Upper Ordovician, through Silurian times until the end of Middle Devonian time. The igneous activity was concentrated along a narrow tectonic zone locally coinciding with a north trending ridge, the Molong Geanticline, which was active and _ passed through the Central West at Orange and extended northwards through Wellington. The geanticline was generally about 20 miles wide and is characterized by the abundance of limestone. This structure disappears to the south. The Mandurama-Panuara Area lies close to and on the east side of the axis of the geanti- cline. To the west of the geanticline lay the Cowra Trough, and to the east the Hill End Trough, limited further to the east by the Capertee Geanticline. Sedimentation of the Ordovician and Silurian rocks of the Area took place partly in the west margin of the Hill End Trough. The area adjacent to the west shows a Shallow shelly facies at Middle Ordo- vician time. Apparently vulcanism during Middle Ordovician and Upper Ordovician times was confined to the east side of the Molong Geanticline as lavas are lacking in the area studied by Ryall, 15 miles to the west (Ryall, 1963). During the period of activity of this volcanic arc there were periods of quiescence and stability with the development of isolated 256 R. 2. SMIPH Secti = oe eee etait Fault West Suggested Environmental Distribution ZZ a @ ? Terrestrial card Neritic / Bathyal Epineritic MA 5 Vv volcanic breccia Neritic = pe greywacke suite, (volcanic) = shale & siltstone Ed limestone or a pillow lava THE GEOLOGY OF MANDURAMA-PANUARA Scale in miles (b) bo “9 a x 256 R. E. SMITH THE GEOLOGY OF MANDURAMA-PANUARA bo ch a Section A-B : ae ' East Wert Suggested Environmental Distribution = in miles x1000%t 10 10 5 a (0) (0) shale & siltstone Neritic / Bathyal SS = : imestone : volcanic breccia - approximate environmental boundary = Epineritic =< p=] - Neritic Saal pillow lava greywacke suite, (volcanic) GEOLOGICAL MAP OF THE MANDURAMA — PANUARA AREA Reo oer Wh ke 3 : \|| : : 4 fE\I = HTT KE fei oe rea ity = \\I : | HT aaa | | : an | 5 Pattie : | ann ee “ / | | tt * YY 4 y eg 1] ty] rotator . : : || 1] HHI : | ment | | ' \| HTT | man : SEES : | PTT TTL Sat . | 1 {\] t] |} Sse HiT f WTVH : 3 : || | By ase MAA | a SEE ] || | | a Hh] | Bas || Bas | iI | jl | | : ay N ce : SS Th e y =". <\secuuen =: = | og 2, 9 ae ZZ WNW Perera THE GEOLOGY OF MANDURAMA-PANUARA 259 840 Ss ——— Mondurama 4 mile 2 ———— PeESS QA ae VN Scale in miles Sh p é 7 7 Sea / / S ‘ / ( —S i —< Se Se \ f \ a Si ii NS Ao me fe =a, Se : - : ens = : ea eM. = TS = ox 7, Aish Hy f Gh s Sa 4 190 +855 FZ + 340—_ GEGLOGICAR MAPS OF” THE MANDURAMA— PANUARA AREA 195 TN.MN @ 26 miles — Orange N= Prince of Wales <<: Dioribe.. © SEES \ WONGALONG—— ie} 4 —@ ~— Junction Reefs = We aie SS MIN) O% fps —s ; / Zs! 2 Lp ff ff Far fs\h / es a Ay 8 Ome ts oy, Yi, SS) S WG Sy, Ye VSS» 1. UM Cys fla PNW AIN ON ‘ YL pO ‘i LG Getty (OS 2 ee GS ZA flO SATA SED) 3 Ri Se) 2 Aas ds SianlG SS , @ || aod ~ a 2 ETL AO ——— i 2 Scale in miles ate" 2 Conowindra 14 miles 190 896 HLINS @ & VAVONVd-VNVYNGNVN AO ADOTOUD AHL iS] -) [ee i ae (No > + e} me) re 2 I) 6) c @ re) 0 E 6 Le INTRUSIVE IGNEOUS ROCKS QUATERNARY |[~L™] Alluvium ———— Fault definite 8 Microdiorite & andesite ETs4 Basalt TERTIARY a 9 1S e 2 £ a J 10) Le 9 a Q 9 s c 25: 52- 52: O7- O7- 56 45 45 38 38 15 15 58 58 33 33 42 42 01 01 17 17 40 40 03 03 13 13 53 53 56 56 28 28 00- 32°! “59 03> 15- 05: 50: 05> Parallax r actors S 014 —2-87 066 —2-70 008 —2-33 009 —2-24 042 —2-16 000 —2-13 039 —2-12 005 —2-21 008 —2-25 028 —1-81 004 —1-83 015 —1-88 017 —1-93 006 —1-99 030 —2-14 052 —2-23 009 —2-32 008 —2-42 017 —2-50 021 —2-63 034 —2-68 004 —2-81 008 —2-88 265 i ce a S de Oo pd oO wt gH 572 573 574 575 576 577 578 579 580 581 582 Star Depend. 5631 0: 348535 5676 0- 281006 5689 0-370460 5659 0-339322 5694 0- 230320 5646 0:430358 5533 0: 247544 5550 0: 348056 5566 0-404400 5541 0-387559 5557 0:414760 5571 0-197681 5514 0- 246458 5525 0: 542316 5533 0- 211226 5511 0-324491 5531 0-483180 5541 0-192329 5398 0: 249288 5412 0-444343 5419 0- 306369 5394 0-368814 5399 0- 236338 5434 0-394848 5353 0-397420 5373 0-352500 5385 0+ 250079 5354 0-308307 5371 0- 287463 5376 0: 404230 5365 0: 279424 5369 0:456096 5378 0- 264480 5351 0+ 228134 5376 0-537033 5377 0- 234832 5802 0-391560 5824 0:446737 5834 0: 161703 5818 0:545149 5819 0: 181263 5822 0: 273588 5768 0: 287014 5782 0: 409896 5739 0- 303090 5770 0+ 242354 5778 0-394268 5784 0- 363378 5713 0-461428 5733 0:178241 5767 0:360331 5760 0- 194840 5719 0-519972 5727 0+ 285188 5614 0: 284582 5617 0:365472 5646 0: 349945 5618 0-333319 5622 0: 424064 5639 0: 242617 5565 0: 263546 5583 0-408502 5599 0-327952 5566 0-394709 5587 0-302812 5609 0-302479 W. H. ROBERTSON TABLE II No. 598 599 600 601 603 604 Star 12833 12857 12901 12817 12882 12893 12812 12833 12871 12797 12808 12901 12751 12824 12847 12785 12808 12833 12642 12705 12723 12635 12725 12730 12306 12309 12369 12280 12326 12402 11383 12256 12280 12203 12227 12309 12161 12225 11279 11222 12163 12241 11157 11196 12122 11170 11229 12105 11073 11136 11157 11097 11170 12078 11037 11073 11136 12039 11098 11157 11037 11073 11136 11036 11170 12039 Depend. -393972 -330118 -275910 -305524 -515288 -179188 -401846 -379492 218662 237698 426162 336139 -301150 *428658 270192 308240 -470998 - 220762 -309514 -321392 -369094 -378195 -312489 -309316 - 297864 - 288936 -413200 -318210 -325256 - 356534 - 272690 -420234 -307077 -330546 - 225400 -444053 - 294550 - 297430 -408021 -313076 - 290948 -395977 - 282036 - 308820 -409144 » 223273 -321429 -455298 -304314 -430860 - 264826 -430934 - 208796 - 360270 - 239062 - 374020 386918 -355332 -492014 - 152654 °375544 - 263126 -361329 -485078 -307852 207070 PRECISE OBSERVATIONS OF MINOR PLANETS TABLE II—continued No. Star Depend. Ieee Dee: 605 11036 0:357081 36-298 03-14 11073 0: 289980 25-956 55-99 11136 0-352939 01-040 17-36 606 11037 0-348352 39-960 46-28 11098 0-187514 55-075 58-06 11114 0-464134 12-473 07-17 607 11037 0-278705 39-959 46-28 11114 0-447774 12-474 07-18 11132 0-273521 43-446 55-51 608 11043 0-308539 17-036 06-73 11073 0-359078 25-956 55-99 11161 0-332383 21-442 58-17 609 11132 0-378674 43-449 55-51 11157 0-324511 56-582 08-58 11215 0:296815 20-105 31-17 610 11098 0:304018 55-074 58-08 11178 0-394725 02-088 54-45 11212 0-301257 47-076 05-89 611 11170 0-343750 02-887 06-83 11212 0:330676 47-076 05-89 11250 0-325574 47-615 11-32 612 11183 0- 253604 18-644 00-52 11196 0-500831 36-887 18-51 11270 0- 245565 27-476 15-88 613 8117 0-325699 20°717 17-65 8151 0- 274892 51-715 61-94 8157 0-399409 17-270 13-28 614 8135 0:474442 05-371 26-63 8142 0-323324 44-445 17-08 8153 0+ 202235 28-162 38-62 615 8157 0-320436 17-270 13-27 8167 0-460834 16-766 22-56 8170 0-218730 08-198 08-18 616 8151 0-301192 51-715 61-95 8160 0-231210 17-244 24-10 8176 0-467598 27-946 28-30 617 8160 0: 162434 17-244 24-10 8167 0-500150 16-766 22-56 8190 0-337416 29-308 28-60 618 8157 0- 259918 17-272 13:27 8171 0-287416 15-271 23-51 8183 0-452666 00-649 33-22 619 8171 0-326676 15-271 23°51 8176 0:423162 27-950 28-29 8204 0: 250162 20-898 13-27 620 8160 0: 256243 17-244 24-10 8182 0-479436 43-594 30-32 8191 0- 264321 31-388 14-97 621 8171 0-336718 15-272 23-51 8182 0:379441 43-594 30-32 8196 0: 283842 21-985 07-55 622 8175 0-319878 55-613 10-67 8176 0- 255540 27-952 28-29 8197 0-424582 26-225 59-44 623 8171 0: 291126 15-272 23°51 8191 0-306490 31-388 14-97 8654 0: 402383 16-954 50-82 624 8168 0-312117 37-313 14-19 8190 0-331462 29-310 28-60 8655 0-356421 48-666 25°21 625 8636 0- 285357 56-662 23-84 8655 0-297258 48-667 25-21 8175 0-417385 55-614 10-67 626 8168 0+ 224434 37-313 14-19 8640 0-423070 01-157 54-01 8654 0-352496 16-954 50-82 No. 627 628 629 630 631 632 633 634 635 639 640 641 642 643 644 645 648 Star 8614 8618 8648 8624 8625 8630 8579 8589 8610 8576 8599 8600 9648 9653 9688 9646 9673 9680 9618 9638 9646 9623 9635 9653 9581 9624 9586 9576 9603 9611 9576 9581 9593 9568 9602 9572 9544 9568 9576 9549 9581 9565 9549 9550 9572 9544 9552 9576 9546 9562 9576 9544 9550 9584 6129 6141 6153 6124 6158 10595 6093 6124 6145 10572 6118 6144 Depend. - 323662 - 380040 296297 -411920 > 260528 -327552 - 342594 -375038 - 282368 -400132 - 190440 -409427 -374056 » 262272 - 363672 *333553 -398395 - 268052 -391804 245196 - 363000 440378 » 253212 - 306410 264499 375896 -359605 -287913 -419565 - 292522 -376900 -357064 - 266036 -312091 -402534 » 285375 -391580 - 279230 -329190 - 365479 - 281505 -353016 -445695 - 326266 > 228040 -524179 » 254154 » 221667 -271188 -504704 - 224108 -332245 -361820 - 305935 -440260 -309546 - 250194 - 324998 -380342 - 294660 252481 417203 -330316 - 276440 - 503346 - 220214 qooocqooqocoqcqoqoooqoqooqocoooeoeocoooqooeqooqooooconoo Soo qo qqooqooooqoooooo oc ooo°oo oc Ooo 2 ooo -358 -399 -031 -674 -658 -597 *321 -714 -730 -854 -365 -968 “179 -916 -224 -704 -192 - 267 -053 -099 - 704 -744 -720 -916 -690 -325 -706 -320 -998 -868 » 249 -690 -543 -698 55: -919 -491 -698 - 249 - 256 -690 -121 » 256 771 -919 °438 - 662 -321 -094 -986 *322 °438 erga | -689 °217 -466 -746 - 684 +925 -968 -675 -684 -360 -879 -408 -536 458 267 268 No Star Depend. 649 6066 0-385044 6107 0-302211 6108 0-312746 650 6073 0: 442580 6118 0: 278696 6090 0- 278724 651 6052 0-313954 6062 0-315824 6092 0-370222 652 6050 0- 486394 6089 0- 338008 6083 0- 175598 653 6021 0- 363988 6052 0-389477 6059 0+ 246535 654 6025 0-331616 6066 0- 336716 6034 0+ 331667 655 5976 0: 358294 5982 0- 380350 6008 0- 261356 656 5983 0-412610 5985 0-391202 6007 0- 196188 657 5947 0-353042 5951 0- 341652 5984 0-305306 658 5941 0- 403667 5967 0- 194898 5971 0-401434 659 5252 0-391539 5282 0+ 302702 5285 0-305760 660 5246 0-340014 5290 0- 214459 0 *445527 R.A. 21 06: *459 23° * 642 -480 *775 -951 -408 *757 -068 -020 -598 -539 Oud “415 °831 - 069 -104 -049 -642 “927 -341 - 286 - 282 -036 »245 - 220 26: 54: -548 *351 -742 -950 -531 -643 *355 363 872 928 Tot W. H. ROBERTSON TABLE II—continued 29. eed 24: 59- 54: 23° No. 661 662 663 664 665 666 667 668 669 670 671 672 Star 5232 5233 5255 5236 5244 5254 5216 5224 5236 5217 5218 5239 5191 5200 5220 5185 5202 5213 5182 5185 5213 5165 5200 5202 5158 5188 5191 5165 5168 5199 5182 5204 4893 5168 5202 4909 Depend. R.A - 232156 28-239 - 293770 29-641 -474074 17-975 237775 12-827 -538307 11-052 - 223918 32-148 224696 46-447 -485041 07-247 - 290263 12-827 - 289978 04-325 385722 21-365 324300 48-676 315439 16-094 397229 19-508 287332 53-969 362944 33° 225 - 263002 02-271 -374054 21-006 -397413 57-605 291532 33° 225 -311055 21-006 - 253937 05-079 - 346268 19-509 -399795 02-271 433378 03-887 -301507 47-717 -265115 16-095 -325186 05-079 -428142 40-643 - 246672 16-576 - 287214 57-605 - 298250 35-701 -414536 08-901 - 382890 40-643 » 222848 02-271 - 394262 48-854 ooooco°o eqoqoqaooooooo ooo ooo o oOo oc ooo coe oe A Abstract of Proceedings, 1964 : Albert, Adrien—Liversidge Research Lecture— Heterocyclic Chemistry, and Some Biological Overtones F us Bs a Annual Report, 1965 ‘ Annual al England Branch Astronomy 121, 133, Average Forces’ in Lossy Electromagnetic Systems, by W. E. Smith = Be B Bailey, Victor Albert—Obituary Bardsley, John Ralph—Obituary Braidwood, N.S.W., The Big Hole at, by Je N. Jennings ; C Canowindra East Area, The gee of, by W. R. Ryall ae Citations ‘ Clarke Medal for 1965 . Be ane =e Clay Mineralogy of Some Upper Devonian Sediments from Central New South Wales, by John R. Conolly .. ‘ Conolly, J. R.—The Stratigraphy of the Hervey Group in Central Western New South Wales Coombs, Frank Andrew—Obituary ee Coonabarabran-Gunnedah District, The Mesozoic Age of the Garrawilla Lavas in the, by J. A. Dulhunty ce Cracow District, Queensland, The Marine Permian Formations of the, by Robin Wass Current Trends in Solid State Science, by Frederick Seitz D Double Stars, Photographic Observations of, by iP. Sims Dulhunty, J. A.—The Mesozoic Age of the Garra- willa Lavas in the Coonabarabran- Gunnedah District E Edgeworth David Medal for 1964 a Electromagnetic pee Average Forces in Lossy, by W. E. Smith 12 Financial Statement Forman, Kenneth Phillip—Obituary Fynn, Anthony Gerard—Obituary G Geological Survey, N.S.W., The Foundations of the, by Ann Mozley .. Re H Hamilton, J. D.—Petrography of Some Permian Sediments from the Lower Hunter pee IN-O: Wis. : Hervey Group in Central Western Nev ew South Wales, The Stratigraphy of the, by J. R. Conolly Heterocyclic Chemistry, and Some Biological Overtones, by Adrien Albert Page 183 11 181 191 263 151 192 192 215 169 194 194 91 INDEX Holman, Mollie David Medal for 1964 : Humphries, J. W.—Some Units and Standards of Weights and Measures J James Cook Medal for 1964 Jennings, J. N. NeS AW: 2: L Late Quaternary Coastal Morphology of the Port Stephens-Myall Lakes Area, N.S.W., by Bruce G. Thom Laterites in the National Park Area, Radioactive, by I. A. Mumme : Lemberg, Max Rudolph—Award of the James Cook Medal for 1964 Lepidopteris Madagascariensis Carpentier (Pelta- spermaceae), by John A. Townrow Liversidge Research Lecture, by Adrien Albert. Lower Hunter Valley, N.S.W., Petrography of Some Permian Sediments from the, by J. D. Hamilton M McCarthy, F. D.—Award of the Society’s Medal for 1964 pd McKern, H. H. CG -volanie Oil ane Plant Taxonomy Mackerras, M. Josephine—Award ‘of the Clarke Medal for 1965 Mandurama-Panuara, The ‘Geology of, by Ree. Smith Marine Permian Formations of the Cracow District, Queensland, The, by Robin Wass Medals, Memorial Lectureships and Prizes Members of the Society, April, 1965 Mesozoic Age of the Garrawilla Lavas in the Coonabarabran-Gunnedah District, by J. A. Dulhunty ‘ Mineralogy of Some Upper ‘Devonian Sediments from Central New South Wales, Clay, by John R. Conolly Minor Planets Observed at “Sydney Observatory During 1964, by W. H. Robertson Mozley, Ann—The Foundations of the Geological Survey of New South Wales : Mumme, I. A.—Radioactive Laterites in the National Park Area Myall Lakes Area, N.S.W., Late Quaternary Coastal Morphology of the Port ee by B. G. Thom : N National Park Area, Radioactive Laterites in the, by I. A. Mumme os Note on the Stratigraphy of the Devonian Garra Beds of New South Wales, by D. L. Strusz. O Officers for 1965-66 101 85 . Inside Back Cover 270 Pp Permian Sediments from the Lower Hunter Valley, N.S.W., Petrography of Some, by JD: Hamilton : Petrography of Some Permian Sediments from the Lower Hunter Valley, N:S3W.; by Jv D: Hamilton Photographic Observations ‘of Double Stars, by K, P. Sims sad Plant Taxonomy, Volatile Oils and, by eis (© McKern Pollock Memorial Lecture for 1965 5, by F, Seitz. Port Stephens-Myall Lakes Area, N.S.W., Late Quaternary Coastal Morphology of, by BG: Thom Precise Observations of Minor Planets at Sydney Observatory During 1963 and 1964 Presidential Addresses : Some Units and Standards of Weights and Measures, by J. W. Humphries ‘ The Mathematical Sciences in the Changing World, by W. B. Smith-White ; Volatile Oils and Plant Taxonomy, by Eig 6G... MekKern f fs R Radioactive Laterites in the National Park Area, by I. A. Mumme Robertson, W. H.— Minor Planets Observed at Sydney Obser- vatory During 1964 Precise Observations of Minor Planets at Sydney Observatory During 1963 and 1964 fi Ryall, W. R.—The Geology of the Canowindra East Area, N.S.W. me + Ss Section of Geology, Abstract of Proceedings Seitz, Frederick—Pollock Memorial Lecture for 1965—Current Trends in Solid State Science 189 1oT, Sims, K. P.—Photographic Observations of Double Stars Smith, R. E.—The Geology of the Mandurama- Panuara. Smith, W. E. Average Forces in - Lossy Electro- magnetic Systems Smith-White, W. B.—The Mathematical Sciences in the Changing World we ; Society’s Medal for 1964 .. ‘ Some Units and Standards of “Weights and Measures, by J. W. Humphries Somerville, Jack Murielle—Obituary_ . Stratigraphy of the Hervey Group in Central New South Wales, by J. R. Conolly : Strusz, D. L.—A Note on the Stratigraphy of the Devonian Garra Beds of New South Wales Sydney Observatory T Thom, Bruce G.—Late Quaternary Coastal Morphology of the Port Stephens-Myall Wakes Area, N-SsWiine Townrow, John A.—On Lepidopteris Madagascar- zensts Carpentier (Pelataspermaceae) U Upper Devonian Sediments in Central New South Wales, Clay Mineralog By of Some, by John R. Conolly V Volatile Oils and Plant Say” We Hie McKern Ww Wass, Robin—The Marine Permian Formations of the Cracow District, Queensland , Weights and Measures, Some Units and Standards of, by J. W. Humphries oe 121, 133, Page 121 239 151 145 195 139 193 37 85 263 23 203 eee 139 ari Sais XS : / < rs Fr heyy ty on oN i Hl BEL hey aa rae *% il se alte | ue i Ny i H Hs - A ae f m ' ae Ne i | 4 k wept i far ed DA ap nigcate, | : s ae ee ‘ “te iveres ge await Sake rtm AO posite SS al at Sallie Z ja Shiny © S “2 pera Pere Abe pe id eet fe aa ; & 4 a f. Re ete Of, Log! y ij ne Ge 2 Pee cee a een oes aa i be Oy Beas heat 3” Sy, os et Cee A Ay ntl AE Pana se a ao ee at ae, Pi: eat TIN fF eee te et ee it SpuTvacta ee ‘ee } | 5] INTE SEH ; ee | Hd 0 wet ons Ay ty if PEs feds YE ar On Fa, 1, oe 0, Bed al te ere ys ‘i ae H pen / >, 5 ? erste : Per abt at ok eae eit ae 2a ape] il ty | 4 " WO sie fi Tem | ‘a ily ti Che se Ear pcan fe e my. i LP as +H at att AS F gaEd 2 v4 Ps fisew Pa Ea wpe * si! as OF ry petra = acter tae ert At ¥ a se rs SrA ai te S “a te az, “St ~ peer at sie y? 4 NER Pina gas, vd a be “ay ae a i 4 | ih : a ne eT ae aid eine oe “Sigal ani ait: ca 8 nga ae eu el: ES ly tapi ao se ath bstd ; eh Ee Le : ere ae 3 i Bt Mrs sien ai Sy ay) ve “enon ec yi ; i a oa Bolt ty [cle site KE feet as ALE. GES oe cos ta ~ eg eet Ne e iNce ieee, iB gs “ei Bras oy BEE Mlhin Ft BS loeb fey, Be Pe EE, ey pe pe sel? co Net es SMITHSONIAN INSTITUTION L| TT, 308 4801 YB Pa ihe eT 2h Fork aa! La