VOL. 77 JULY 1954 ee oo TRANSACTIONS OF THE ROYALE SOCIETY OF SOUTH AUSTRALIA INCORPORATED CENTENARY VOLUME ADELAIDE PUBLISHED AND SOLD AT THE SOCIETY’S ROOMS KINTORE AVENUE, ADELAIDE Registered at the General Post Office, Adelaide, for tranmission by post as a periodical VOL. 77 JULY 1954 TRANSACTIONS OF THE ROYAL SOCIETY OF SOUTH AUSTRALIA INCORPORATED CENTENARY VOLUME ADELAIDE PUBLISHED AND SOLD AT THE SOCIETY’S ROOMS KINTORE AVENUE, ADELAIDE Registered at the General Post Office, Adelaide, for tranmission by post as a periodical ROYAL SOCIETY OF SOUTH AUSTRALIA INCORPORATED OFFICERS FOR 1953-1954 Patron HIS EXCELLENCY AIR VICE-MARSHAL SIR ROBERT GEORGE K.B.E., C.B., M.C. President J. K. TAYLOR, B.A., M.Sc., B.Ag.Sc. Vice-Presidents R. V. SOUTHCOTT, M.B., B.S. S. B. DICKINSON, M.Sc. Secretary Treasurer L. W. PARKIN, M.Sc. H. M. HALE Editor I. G. SYMONS Librarian Programme Secretary N. B. TINDALE, B.Sc. T. D. SCOTT, B.Sc. Members of Council D. C. SWAN, M.Sc. S. J. EDMONDS, B.A., M.Sc. M. F. GLAESSNER, Ph.D., D.Sc. C. M. DELAND, M.B., B.S. C. G. STEPHENS, D.Sc. Auditors F. M. ANGEL N.S. ANGEL CENTENARY MEETING OF THE ROYAL SOCIETY OF SOUTH AUSTRALIA The Centenary Meeting was held in the Mawson Theatre in the University of Adelaide, on 24 September 1953, in the presence of the Society’s Patron, His Excellency the Governor of South Australia, Air Vice-Marshal Sir Robert George, K.B.E., L.B., M.C., and Lady George > VP, CENTENARY OF THE SOCIETY By S. B. Dicx1nson* President of the Society On this occasion of the centenary of the foundation of the Royal Society of South Australia it falls to my lot as President to extend to Your Excel- lency a cordial and warm welcome. We are honoured to have you as our patron and we also bear in grateful memory the services which have been rendered by your predecessors. We are equally delighted and honoured that Lady George has been able to attend this historic meeting. We welcome the Hon. R. Rudall, Minister of Education, representing the Government which has given the Society its support over many years. I also welcome the representatives of kindred societies and other scien- tific bodies and the many distinguished scientists who have honoured us with their presence. Messages of greeting have been received from: The Royal Society of London; The Linnean Society of New South Wales; The Royal Society of Australia; The Royal Society of New South Wales; The Royal Society of Victoria; The Royal Society of Western Australia; The Royal Society of Tasmania; The Royal Society of Queensland. On an occasion such as this, when the Royal Society of South Australia has completed a century’s honourable service to the community, something different, it seems, should be said, something in recognition of the special occasion. We have great cause to be thankful that our Society has been permitted to survive the full span of 100 years. We are thankful for the honoured place ' it holds in the community, for its friendly association with its kindred scien- tific societies, for its achievements. Many of its fellows have gained high renown. It is natural on this occasion to let our minds wander back and think of our beginnings when the Society was originally launched on its voyage on January 10th, 1853. On that day five prominent Adelaide citizens met together to organise learned discussions on subjects connected with literature and art. At this meeting the Adelaide Philosophical Society was formed, which later became the Royal Society by merely a change of name. I do not intend to say anything about our early history, as much on that subject will be found meticulously recorded in past numbers of the Trans- actions™, except to remind you that our originators, besides pledging them- ~ ©) R. S, Rogers—“A History of the Society, particularly in its relation to other Institutions in the State.” Presidential address, Transactions and Proceedings of the Royal Society, 46, 1922. C. T. Madigan —"“The Past, Present, and Future of the Society, and its relation to the Welfare and Progress of the State.” Presidential address, Transactions and Pro- ceedings of the Royal Society, 60, 1936. * S. B. Dickinson, M.Sc., Director of Mines, South Australia. en ee il selves to the promotion of public interest in literature and art, also dedicated themselves to the pursuit of scientific knowledge. This association of scien- tific and literary interests was perhaps the most outstanding feature of our early beginning. A more enlightened objective can scarcely be put forward today when it is becoming more and more apparent that education and cul- tural interests need to include something of science as well as of literature. With these noble aspirations it 1s no wonder the Society grew and flourished. In the year 1880 Her Majesty Queen Victoria graciously acknowledged the Society by becoming its Patron. Her Majesty also approved the Society being styled the Royal Society of South Australia. This title is one of our most precious possessions, To us it implies a direct association with the Royal Society of the United Kingdom, and with it the inheritance of a great name and great responsibilities. We acknowledge gratefully the continued patronage accorded to us by your Excellency. Jt preserves this link with the Mother Country, with the Royal Societies of the British Commonwealth, and the traditions and work which have won the respect of the scientific world. In these brief introductory remarks I have not sufficient time to bring to your attention the many achievements of the Society. Neither is it pos- sible for me to pay tribute to the many fellows, both past and present, whose energy and devotion to the pursuit of truth have built up the Society’s treastire house of knowledge. From the subsequent addresses, however, I feel you will gain a clear concept of the debt we owe to our members, who during the past 100 years have given worthy intellectual and scientific guid- ance to the people of South Australia, Tt is difficult for the man of the world to understand the altruistic spirit which induces men of science to band themselves together in societies having for their sole aim the advancement of knowledge in particular directions; and in very many cases sacrifice their leisure, and draw upon their limited resources, not only that knowledge may be increased, but also that the gain may be published to the world, which is free to make use of it; yet such is the case. The publications of otiginal scientific work by the society have been continuous for 76 years and are to be found on the shelves of every important scientific library throughout the world. In its early years the Society participated much more prominently in public affairs than it does today. It was not uncommon for the Governor of the State to occupy the Chair, and for the Chief Justice, the Judges, the Surveyor-General, the Postmaster-General, and leading educationalists and newspapes editors to engage in lengthy discussions and present reports on matters relating to development of the Colony. Actually it was the only body in the country, at that time, which could speak with any authority on matters of education and pure and applied sciences. The old Society was thus the forerunner of many of our public institutions and of nearly all the scientific bodies which have arisen since. It played a major role in the establishment of the Public Library, the Museum, and the Art Gallery. Its efforts led to the establishment of many of the Government departments. It was prominent in the original movement for the establishment of the University in this State. It is thus fitting that we should be celebrating this historic occasion within the University. I desire to express our thanks to the Chancellor, the Vice- Chancellor and members of the staff of the University for their undiminished support of our efforts. It has aided us immensely in living up to our professed objective—the advancement of knowledge. iil With the establishment of the educational institutions in the State, especially the University, the interests of the Society gradually turned to essentially scientific pursuits. Professor Ralph Tate, the first Professor of Natural History in the University, became the soul of the Society during these transition years. Besides encouraging original work, an equally strong desire prompted him to spread scientific knowledge and promote its general use by the ordinary citizen. His untiring efforts led to the establishment of the Field Naturalists’ Section of the Society, which encourages the study of natural history essentially as a hobby. This Section has become a very active body. Its efforts in collaboration with those of the Fauna and Flora Pro- tection Committee have been responsible for much of the legislation relating to the protection of ainmals and plants and also for the establishment of our National Parks. In its career of scientific endeavour, which we may date from the foun- dation of the University, the Society may properly claim to have done out- standing service. It makes one award for distinction in scientific work and that is the Sir Joseph Verco Medal. Sir Joseph Verco was one of the greatest workers and most outstanding personalities in our later history. The award is made at such times as the Council considers there is a worthy recipient. They have been made to Professor Walter Howchin, Mr. J]. M. Black, Sir Douglas Mawson, Professor J. B. Cleland, Professor T. Harvey Johnston, Professor J. A. Prescott, Mr. H. Womersley, Professor J. G. Wood, Dr. C. T. Madigan and Mr, H. M. Hale, whose names are prominently recorded in our annals of science. Throughout its career the Society has been materially assisted by the Government of the State in many ways, and continues to enjoy its support. The annual Government grant largely provides the means of publishing the results of investigations. For such Government assistance the Council is truly grateful. In conclusion I would like to strike a note of dedication. Every conquest of science brings the human race nearer the day when it will have complete control over the forces of nature and be able to use them for its own purposes. I think it is obvious to us all that we have now moved into an era in which science can be no longer regarded as something extraneous or additional. On the other hand, it has become an essential part of our everyday life. There must therefore be no resting, satisfied with achievements, but persistent endeavour. Success in the discovery of new natural facts and relationships, however, is not enough. Whether good or evil uses are made of these discoveries depends on the aims and character of the community, rather than upon the studies themselves. ~ I would therefore urge the Society towards a new outlook of service to the community as well as to science itself. What is more urgent now is to integrate scientific work and human needs and to do something to lessen the gap of ignorance between the scientists and the public—a gap that is widen- ing as scientific specialisation proceeds, Let us hope that the Society will have an even greater influence in the future than it has had in the past 100 years in this country of ours. lv THE BIOLOGICAL SCIENCES By Wititam P. Rocers * The body of knowledge which we call the biological sciences covers a wide field; it embraces a complex of interrelated disciplines. Until recently it was convenient to divide these disciplines into two groups. One, descrip- tive biology, included such subjects as morphology, natural history and taxonomy. The other was called experimental biology and covered such subjects as ecology, genetics and physiology. But today this type of distinc- tion between the different biological sciences is going. ‘There is now, for instance, a branch of biology known as experimental morphology; at one time the two words would have been regarded almost as contradictory, The systematist, once regarded as a completely descriptive biologist, cannot even grasp the significance of his fundamental unit, the species, if he has not an understanding of ecology and genetics. And, in turn, both these sciences are Jargely based on an understanding of physiology. The modern division of biology is not so much between experimental and descriptive biology but rather between analytical biology and its opposite. This distinction is tnportant; the major contributions in modern biology, however diverse they may be, have certainly been made by the analytical treatment of biological problems. It is difficult to define non-analytical biology. In Medawar’s words, its field “is hardly yet coherent enough to have earned itself a special name, but the distinction is partly co-extensive with the antithesis between vitalism and mechanism, and yet again with the antithesis between Lamarckism and selection theory.” Indeed, Medawar considers that, “the threefold belief in vitalism, holism and the inheritance of acquired characters, combined with an active detestation of mathematical analysis is a syndrome which has now acquired an almost clinica] dignity.” This, I think, is the best way to regard non-analytical biology. In the history of biology in any country we see first the growth of descriptive biology and later, its merging with experimental biology which, in its broader aspects, becomes analytical biology. This is the typical and proper growth of biological science and we see something of this sort of development in the papers of the Proceedings and Transactions of the Royal Society of South Australia. The descriptive phase gives us the anatomy and classification of the plants and animals of this State. Later, with this know- ledge as background, the examination of the relationships of the organisms with one another and the environment began and publications in ecology appeared. At this stage, interest in physiological and genetical investigations also developed. As our knowledge of biology passes through these phases it loses more and more of its local character and becomes, part of general biological science without particular geographical significance. The history of biological science in South Australia was fully discussed by several speakers on the occasion of the centenary of South Australia in 1936. In particular, the late Professor Harvey Johnston looked back over our publications in zoology. Professor J. G. Wood chose rather to look forward and ended his address with a discussion on the role of plant physiology. I will not attempt to review the matters so ably discussed on that occasion. Rather I would like to discuss what I think would be the most fruitful way in which biological sciences should develop here in the future. * Professor W. P. Rogers, Ph.D., University of Adelaide. v I suggest that problems should be investigated not only for their local interest, but largely with the view that such investigations can make valuable contributions to biological science in general. Two examples from investi- gations in animal biology already carried out here will show what I mean. In a C.S.I.R.O. laboratory, under the leadership of Mr. H. Marston, what was first a problem in the biology of ruminants of particular signifi- cance in South Australia has developed into a study of importance the world over. Thus a problem arising from the deficiency of cobalt in certain pastures of South Australia has developed into a problem in the metabolism of vitamin B,,. In the University, Dr. W. R. Adey has been studying the anatomy and physiology of the marsupial brain. The marsupial is an animal which is almost exclusively Australian and thus this work had initially a particular local flavour. But the results obtained have a very wide significance and throw light on the cortical perception of deep-seated sensations in mammals generally and thus are of importance in the general field of animal biology. If this sort of pattern of development of biological science is to be fol- lowed in South Australia, what are the chief investigations which have local significance and yet would have an important bearing on biological science in general? In animal biology, I think that these problems are fairly obvious. The first deals with animal ecology. We have in South Australia ecological problems which are almost unique and the solving of these prob- lems will have important repercussions in the general field of ecology, The climate and terrain, the animals and plants in many parts of South Australia are such that investigations can lead to clear cut results which could not be obtained in the more complex ecological conditions which prevail in many other countries. In fact, 1 believe that the investigation of these problems js something of an obligation; the problems are ours and we have a particular responsibility to examine them. The second field of investigation that I think we should take pains to encourage is that of biology of the marsupials and monotremes. Here we have a host of problems which are peculiarly Australian but the solving of them would be of great importance in gaining a fuller understanding of the higher mammals. The early biologists in South Australia have recognised these problems and much fine work on the anatomy and natural history of the marsupials has already been published. But the study of the physiology of these animals has hardly been attempted, Admittedly the problems are difficult but that only serves to make our responsibility the greater. You may perhaps wonder why I should, at this centenary meeting of the Royal Society of South Australia, give so much emphasis on the matter of future development of biological science in this State. It is because I feel very strongly that the Society should take a more active part in encour- aging the development of biological research. In the past the Society has played an important but somewhat passive role; it has provided a meeting place where people could discuss their work and has provided a journal in which results could be published. It has initiated many schemes which have aided the development of science in South Australia. In this way it has given outstanding service in assisting science, particularly in the early years of South Australia, but in the future, particularly in relation to academic biological research, I believe that it has an even more important and active part to play. To give you the premises on which I base this suggestion I must briefly review the changes which have occurred in biological science generally since the activities of the Society were reviewed in 1936. Since that time two inter-related factors have had considerable effects on the development vi of biology. These factors were the growth, or rather the practice of certain extreme political philosophies and the war of 1939-1945. Both these factors have led to an increased pressure on biology, both from the “philosophical” and technicological points of view. It has become clear that the distortion of biological science to serve particular brands of political philosophy can have most unfortunate effects, and, indeed, can lead to the undermining of fundamental importance of fac- tual evidence on which science is built. It is of course unlikely that circum- stances in Australia will change and that science here will have to suffer the indignities that it has in some countries. Nevertheless, bodies such as the Royal Society of South Australia, which are devoted entirely to the further- ance of scholarship and research now have an increased responsibility in preserving the independence of scientific thought. Now let me consider the effect of the war on the technicological devel- opment of biological science. During the war the scope of applied biology was suddenly expanded into a wide variety of previously unconsidetred fields. Biologists took part in the development of operational research; air, tank, and submarine crew physiology became important fields of investigation ; entomologists worked with the troops in many forward areas, Parasitolo- gists, particularly from America, moved from their laboratories and applied their knowledge to practical matters in the field. Biologists became involved in the researches of biological and chemical warfare. There was a wide recognition of the part biology can play in practical matters and this has led to an increased pressure on the application of biology for economic purposes. In those fields of applied biology such as agriculture and medicine which have been so important in the development of mankind, the importance of fundamental research has been recognised and efforts have been made to maintain a basis of fundamental knowledge on which application depends. But I fear that the application of biological science to economic problems generally may soon, if it has not already, outstrip our fund of basal informa- tion, and become even more empirical than it has been in recent years. If we are to keep a proper balance between applied and academic biological research, the increased support for applied biology should be paralleled by an increased support for academic investigations. I have in this discussion somewhat exaggerated the division between applied and fundamental biology. As far as the more able biologists are concerned, this distinction does not really exist. The biologist studying the economic problem usually has to return continually to the fundamental aspects if he is to solve his economic problem. But in many parts of the world those on whose support biologists are dependent for the wherewithal to carry out their work frequently make an undue and false distinction between what is “useful” biological research and what is not. It is here again that I think events have thrust increased responsibilities on learned societies as supporters of academic research. The success of the Royal Society of South Australia during the next century of its history may well depend upon the vigour with which it upholds the independence of scientific thought and the value of scholarship in scientific research, vii AGRICULTURAL SCIENCES J. A. Prescott * In the early years of any organization such as a learned society a great deal of interest is usually taken in the “Arts” as well as the “Sciences,” and by the arts we understand all those branches of human activity which demand some special personal skill whether this be handling the plough, painting a picture or producing a fire by rubbing two sticks together. It is appropriate therefore that the early records of the Adelaide Philosophical Society should have included a number of papers on agriculture which dealt with such mat- ters, on the traditional level of the art, as the fertility of soils, the drying of fruits, the preservation of meat, viticulture and the fermentation of grape juice, all of which subjects had already acquired a skill based on long tradition and experience in overseas countries. The science of agriculture was to come later, first in its efforts to explain traditional practice and later, by research, to enlarge the basis of knowledge on which the art itself could be developed. In a young country such as Australia, traditional experience sometimes breaks down or is of no avail and research becomes in fact, as no doubt it has always been, an art itseli—that of manufacturing experience. C. T, Madigan in his presidential address in 1936 to celebrate the Centenary of the State recorded that the word “Arts” was quietly dropped out of the interests of the Society when the rules were revised in 1902. In dealing with the development of agricultural science in South Aus- tralia the Society contributed notably through the awareness of one of its Presidents, E. H. Rennie. In two presidential addresses, those of 1889 and 1901, Rennie concerned himself with the application of his own science of chemistry to the agricultural needs of the Colony and State, The land now occupied hy Roseworthy College had been purchased and established as an experimental farm in 1881 and the College itself opened in 1884 under J. D. Custance. It was under W. Lowrie’s direction from 1887 until 1901, and Rennie was in close touch with Lowrie during this period and subsequently, It was Rennie who took me to see Lowrie on his farm at Echunga when I reached Adelaide in 1924. In his address of 1889, Rennie concerned himself with the reputed decline in wheat yields in relation to soil exhaustion. He referred to the need for conserving all materials for manurial purposes, such as wood ash, bones and farmyard manure and deplored the export of superphosphate and sulphate of ammonia from the colony which was then actually taking place. He realised, moreover, that the conservation of all possible materials of manurial value would still be inadequate. “Is it not desirable,” he said, “that experiments should be undertaken with a view to discovering what are the best methods of farming in this colony under varying conditions?” He advocated among other non-agricultural things the production of salt by solar evaporation. In 1901, when Rennie gave his second address, the agriculture of the newly formed State was passing through a critical period. Since his pres- idential address eleven years before, the average yield of wheat in the Colony had been rather less than five bushels per acre. He claimed there was a “crying need for accurate scientific investigation, such investigation being necessary, not merely to elucidate scientific theories but to improve our material condition.” He was deeply impressed by the very recent European work on nitrification and nitrogen fixation and recognised the importance of * Professor J. A. Prescott, C.B.E., D.Sc, A.LC., F.R.S., Director, Waite Agri- cultural Research Institute, Adelaide. vili using peas as a crop for raising the nitrogen level of the soil. He recalled that Lowrie was puzzled by the small responses of wheat to nitrogenous fertilisers and that he had attributed this to something that took place in the process of barefallowing. To Lowrie, the most likely process appeared to be the fixation of nitrogen by bacteria in symbiosis with algae. Later scien- tific work established, however, that the nitrification of the reserves of nit- rogen already in the soil adequately accounted for this. Scientific investigations on behalf of agriculture of the kind envisaged by Renhie had to wait, however, nearly 25 years, with the foundation of the Waite Institute by the University in 1924, Even the need for such a Federal body as the Commonwealth Scientific and Industrial Research Organization was foreseen by Rennie for he referred to the advocacy by Sir John Quick in the first Federal Parliament for an organisation similar to that of the United States Department of Agriculture. Referring to the current develop- ments in America and in New South Wales, Rennie said, “We must have similar work done here.” I have no doubt whatever that he had a great influence with the Council of the University in determining its policy when the splendid gift of Peter Waite became available for the benefit of agriculture in South Australia. Some practical problems needing urgent attention according to Rennie were the losses, failures and distresses in the irrigation settlement at Ren- mark, the depredations of insect pests, the pathology of plant diseases, dis- eases of wines and rural engineering, Apart from rural engineering, the need for which is still being discussed, the others have all been taken up at the Waite Institute either as activities of the University or of the Commonwealth Research Organization. The soil survey of Australia began in fact at Renmark. In the earlier years there were occasional papers, to the Society on some of these problems. Diseases of wheat had been discussed by the Philosoph- ical Society. In 1879, J. G. O. Tepper presented a paper on wheat rust and in 1880 on potato moth. In 1884 F. S. Crawford dealt with the disease of apricots. Samuel Dixon (1884-1892) took a special interest in native shrubs as fodder plants and in the effects of settlement and pastoral occupation on these plants, an interest later to be reflected in the work of T. G. B. Osborn and J. G. Wood at the Koonamore Vegetation Reserve and published by the Society in 1925, The first meeting of the Society which I had the privilege of attending was that of October 1924 and I recall the important paper then presented by T. Harvey Johnston on the relation of climate to the spread of Prickly Pear in Australia. This proved to be the first of a series of papers in applied climatology to be presented to the Society during the next twenty five years or so dealing with climate in relation to insect pests, to agricultural pos- sibilities and to plant introduction. Most, if not all, of this work has been contributed by officers of the Waite Institute, including J. Davidson, H. C. Trumble and J. A. Prescott and has had as its background the search for better criteria of the efficiency of the rainfall than could be provided by the crude rainfall figures themselves. This work has emphasized the importance of the evaporative power of the air in modifying the value of the rainfall and there has been a constant conscious search for criteria which would have the widest possible application. An interesting development of this work has been the study of evaporation by C. W. Bonython (1950) arising out of the need to measure the efficiency of the production of salt by solar evaporation which may be recalled was mentioned by Rennie in 1889. This work in climatology also illustrates one of the functions of a society such as ours. Climatology is the meeting ground of meteorology and geog- ix raphy. Any new principles involved in its study must be tested out against a geographical background and South Australian agriculture and biology have provided such a background, with Australia as a whole as an extension of South Australian experience. The Transactions of the Society provide the ideal medium of publication for such work and it is only at a later stage when the concepts have matured and been tested in time and can be applied with a wider geographical framework that publication overseas becomes appropriate. The most characteristic contribution of the South Australian school of climatology as recorded in our Transactions has been the establishment of criteria whereby the length of the season favourable to agricultural and pas- toral production can be determined as well as that favourable to certain aspects of insect activity. New methods of characterising temperatures in terms of the mathematical analysis of the wave form of the annual curve of mean monthly temperatures have enabled temperature regimes to be more conveniently defined and this method has been proved particularly useful in seeking parallel climatic regimes in other parts of the world, specially in relation to the introduction of new plants to Australia and in relation to the understanding of the success or failure of species already introduced. The . success for example of the Monterey pine (Pinus radiata) in South Australia is related, as was shown by J. A. Prescott and C. EF. Lane-Poole (1947), to the close parallels in many respects of the climatic regimes of the coast of Cali- fornia and of south eastern Australia. Climate is, however, but one aspect of the South Australian environment and it is natural that the two other ecological components, namely vege- tation and soils, important in biology, as in agriculture, should have received attention. . The basal information on which all vegetation studies must be based is the systematic account of all the plant species to be encountered in South Australia—those that are native and those that have been introduced. The outstanding contribution is, of course, that of J. M. Black whose 45th addition to the Flora of South Australia appeared in the volume for 1950, In another field, that of enumeration of species and in relation to their geography, J. B. Cleland has made important contributions. The first con- tribution on ecology proper—that is the relationship of plants to their sur- roundings—came in 1922 when T. G. B. Osborn published two papets in our ‘Transactions—one relating to the Franklin Islands and the second in collab- oration with R. S. Adamson, a visitor from South Africa, dealing with Ooldea on the Transcontinental railway. In 1924 there followed the account by these same two authors of the ecology of the Mount Lofty Ranges and there was then established by Osborn’s student and successor J. G. Wood and by Wood’s own students a series of contributions on the ecology of South Australia which form the basis of the understanding of the vegetation associations of the State and have further presented opportunities for testing out ecological concepts developed overseas in an Australian environment. The plant associations of many parts of South Australia are now reason- ably well established and one need mention only the work in more recent years of R. L. Crocker (1944, 1946) R. W. Jessup (1946, 1948, 1951) R. L. Specht (1948, 1951) and C. D. Boomsma (1946, 1948) to realise how much of the State has been covered. To one, like myself, who has watched this development and made frequent use of the information so obtained there is a continuous tradition starting with Goyder and his line of rainfall presented in a Parliamentary paper (1866), through the work of our Land Surveyors and land Valuers to this modern assessment of the resources of the State. It is fortunate that we have in Australia such large areas of unspoiled native vegetation, so closely dependent on soil and climate. The surveyors of this State, as of the other States, have been able to use the description of our native vegetation as an aid to land classification and this has been extended to the modern work in soil surveys. These soil surveys and other work of a more general character on the soils of South Australia have estab- lished the existence of a range of fertility levels in our native soils which can most frequently be defined in terms of phosphate content in the soil. Wood (1939) was able to demonstrate how closely the vegetation associations then recognised in the State, could be related to this level of soil fertility, to the degree of soil acidity and to the rainfall. In the agricultural development of the State, it is almost always necessary to replace the native vegetation, particularly where this is heath or scrub, by new associations of pasture plants needing a very much higher level of soil fertility. The ecological principles established in the study of our native vegetation can still be applied by the agronomist to the introduced pastures and to the crops with their associated weeds. There are still however—and we tend to overlook this—large areas of native grassland and shrub steppe where the most important problem at the moment is the management of these areas so as to maintain for all time what is in itself a yaluable asset to the State. The work of the University Schools (Botany and Waite Institute) at Koonamore and Yudnapinna should play an important part in, the devel- opment of scientific principles of pastoral management and this could be extended to the nearer pastoral country of our mid-north. The native and introduced plants provide food for a wide fauna, and the ecology of this fauna, particularly of the insects, has afforded an opportunity for a series of studies on insect ecology of which the most typical are perhaps those relating to the two grasshoppers with which we have been plagued from time to time. The work of J. Davidson (1936) and H. G, Andrewartha (1940, 1944) are outstanding examples of this kind of work, The edaphic element in the environment has been the subject of a series of papers on soils, starting with the paper by Prescott (1927) on the reaction of our South Australian soils in which the close dependence of soil acidity on rainfall was first demonstrated for the State and paved the way for further studies of soils in relation to the climate in which they were encountered. This led further to the recognition that some soils, those derived from laterite, and common in the State, owed many of their properties to conditions in the Pliocene or Miocene and our transactions include a few papers dealing with laterite. The two major soil groups, the Mallee and the Red Brown Earths were described in 1932 and 1938 and many of you may recall the extraordin- ary interest displayed by our members in a paper by C. S. Piper (1932) on the soils used in the preparation of turf wickets. Formal soil surveys are not normally suitable for discussion in our Transactions but they afford many opportunities for pedological discussion amongst which we may include the mathematical presentation of C. G. Stephens (1947) on soil forming factors. Agriculture, as crop and pasture husbandry and even as animal hus- bandry is in one sense applied ecology and there will always be a scope for the Society in dealing with the South Australian environment. In the second sense of applied physiology the opportunity is experimental rather than des- criptive and for this reason is rarely presented to or discussed in our meetings —even some aspects of climatology are now reaching the experimental] stage. in which the water needs of plants are being determined directly by experi- ment rather than deduced from observations on natural phenomena. There is still scope however for much descriptive work; our arid regions in particular, afford abundant scope for studies of soils and climate in relation to geo-morphology. In soil chemistry there is in sight the possibility of much xi work in defining the geochemical provinces of the State, particularly as the geology and particularly the petrology of the State is so much better known than was the case 25 years ago. Such studies will give a sounder chemical background to the understanding of the nature of our problems in soil fertility particularly with respect to phosphate, to potassium and to the micro elements. On the more purely ecological side I should like to see a greater devel- opment of interest in the physical properties of the soil profile, particularly the capacity for retaining useful water. These two groups of studies linking geology through the soil with the plant associations could be conveniently defined as edaphics. It is in this direction, I believe, that descriptive science will have most to offer to agriculture in the next twenty five years or so. xt THE ROLE OF GEOLOGY IN THE ACTIVITIES OF THE ROYAL SOCIETY OF SOUTH AUSTRALIA By D. Mawson * What was later to be known as the Royal Society of South Australia was initiated on the 10th January, 1853, under the title of The Adelaide Phil- osophical Society. At that time the membership was small but comprised the State Governor and most of the leading citizens of the period. Their deliberations were stated to comprise discussion of “all subjects concerned with science, literature or art.” Observations of a geological nature were in a minority in those days, During the 23 years period prior to the change of status in 1876, when it became known as the Royal Society of South Australia, geological discussions amounted to only about 10 per cent of the transactions. The first geological paper was introduced in the gold rush period, at the October meeting of 1854, That was: “The Geology of Bendigo Gold Field with speculations on the origin of the Gold” contributed by W. H. Light, who had been engaged in gold mining at Bendigo, Referring to the auriferous quartz reefs he advocated that these have a plutonic origin and “were prob- ably injected in a liquid state from great depths below into veins and crevices in the stratified rocks.” An explanation which, you will agree, is correct only in part unless we interpret his “liquid state” as an aqueous solution, The most notable contributions of that time so far as geology is con- cerned were several papers by the Rev. Tennison Woods, who was a really able geologist of that period. He dealt with fossils in the Marine Tertiary Limestones of the South East of the State. Also there was delivered by the same author a general paper on the Geology of that area. The Chief Justice, Hanson, also contributed a lengthy observation on the geology of the South East, in part intended to correct what he regarded as weaknesses in Tennison Woods’ arguments. However the latter showed the amateur geologist Hanson to be in error, By the year 1872 the Adelaide Philosophical Society had reached a very low ebb, in fact meetings were suspended for a time. There then arrived in Adelaide, in the person of Professor Ralph Tate, a dynamic character who lost no time in reorganising the Society. From thence onward, as the Royal Society of South Australia it has flourished: a very active organisation and valuable recording medium for discoveries and developments of scientific interest within the State. This advance in the status of the Society coincided with the establishment of the University of Adelaide which resulted in an accession to the community of men of scientific and literary standing. That geology should figure prom- inently thereafter was to be expected, with Professor Tate in the role of prime mover and President for some years. However, Tate was absorbed not only in Geological studies but as Professor of Natural Philosophy was required to cover Botany as well as Geology, With these two interests at heart he soon reconnoitred large areas of the State and set the foundations for the Geology of South Australia. To the time of Tate’s arrival the known fossiliferous strata were restricted to the Cainozoic Era, and in that division Tennison Woods had already pioneered the ground in the South Eastern division. Tate rapidly advanced knowledge of the nature and fossil contents of the marine Tertiary strata of South Australia, well illustrated in his series of papers published in the Royal Society’s volumes. * Professor Sir Douglas Mawson, O.B.E., D.Sc, B.E., F.R.S., University of Adelaide. xiii Tn 1875 trilobites and coral-like fossils from near Maitland on Yorke Penin- sula were submitted for identification. The latter were eventually identified as archaeocyathids, The rock formation in which they were obtained was in the first instance, referred to the Silurian Period, but was later determined as Cambrian. That discovery was however an isolated occurrence. It was not until long afterwards that Cambrian fossils were located, widely distributed in many parts of South Australia. For years Tate kept a sharp lookout for fossils in the older rocks of the Mount Lofty Ranges. He was so far unsuccessful that in 1896 he was so cer- tain that those formations would not be found to yield fossils that he wagered he would “eat my hat” if Professor T. W. E. David, then visiting Adelaide, should succeed in discovering any. A few days later David when in company with the Reverend Walter Howchin, in a field trip south of Adelaide, found fossil archaeocyathids in the limestones of Sellick’s Hill. About the time of Tate’s arrival in South Australia, Mesozoic fossils were found in the far north and it became apparent that the Great Artesian Basin extended from New South Wales and Queensland far into North Eastern South Australia. Thus it was apparent that Tate and the revitalised Royal Society were responsible for a marked advance in the study of Geology in this State. But the Society’s influence did not stop there, for in 1877 they pressed the Govern- ment to appoint a Government Geologist. It was realised that a territory the size of South Australia, then the largest section of all Australia, for it included under its jurisdiction Central Australia and the Northern Territory, must embrace important ore deposits and geological problems of great national interest such as underground water supplies. The outcome of this advice to the Government was the appointment of H.Y.L. Brown as the first Government Geologist and the initiation of the Department of Mines and Geological Survey; the latter, in these days of our present President, has blossomed forth on a grand scale. Thus it was that Tate, during his 25 years of active association with the Royal Society greatly advanced knowledge of the geology of South Australia. During the last decade of that period these advances were stimulated by another active and enthusiastic geologist who for some 40 years did yeoman service for the Royal Society as its able honorary editor. This was the Rev. Walter Howchin who had arrived in ill health in South Australia in 1882. The salubrious climate soon restored his health and he gradually took an increasing interest in local geological phenomena until in later years, after appointment as lecturer in Geology and Palaeontology at the University of Adelaide, he published “The Geology of South Australia.” Howchin dedicated himself first and foremost to the self-imposed hon- orary task of editing the Society’s volumes. In his official position with the Society and with increasing geological status, Howchin did much to maintain the geological tradition established by Tate in matters relating to the Society. Perusing the records I find that during the past 100 years about 364 papers dealing with definitely geological matters have been read before the Society. Since Tate’s time, that is in the present series of volumes, the strictly geological contributions have averaged 22% of the papers presented. During the past 30 years, scientific activities in South Australia have been greatly increased both by new developments and by expansion of existing bodies. The scientific life of our community has become more specialised. The Society no longer listens to dissertations on sewage. problems, reform- atories and education. Other bodies specialising in more limited spheres of xiv enquiry have been established. The chemists, the physicists, the engineers and the medical fraternity now all have their own organisations. However, the parent body still remains in full vitality and should always constitute a forum for students of general and fundamental science though less so for those involved in the specialisations of applied science. Our Society should not only provide a medium for the publication of the results of local scientific research, but would do well to foster a wider field of activity. It could well be the local disseminator of the latest developments in the world of science and guardian of the interests of Science in South Australia. It was in these latter roles that the Adelaide Philosophical Society functioned one hundred years ago. Many far-sighted and beneficial developments in South Australia owed their origin to the Society’s influence in matters of national importance. Thus through the representations of our Society the following developments were effected: the establishment of the State Geological Survey; the establishment of the South Australian Museum and appointment of the Director; the estab- lishment of the National Park and Flinders Chase; the gazetting of several fauna and flora reserves. In fact the Royal Society, pressing for the Govern- ment to undertake beneficial works, prompted most of the major develop- ments in the State: amongst these may be mentioned the introduction of universal Public Instruction and the Sewerage System for Adelaide. Beginning somewhat more than 50 years ago, fostered by the Royal Society, there was a period of pressure for soil and agricultural research. This undoubtedly had an influence on the establishment of the Waite Agricultural Research Institute. AUSTRALIAN NEREIDAE INCLUDING DESCRIPTIONS OF THREE NEW SPECIES AND ONE GENUS, TOGETHER WITH SUMMARIES OF PREVIOUS RECORDS AND KEYS TO SPECIES BY OLGA HARTMAN (COMMUNICATED BY S. J. EDMONDS) Summary The Australian (and New Zealand) Nereidae are recorded with 47 species in 13 genera. One genus, Anstralonereis is new; two species, Ceratocephala edmondsi and Micronereis halei, and one subspecies, Platynereis dumerilii antipoda are newly described. There are many new records of distribution, particularly for the species occurring in the Flindersian and Peronian provinces. The recorded data of all the species are summarised in a series of charts. t AUSTRALIAN NEREIDAE Including descriptions of three new species and one genus, together with summaries of previous récofds and keys to species. By Guica HartMaAn * Communicated by S. J. Edmonds [Read & May 1953] SUMMARY The Australian (and New Zealawi) Nereidae are recorded with 47 species in 13 genera. One genus, Ansiralonereis is ews two species, Ceratocephala edmonds and Micronerets halvi, and one subspecies, Platyaereis diaverili antipoda ate newly described. There are many new records, of distribution, particularly for the species occtirring in the Flindersian and Peronian provinces. The recorded data of all the species are summarised in a series of charts. INTRODUCTION The polychaetous annelids of the family Nereidae are among the more con- spicuous, well represented groups of marine invertebrates in the Commonweaith of Australia. and the Dominion of New Zealand, As in other known geographic areas, they are largely littoral. Curiously, however, the present study indicates that the nereids, at least for the southern half of Australia, are unusually diversi- hed and modified, probably more so than in any other geographic area of comi- parable size. Thus, among the 47 species in 13 genera, there are some with very primitive characters, such as presence of setae in the first segment; others, such as Australonereis, have functional coelomoducts and papillaled ventrum. These facts make it particularly desirable to recognize their positions or affinities with the nerejds of other parts. of the world. In spite of the fairly large number (47) recorded here, it can haedly be assutned that the number of species is even nearly complete. Much of the coast- line remains almost unknown with respect to its polychaetous fauna. The records ta date are largely those made by incidental collecting. There have been no extensive surveys of coastal arcas such as was done for the echinoderms (Clark, 1946), Recent. studies by Knox (1951) on the nereids of New Zealand indicate that there are conspicuous differences in the fauna of the Dominion and the Com- monvwealth, at least for its southern halt, Coimparison has been difficult in many cases for the literature is scattered and sometimes obsctire in essential details. Type collections, if existing, are often deposited in museums outside of Australia. Au attempt is here made to correlate and assemble these scattered data. Charts I to IV summarize the records of the 47 species, including: acceptable naine, date and source of original publication, place of origin, diagnostic accounts, synonyms, distributional data and new records, ecologic niche. unique charac- teristics, method of reproduction in so far as known, and the formulae of the proboscidial processes, The materials on which these studies are hased were collected mainly from littoral zones of South Australia, Victoria and New South Wales, thus are largely south-eastern Australia, These areas fall within the Peronian and Flindersian provinces of Iledley. Kased on studies of the echinoderm fauna, H. L, Clark (1946) finds that these two provinces have the most numerous endemic species (82% of the Peronian and 89% of the Flindersian echinoderms are endemic in Australiz), If the annelids are equally unique, as a comparison of the charts indicates, one may expect a widely diversified polychaetous fauna. * Allan Hancack Foundation of the University of Southern California. Contribunon No. 148, Trans Ruy Sac. S. Aust., 77, July, 1954 ? I am indebted to the following people and institutions for the collections on which the present study is based: Mr. Herbert M. Hale and associates of the South Australian Museum, Mr. S. J. Edmonds of the University of Adelaide, and Miss Barbara Dew of Cronulla, New South Wales. The Administration of the Allan Hancock Foundation of the University of Southern Californa pro- vided material aid and support to conduct these studies, Illustrations are by Anker Petersen of the Allan Hancock Foundation. Types and complete series of species are deposited in the institutions from which the collections originate. 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Ventrum of antenor segments with rows of apie ( fig, 2) Australonereis ‘chlersi Ventrum without rows of papillae... - fa. Was ei pros Proboseis with fleshy, cirmis-like papillae (fig. 13) . eel uw Ceratocephala edmondss Probescis with dark horny paragnaths on some or wll areas as «! “ui the Probescis without processes, its epithelium smooth or at most wrinkled Nicon uestuariensis Paragnaths absent from oral tihng of proboscis .... ss00 min a. Ceratonereis Paragnaths absent from maxillary Ging of proboscis... ane wis Eunereis marrt Paragnaths typically presetit on hoth oral and maxillary rings of proboscis... Parsgnaths in the form of pectinated rows on sume or all gress ke sth ina Paragnaths in the form of conical, separated processes, ..., etal Maxillary ring with conical, and oral ting with pectinated processes Preudunereis Thoth Fings af proboscis with pectinated processes, or areas 1, If and V tstally bate Platynerets Area VI of proboscis with transverse ridges, or the ridges broken up inta poitits in a straight transverse row a este Shee tees es Perinereis Area VI of proboscis. with conical processes day S Median and posterior notopodia with falcigers (fig. 30) ‘OF r also. ‘sflinigers is » Nereis Notopodia with spinigers; lacking falcigers ..., se a4 ati Neonthes Prostomium deeply incised at midfront; dorsal cirri very long Ceralonerets wivabilis Prostomium hot incised in front; dorsal cirri nat unusually long . Neuropodia with simple and composite Foleigers ine wu Ceratonereis er wihracensis Neuropodia without simple falcigers .. Dorsal and ventral cirri greatly reduced: area J “of proboscis “with 34 or “to 6.9. Pointed patagnaths .... oft Ceratonereis anquisetis Dorsal and ventral arri not ‘greatly “reduced; area J of prohoscis bare Ceratonereis lapinigensis Notopodia without homogomph falcigers .... 4360 a. Pseudonereis rotinestiana Notopodia with homogomph falcigers in posterior segments Pseudonereis anomala Notopodia with simple, heavy falcigers (fig. 38) in median and posterior segments Platynerets bicanaliculate Notopodia without simple falcigers. dao ses Posterior notopodia with composite setae in which the aypetmboes “is strikingly tidged transversely... dose ond Platynereis polyscalma Posterior notapodia without setac that are ‘distally ridged Las ang ia dn Posterior notopodia with homogomph falcigers (fix, 37) Oe EES be “ee Pasterior notopodia without falcigers or only an occasional ineotispicuous one Plafynereis nunalhacnyts Modified natatory parapodia in female present afier segment 2 Peenieots dumenhi antipoda Modified natatory parapodia in female present after segment 30 Platynercix australts Area VI of proboscis with a single ridge on each side (Includes Perinerets amblyodonta, barbara, calmani, helleri, cam guina, obfuscuta, nigropunctata and pseudocamnguinu. See Chart 1V for distinguishing characteristics of each.) Area VI of proboscis with two ridges on each side (Includes Perinerets camiguinaides, variodentafa and vancaunicit. See Chart IV for distinguishing characteristics, ) Area VI of proboscis with four ridges on a side ..., we Pevingrcis ponmtensts Area VI of proboscis with a continuous transverse series of cones that extends across areas V and VI (includes Perinerets vallata and brevicirrts. See Chart TV for dis- tinguishing characteristics.) Notopodial lobe diminishes in size ( fig. 26) in posterior segments a so vere Nutopodial lobe does not diminish in size Rosterionly we amas oii Homogomph falcigers distally boldly bifid (fig. a) vr McIstosn, W. C. 1885 Report on the Annelida Polychacta collected by H.M-S. Challenger during the years 1873-76, Challenger Reports, 12, pp. 1-554, 55 and 39a pls. MAkENZELLER, FE. vow. 1879 Stidjapanische Anneliden. Akas. Wiss. Wien, Denkschr., 41, pp. 109-152, 6 pls. Monro, C. 1926 On the Polvchaecta collected by H-MLS. .4lert, 1881-1882. Fannhes Hesioni- dae and Nereidae. Linn Soc. London, Jour,, 36, pp, 311-323 Monro, C. 1930 Polychaete Worms, Discovery Reports, 2, pp. 1-222, 91 figs. Monro, C, 1931 Polychaeta, Oligochaeta, Echiuroidea and Sipunculoidea, Great Barrier Reef (Qld) Exp. 1928-20. Sci. Rep. Brit. Mus. (Nat. Hist.), 4 (1), pp. 1-37, 15 figs. Monro, C. 1936 Polychaete Worms. If, Discovery Reports, 12, pp. 59-198, 34 figs, Monro, C, 1937 The John Murray Expedition 1933-34. Scientific Reports, Polychateia. 8, No. 8 pp. 243-321, 28 figs, Monro, C. 1938 On a small collection of Polychaeta from Swan River, Western Australia. Ann. Mag. Nat. Hist. London, ser, 11, 2, pp. 614-624, 13 figs. | Monro, C. 19399 Polychaeta Antarctic Research Expedition, 1929-1931. Adelaide, Australia. Reports, Ser. B (Zoology and Botany), 4, pt. 4, pp. 89-156, 28 figs. Monro, C, 193%) On some Tropical Polychaeta in the British Museum, mostly collected by Dr. C, rpeslat al Zanzibar, Tahiti and the Marquesas, Novitat. Zool, Landon, 41, pp. 302-30. Oxupa, §. 1938 Polychaetous Annelids from the vicinity of the Mitsui Institute of Marine Biology. Japan, Jour. Zool., 8, pp. 75-105, 15 figs. Oxuna, S. 1940 Polychactous Annelids of the Ryukyn Islands. Biogeogr. Soc. Japan, Bull., 10, No. 1, pp. 1-24, 9 figs, Pruvot, G. 1930 Annélides Polychétes de Nouvelle-Caledome recueillies par M. Francois. Arch, zool. exp, gen. Paris, 70, pp. 1-94, & figs. 3 pls. ; Quatreraces, A. pr. 1865 Histoire naturelle des Annéles marina et d'eau douce. Patis, 1, pp, 1-588 Racovirza, E. 1893 Sur la Micronercis variegata Clpd, Acad, Sci. Paris, C.R., 116, pp: 1,390- 1,392 Scamarpa, L, 1861 Neue wirbellose Thicre beobachtet und gesanimelt auf einer Reise um die Erde, 1853 bis 1857. Leipzig. Pt. 2. pp. 1-164, 22 pls. R Winey, A, 1905 Renort on the Polychaeta collected hy Professor Herdman, at Ceylon, in 1902. Ceylon Pearl Oyster Fisheries, Suppl. Rep., pt. 4, pp. 243-324, 8 pls. THE MOLLUSCAN FAUNA OF THE PLIOCENE STRATA UNDERLYING THE ADELAIDE PLAINS BY N. H. LUDBROOK Summary The molluscan fauna of the South Australian Pliocene is best developed and preserved in the Dry Creek Sands which have been thrown down to the west of the City of Adelaide by the Para Fault. red THE MOLLUSCAN FAUNA OF THE PLIOCENE STRATA UNDERLYING THE ADELAIDE PLAINS PART I By. N. H. Luprroox * [Read 9 April 1953] SUMMARY Thé molliscan fauna of the South Australian Pliccene is best deyeloped and pre- served in the Dry Creek Sands which have been thrown down to the west of the City of Adelaide by the Para Fault. Pliocene strata were deposited unconformably on a post-Burdigalian erosion surface, and are overlain by Pleistocene to Recent sands and clays, mainly of freshwater origin, and nodular kunkar. In the Adelaide Basin shell heaps concentrated by ctrrents are frequent im the north-eastern portion, and are of economic importance since they generally mark the aquifer. Readily distingttishable lithologically, the light-grey fine sharp quartz sands carry a well-preserved rich molluscan fauna, mainly of the epineritic environment. The molltisca cotistitute essentially a tropical marine fauna in which four distinct elements may be recognized: a dominant Indo-Pacific, a Tethyan Eocene, a Recent Australasian, and a cosmopolitan, The presence of undoubted Tethyan Eocene subgetiera js of particular interest. The stage at which these reached Australia ts not at present determinable, but it is Hkely that they date at least from the Oligocene. Distinct from the two tropical elements are a large autochthonous Australasian element probably derived from an endemic stock, and a fourth element coimposed of cosmopolitan of widespread subgenera. Since 5790 of the species are restricted to the fauna, the age is detertninable only by correlation with known Pliocene faunas in Australia. Available evideiice suggests that the strata may be slightly younger than Pliocette strata (“Kalimian") in Eastern Victoria, but much work remains to be done before complete correlation is achieved. I, INTRODUCTION During the past 70 years the Adelaide Plains, comprising the eastern portion oi the St. Vincent Gulf—Adelaide Plains graben on which the City of Adelaide is built, have been at first intermittently and recently intensively drilled in the search for a supplementary or alternative water supply for the domestic and agricultural needs of the city and its environs. For the fiity years following the drilling of the first deep hole at Kent Town, close to the city area, borings were sunk at sporadic intervals by landowners for agricultural purposes. With the growth of the city and threatened failure of normal water supply from storage reservoirs in times of drought, a programme of drilling was initiated by the South Australian Mines Department in 1934 and greatly intensified in 1945. The area drilled covers some 250 square miles from the Gawler River 18 miles north of Adelaide, south to Brighton 9 miles south-south-west of the city, bounded on the west by Gulf St. Vincent and on the east by the foothills of the Mount Lofty Range along the line of the Burnside and Eden Faults. Practice has heen to seal the Government bores until drought necessitates opening them to supplement the city water supply. Material from several of the borings. was submitted to the writer by the South Australian Mines Department for palaeontological exaniination. Results of examination of the mollusca are embodied in the present study. During the past twenty years, Australian molluscan systematics have become confused by the reluctance of some workers to recognize generic affinitres between most of the Australian species and their relatives elsewhere. As a result, accurate * Department of Mines, South Australia. Trans. Rey Suc. S. Aust., 77, July, 1954 43 and detailed correlation of faunas has not been attempted. An additional problem arises from the fact that faunas from type areas are imperfectly known, Collect- ing has been done from easily accessible localities where fossils are numerous, but little systematic sampling has been carried out. With the aim of reducing some of the anomalies so created a representative series of the mollusca contained in the bores submitted to the writer was taken to London for comparison with type and other material in the British Museum. The fauna has now been completely revised and the nomenclature brought into line with that employed by specialists outside Australia, The stage name “Adelaidean” previously in use for the strata is abandoned in accordance with the suggestion of Mawson and Sprigg (1950, p. 69), Howchin (1928. p. 422) proposed the term for the richly fossiliferous marine sub-surface strata, which he considered to be of Upper Pliocene age, known only from borings within short distances of Adelaide. Smce confusion is always hkely to arise from the use of the term Adelaidean for the Pliocene marine sands when there is the well-established Adelaide System (formerly Series) of Pre-Cambrian age, Glaess- ner (1951, p. 280) has recommended its replacement by the name Dry Creek Sands, ‘II. HISTORICAL SURVEY The Dry Creek Sands were first discovered in 1889 when a deep bore ih search of water was sunk at Dry Creek, 6 miles due north of Adelaide, by the Australian Smelting Company. On this classical boring the discovery of marine deposits younger than beds then considered to be of Miocene age and older than admitted Pleistocene strata was claimed. In the following year a bore was sunk at Croydon 34 miles north-west of Adelaide and reported upon by Tate (1890b), who published a section showing that the Pliocene strata recognized in the Dry Creek Bore were penetrated at 340 feet; a thickness of 406 fect for the Pliocene was postulated. The boring was stopped at 800 feet. Subsequently a second bore was sunk at Croydon to a depth of 2.296 feet, adjacent to the first. The Pliocene and underlying strata were again reported upon by Tate (1898}, Pliocene being identified from 395 to 715 feet. No detailed palaeontological work was done to advance the knowledge of the fauna, although varying and speculative opinions on the age of the strata and their relative stratigraphical position were published, These may be briefly summarized as follows: Tate and Dennant (1896, p. 148) placed them above the beds now known as Kalimnan in Victoria and in the Pliocene. Hall and Pritchard (1902, p. 80) named the Kalimnan (p. 78) and con- sidered the beds described by Tate from Dry Creek to be contemporaneous and therefore of “Miocene” age. Howchin (1914, p. 156) differentiated them from the Kalinman (“Second Marine Series? Miocene”) as “Third Marine Series—Older Pliocene.” Chapman (1916, p. 156) accepted the view of Hall and Pritchard that the beds were contemporaneous with the Kalimnan, but supported the tarlier view of McCoy and the Geological Survey of Victoria that the Kalimnan was Lower Phiocene in age. - Howchin (1928, p. 422; 1929, p, 235) mtroduced the name Adelaidean, and “proposed to distinguish ..., the Adelaidean Upper Pliocene” from the Werri- kooian Upper Pliocene of Victoria. In a preliminary note on the stratigraphical position of the beds the writer expressed the view (Ludbrook, 1938, p. 445) that the beds now known as the Dry Creek Sands were probably contemporaneous with other beds of accepted Lower Pliocene age in Southern Australia. This opinion was strongly opposed by Howchin and Parr (1938, p. 289) and Parr (1939) who continued to maintain 44 an Upper Pliocene age for the fauna, Chapman (in Howchin and Parr, 1938, p. 290) agreed with Howchin that the Dry Creek Sands were younger than the Kalimnan, but considered them contemporaneous with the Pliocene beds at Hallett Cove. Singleton (1941, p, 22) established and defined the Adelaidean as a Stage. MAP SHOWING POSITION OF BORES STUDIED 978 e207 BORE al? SECTION LINE hye yb Fig. 1 Bore 215 is within the boundary of the City of Adelaide. On completion of a systematic study and analysis of the gastropod fauna of Abattoirs Bore, and taking into account the view of Howchin and Parr that the foraminifera had a more recent aspect than those of the Kalimnan, the writer (1941, p. 80) placed the Dry Creek Sands in the Lower-Middle Pliocene. Since the present work was completed the publication of a comprehensive report on the geology and underground water resources of the Adelaide Plains area (Miles, 1952) has added greatly to the knowledge of the subsurface geology of the area. In an appendix to the report Crespin and Cotton (1952) have corre- lated the Pliocene strata with the Kalimnan of Victoria, the faunal differences being attributed to facies. In the present study the molluscan fauna has been increased to 380 species, 78 of which have not been previously described; four new subgenera have been erected, The composition of the fauna has been determined as accurately as possible, its relationships with other comparable faunas analysed and its bearing upon the stratigraphical position of the strata discussed. The establishment beyond doubt of a faunal link between the European Eocene, Australian Pliocene, and the Recent Indo-Pacific Region is an important fact to emerge. Some faunal 45 migration, probably by way of Tethys, has almost certainly taken place, and closer study of faunas linking Australia to the Northern Hemisphere is warranted. There is at present no evidence of any faunal link with known American Tertiaries, and the study confirms the opinion that the deep waters of the Pacific Ocean have always been a barrier between the faunas of its western shores and those of the east, except in the extreme north and south where move- ment along the coastline has been possible. SECTION ALONG LINE 4B FROM BORES7 TO BORE 2i5 5 2 Unfestireaue matted chy cis [ix] Untmusfereve sands & grovel Sy Chay 20 ES Ged, wreund ‘ sy clay | beeniah sendy cley DET. EF Masato PLEISTOCENE TO RECENT 200 Bd Sand gravel 305 be ES alvishelay 415 330. el Lineatone HOT SAMPLED IN DETAIL! NOT SAMPLED 1 Dark send, chy wy = a 8 J a Fes} Kegilfaceaur amid ET Te he | an pendy mart aS fa Blue blac mudiparen, ma : Yeltes dandy mar! MIOCENE / HORIZONTAL SCALE ce] MILES Fig. 2 UI. GENERAL AND STRUCTURAL GEOLOGY Pliocene strata ate exposed as isolated remnants at irregular intervals along the eastern coast of Gulf St, Vincent from Aldinga Bay in the south 10 the City of Adelaide in the north (Howchin, 1923; Segnit, 1940). Pliocene lime- stone formerly outcropped along the banks of the River Torrens (Howchin, 1923, p- 283) and has been exposed in quarries on the south bank of the River at the tear of Government House (Tate, 1882, p. 40) and in the University grounds. ft has been frequently penetrated in shallow well sinkings and in borings in the City area at about 50 10 70 feet depth, including Kent Town Bore (Tate, 1882), Black Forest Bore (Howchin, 1935), Bank of the New South Wales Well (Cotton, 1947), and was noted by the writer in West End Brewery No, 2 Well, 6 Hindley Street, at depth from 69 to 70 feet, Fossils typical of the Dry Creek Sands were present mainly as moulds. Elsewhere the Pliocene has been penetrated only by borings into the Dry Creek Sands from Gawler River in the north to Glenelg in the south. The average depth below datum level at which the beds are penetrated ig 315 feet. Where the thickness is proved, the beds are generally from 150 to 180 feet thick, although an exceptional thickness of 320 teet was passed through in the Croydon Bore (Tate, 1898, p. 195). The average thickness iu six bores which reached the Miocene is 190 feet. The greater thickness of the Dry Creek Sands as compared with that of the sandy limestones in the City area and in exposures south of Adchiide is consequent upon tectonic movements which disturbed the area in Jate Tertiary and Quaternary times. The Moimt Lofty Ranges and Adelaide Plains are units in a system of regional meridional block faulting in which the St. Vincent Gulf-Adelaide Plains form a graben and the Mount Lofty Ranges a horst to the east. The general structure of the fault system has been described chiefly by Benson (1911), Fenner (1930), and Sprigg (1945). The major faults in the Adelaide Plains and Western Mount Lofty Ranges are shown on fig. | The trend Imes are broadly N.N.E.- §.5,W. Fenner (1930, p. 15} has suggested that two periods of block iawlting are probably involved; while there is at present no direct evidence that this is the case, it is not improbable that the orogenic movements which elevated the Mount Lofty Ranges horst antedated the deposition of the Dry Creek Sands and their subsequent down-faulting to the west of the Para Fault. To the south and east of the Para Fault in the immediate neighbourhond of Adelaide only the more resistant caleareaus equivalents of the Dry Creek Sands have been preserved at shallaw depth. West of the Para Fault, however, the sediments have been thrown down to a maximum of the order of 350 feet, and an average thickness of 190 feet of unconsolidated sands has been preserved beneath a cover of later marine and freshwater sediments. The subsurface rela- tionship of the Dry Creek Sands to the overlying and underlying sedi- ments and to the Para Fault is shown in the section (fig. 2) dtawn along the line AB of fig. 1. The position of the Pliocene remnant underlying the City is shown hy the narrow band 69 feet below the surface in Bore 215 to the east of the fault. IV. SEDIMENTATION AND LITHOLOGY The Dry Creek Sands and their equivalents in the Phocene were deposites! in a2 shallow bay or gulf of the Pliocene seas after the depression af the ol:ler strata which had been reduced to base surface at the end of the Mesozoic ane submerged during the early Tertiary, At the close of the Lower Miocene a cycle of erosion occurred in South Australia, where, unlike Eastern Victoria, no continuous sequence from Lower Miocene to Pliocene is revealed and a marked unconformity separates the Pliocene from the underlying strata, the youngest of which sre Lower Miocene, with the restricted Lower Miocene foraminifer, dustrotrillina howchinit. On this Tertiaty erosion surface the Dry Creek Sands and the sandy Hme- stones were deposited. As revealed in the borings, the Dry Creek Sands are a well-defined lithological and palaeontological unit usually readily distinguishable from the underlying tarlier Tertiary strata. The Miocene is generally but not always a yellowish sandy marl or calcareous santstone. The sand grains are frequently muck encrusted, Overlying the Miocene, the light-grey or sitvery, fine. sharp Pliocene sands and clays, carry a rich marine fauna. Intercalated bands of grey and white limestone occur apparently irregularly throughout the strata, Present knowledge does not permit the correlation of these bands in any way. They may be the equivalents of the more resistant members of the Phocene which 47 underlie the City to the east of the Para Fault, but the writer’s opinion is that the sandy limestones to the east of ihe Para Fault represent the shallow littoral facies. Bores examined in detail demonstrate that very fossiliferous bands occur at more than one level in the Pliocene, their position probably being determined by the operation of currents in the bay in which the sands were deposited, The indication is that the general direction of such currents was north- easterly. This would account for the unusually rich bands penetrated in Abattoirs, Weymouth’s, and Salisbury Bores in the north-eastern portion of the basin. These highly fossiliferous bands were not deposited evenly on the floor of the _COMPOSITION OF THE FAUNA y eb - boo BO ih ow \~wae J = "Tanjukus’, L © “Lenpferdian”, B} > “Baresferdian y Baiconbien’, By © Baiensdahen’ ce 'Chetlenharnian™ Fig. 3 basin in still water, but were produced by the concentration of shells along the shore lines by surface currents. Variation in intensity of the currents would account for the uneven distribution of the load. As the highly fossiliferous shelly band is most frequently the aquifer, boring generally stops when it is reached. Where the band has been passed through and the boring continued, less fossilifer- ous strata are revealed. 48 Overlying the Dry Creek Sands are approximately 300 feet of superficial clays, sands, and gtavels of Pleistocene to Recent age of alluvial deltaic origin consequent upon the upliit of the Mount Lofty Ranges horst. They form a helt af piedmont alluvitim widening northwards and about 10 miles wide in the immediate vicinity of Adelaide. North of Adelaide remains of extinct marsupials, including Diprotodon, have been found in the alluvium. Except for two recent incursions of the sea, cach represented by less than five feet of sediments (Miles, 1952, p. 32) there was no general submergence of the Adelaide Plains during the Quaternary. The downward succession from Recent to Miocene may be exemplified by Filsell’s Bore (No, 169), examined by the writer and sampled to a depth of 540 [vet when boring ceased in the Miocene; Surface -302 feet. 302-517 feet. —- 317-348 feet, | 343-360 Feet. 360-373 feet. Clays and gravels of Pleistocene to Recent age. Greyish-brown fine glauconitic sand with Rotalia beccarii, Ostrea. sp. and “Mactra” sp, Greemsh-grey silt with a similar fossil content. Fine grey sand, highly fossiliferous, with typical assemblage, mainly imolltsca, Fine sharp quartz sand, highly fossiliferous with mostly small mollusca and foraminifera, together with six species of bryozna. 378-382 feet. 382-396 feet, 396-409 Feet. ADOPTS Feet. 443-452 feel. 4152-192 feet. Dark-grey fine fossiliferous sand. Fine silver-grey sand, very highly fossiliferons, with a typical molluscan assemblage, mostly pelecypoda. Fine grey fossiliferous silt, 90% disappearing on washing, with the pelecypod Cond ylocardia tenuicostae and associated but not restricted foraminifera and gastropoda, Fine grey fossiliferous silt. flard grey fossiliferous limestone. Grey fossiliferous sands with brynzoa and an admixture of Pliocene and Miocene fossil species. indicating that the lowest level of the Pliocene hus been reached and the Miocene penetrated, Yellowish sands, much encrusted with calcium carbonate, with the Miocene foraminifer. Operculina wictoriensis and bryozoon Mecynoetia proboscidea. Hard yellow limestone with Operculina victoriensis and an associated Miocene fauna, Greyish-brown sands with a similar fossil content. 492-504 feet. S(i4¥-524 feet. 524-530 feet. From the manner of collecting the samples only over broad intervals accurate zoning cannot be achieved, From the surface to 302 feet the typical alluvial clays and gravels forming the stitface cover of the Adelaide Plains are probably of Pleistocene to Reeent age. These correspond to the 341 feet of sand and clay penetrated in Abattoirs Bore (level of collar 170 feet). From 302 feet to 348 feet the section may be Upper Pliocene in age, No restricted fossils are present; they are generally few. and Recent in character. The Dry Creek Sands occur from 348 feet to approximately 475 fcet, the highly fossiliferous band being between the 382 and 396-fnot level, Pre-Pliocene beds occur below 492 feet and the lithology shows a protiounced change at that level, the characteristic yellow colour replacing the grey sainds of the Pliocene. The Miocene foraminifer Operculina victoricusis makes its appearance. The change from Dry Creek Sands to the underlying Miocene may also be indicated by the sudden increase in the number of bryazoa which are not common in the Pliocene, although they do occur in some nitinbers representing numerous species in certain borings, such as Hindmarsh. a The sandy limestones underlying the City of Adelaide carry Dry Creek mnolluscs—mainly in the form of moulds of Pwurritelia (Haustator) avricula adefaidensis, Polinices (Conuber) balteatella, and species of Polinices, 'Mar- ginella,” Emarginula, Euchelus, and “Venus.” Where they are belter preserved as tn the unleached block removed in the excavations for the foundations of the Bank of New South Wales building the determinable fauna is similar to that of the calcareous sandstones exposed at [Hallett Cove and Ainge Bay, with Chlamys antiausiralis, Chlamys (Equichlamys) consobrinus, Chlamys (Equichlamys) sublifrons, Spondylus spondylotdes, OStrea arenicola, Glycymeris (Veletuceta) subradians, Diastoma provisi, and Polinices (Conuber) batteatella, The lime- stones are allochthonous, of the fassiliferous-fragmental type commonly found in association wilh quattzose sandstone (Krumbein and Sloss, 1951, p. 139), Accord- ig to those authors, such associated rucks are depusited under essentially stable conditions with mild subsidence ot the depositional area. V, PALAEOECOLOGY The environmental and climatic conditions under which the community preserved in the Dry Creek Sands lived are determinable ouly by the thanato- coenose or assemblage of fossils so well represented in borings such as Abattnirs (No. 89), Weymouth’s (No. 207), snd Hindmarsh (No. 6). That it is most unlikely that the mollusca existed in fife in the position in which they were deposited has already been suggested in the pteyious section, where the role played by surface currents in deposition of the sediments is briefly cescribed. That many of the mollusca were dead before their shells were deposited is demonstrated by the fact that large numbers of pelecypnds and gastropods, many of them very small, have been bored by predatory mollusca, perhaps the Hinia (Reticunassa) which occurs numerously in the Hindmarsh Bore. Shells were obviously piled in heaps by surface currents operating towards the north-east, such heaps constituting the shelly band of “oyster bed” which is generally the aquifer in the Dry Creek Sands and in which the oyster Ostrea arenicole is one of the conimonest species, Notwithstanding the mode of deposition, the fauna is sufficiently uniform for an accurate estimate of the ecology to he made, It has long been recognised that Australian Pliocene and Miocene mollusca belonged in the main to tropical genera chiefly inhabiting the Indo-Pacific region today. However, no serious attempt has been made to correlate them in any detail, The origin and relation- ships of the Dry Creek Sands fauna will be discussed in detail in the sueceed- ing séclien and separately, under such species as are concerned, in the taxonomic study of the species, The Dry Creek Sands carry essentially a tropical marine fauna, with a large percentage of its subgenera tepresented in the Indo-Pacific region today. The subgenus, as a practical indicator of climatic conditions (Chavan, 1949) has been freely employed throughout this study. The living community now partly pre- served in the Dry Creel Sands undoubtedly inhabited a sandy bay of the Pliocene seas with relatively sheltered conditions and little disturbance except from surface currents, Apart from the evidence of differential deposition of load, the presence of bryozoa which require circulating waters for their existence indicates that the sediments were not lai] down in still waters. The environment was epineritic, with shallow water species and subgenera prevailing, East of the Para Fault the limestones ate tnore characteristic of the littoral environment and littoral species af Chlumys and Polinices (Conuber) are more common. The geaus Terebratia, formerly identified from the Dry Creek Sands and apparently indicating tropical mangrove swamp conditions (Crespin and Colton, 1952, p. 233) similar to these of the native habitat in Northern Australia, has E 30 been erroneously identified. The restricted species described as Terebralia ade- laidensis Howchin and Cotton is not a Terebrafia but a Thericinm belonging to a lineage represented in the Italian Pliocene, Recent Indo-Pacific, and probably the Parisian Eocene. Tropical subgenera of the littoral or epineritic environment which occur in the Dry Creek Sands include the pelecypoda Arca, Cucullaca, Pinctada, Sportelia, Belluctna, Prophetilora, Vasticardixm, and the gastropoda Notohaliotis, Laetifur- tor, Pulehrastele, Calthalotia, Tugali, Gena, Cocculinella, Nina, Pelecydint, Obtortio, Semibittium, Semivertagus, Amaes, Margineulima, Agatha, Pyrga- lampros, Cypraeerato, Globularia, Trunculariopsis, Pterochelus, Latiaxis, Fusinis, Bavyspira, Turrancilla, Mitra, Tudicla, Cymbiola, Aulicina, Cancellaphero, Gibberula, Closia, Volvarina, Tomopleura, Etrema, Veprecula, Floraconus. Subgenera inhabiting warm seas but with a greater range of thermal tolerance than the above are the pelecypoda Barbatia, Tucetona, Tucetilia, Chama, Milthe, Regozara, and the gastropoda Emarginula, Astele, Phasianotrochus, Euriclaneulus, Minolia, Spectamen, Phenacolepas, Tenagodus, Ataxacerithium, Hirtoscala, Niso, Syrnola, Puposyrnola, Turbanilla, Chemnitzia, Pyrgiscus, Cheilea, Sabia, Argo- buccinnm, Cymatiella, Murexsul, Homolocantha, Phos, Reticunassa, Serrata. The distribution table (pp, 56-62) attempts to show the horizontal distribution of cach of the species constituting the molluscat fauna recovered from the Pliocene of 14 borings. Hores are arranged from north to south from the most northerly, Tennant's Bore (No. 189), to the most southerly, Brooklyn Park (No. 17). Numbers of the bores are as follows: Tennant’s (189}, Weymouth’s (207), Abattoirs (89), Dry Creek (178), Glanville (57), Filsell’s (169), Holden’s (81), York (14}, Croydon {51}, Hindmarsh (6), Bore 65, Cowandilla (5), Kooyonga (105), Brooklyn Park (17). The inference to be drawn from the table is that there is greater concentration of species in the northerly bores. and that in the southerly bores those that are to the east and nearer the Para Fault and the presumed shoreline are more fossiliferous, Such concentrations have been effected apparently on or near the shore line, generally towards the north-east of the bay. The associated foraminiferal fauna contains a number of genera living today in shallow warm waters, including the Peneroplid genera Peneroplis, Sorites, Amphisorus, and Marginopora, Marginopora vertebralis is extremely common in some borings, and together with Peneroplis planatus ts exposed on weathered surfaces of the sandy limestones of the littoral facies. Rotalia beccarit is found in almost every sample and is perhaps the mast commonly occurring foraminifer in the Dry Creek Sands. Its presence in large numbers is indicative of a bay- littoral environment. Associated with the Peneroplidae and Rotaliidae are species typical of the Recent Flindersian Province such as Flintina triguetra ( Brady) and Nubecularia luctfuga vat, lapidea Wiesner. VIL FAUNAL RELATIONSHIPS Four distinct elements may be recognised in the fauna: a dominant Recent Indo-Pacific, a Tethyan Eocene, a Recent Australasian, and a cosmopolitan, A. Tue Recent Inpo-Pacipic ELEMENT The dominant element in the fauna is Indo-Pacific. Although the tropical character of Australian Tertiary molluscs has always been recog- nised, no detailed attempt has hitherto been made to correlate Australian Tertiary faunas with the living faunas of the Indo-Pacific Region. With the possible exception of one or two species living today in North Queensland, with which examples in the Dry Creek Sands appear to be conspecific. the fauna has nO species in common with the Recent Indo-Pacific, but the resemblance or affinity in many cases is remarkably close and the species are subgenerically identical. 31 The affinities between species of pelécypoda appear ta be less striking than those between gastropod species. This is perhaps due to the fact that the gastropoda are more restricted and generally shorter ranging than pelecypoda, and such affinities as do occur are more conspicuous. Species of pelecypoda which may he directly correlated with Indo-Pacific or Northern Australian specics are: Montlilora (Prophetilora) chavani sp. nov. with M. (P.) arizelo Iredale; Vasticardtum submaculosum sp, nov, with V. maculosum Wood, V. transcendens Melvill and Standen, and V. mauritianum Deshayes ; Antigona {Proxichione) cognata (Pritchard) with A, (P.) listert Gra and A. (P.) refiexlatum Linné,; Gafroriuns perarnatum N, H. Woods with G. dispar Dillwyn; Veremolpa protemarica (Cotton) with F. marica (Linne). The scaphopod species Dentalium (Dentalium) howchini (Cotton and Ludbrook) is related to D, (D.) elephantinum Linné, Affinities in the gastropoda are to be found between Calliostoma (Lactifautor) spp, and C. (L,) deceptum Simith; Astele (Pulchrastele) planiconicum (Ludbrook) and A. (P.) seplenartum Melvill and Standen; Thalotia (Calthalotia) nitidissima (Ludbrook) and T. (C.) arruersi¢ Watson; Clanculus (Euriclanculus) quadricingulatus Ludbrook and C. (E.) cevlonicus G. and H. Nevill; /sanda (Minolia) perglobosa (Ludbrook) and [, (M.) pulcherrima Angas; Speclamen planicarinatum sp. nov. and S. hiangulatum Adams; Spectamen preecursor sp, nov, and S. sayademalha Mel- vill; Trbiola (Partwbiola) depressispira (Ludbrook) and T. (P.) _carinata, T. (P.) quinguecarinata and T. (P.) novemcdrinata all of Melvill; Therictun adelaidense (Howchin and Cotton) and 7. opporlumen Bayle; Amaca (Amaea) triplicata (Tate) and A, (A) kieneri (Canefri); Tranculariopsis pera- mangus (Ludbrook) and T, érunculits (Linné) ; Hemolocantha antecedetis sp, nov, and H. secunda (Lamarck) and H. varicose Sowerby ; Latiaxis dissitus Cotton and L. mawae (Gray); Austromitra angusticostata Ludbrook and A. capensis (Dunker), 4. turtiger (Reeve), A. kowtensis (Sowerby), 4. capri- cormia Hedley; Tudicla sinotecta Ludbrook and T, spirillus (Linné) ; Cymbtola tabulota (Tate) and C. pulchra (Sowerby), Volvaring (7) incommoda sp. nov. and F’, (2?) sercodes Tomlin, V. (?) serra Bavay- BR, Tue Tetuvan Eocewe ELEMENT One of the most interesting faets to emerge {rom the attempt to correct the generic and subgeneric locations of the mollusca is that several subgenera well represented in the European Eocene have closely allied representatives in the Dry Creek Sands. This is perhaps not altogether unexpected in view of the dominance of the Indo-Pacific element to which the Tethyan Eocene is ancestral {Martin 1914; Umbgrove, 1930; Davies, 1934, p. 104). It seems somewhat improbable that the ‘Tethyan element in the South Australian Pliocene was intro- duced by late migration by way of the East Indies. Molluscan faunas of the East Indieg and those of the Australian Tertiaries seem to have less in common than might be expected. The most convincing conclusion to he drawn is that the Tethyan molluscan elements had already reached Australia during the Eocene or Qligovene, This is supported by the writer's recent discovery of the subgenus Bellucina in clays of prohable Eocene age from the South-last of South Aus- tralia. Tethyan foraminifera Nwmmulites, Discocyclina, and Pellatispira have been recorded from the Eocene of the North West Cape—Cape Cuvier area in Western Australia (Chapman ard Crespin, 1945), and additions to the knowledge of ihe Tertiaries in the North-West of Western Australia may establish the presence of an allied molluscan fauna, Present knowledge of the affinities of pre-Pliocene Tertiary mollusca from southern Australia is too limited to petmit confirmation in more than the one instance cited af the preservation of the Eocene element within the Australian faunas, but that this is the case is more than probable. It is supported by the 52 strong Indo-Pacific affinity of the foraminiferal and molluscan faunas of the Tertiary marine sedimentary rocks exposed at intervals over a wide geographical range trom Notth West Cape in, Western Australia to north-western Victoria. The geological record over this area is very imperfect and no gid conclusions may be drawn, but information is available to suggest that thermal conditions were very uniform over this and the whole of the Indo-Pacific region during most of the Tertiary, and no sudden change of temperature ur ecological condi- tions led to the extinction of faunas between the end of the Eocene and the Middle Pliocene. Evidence of the preservation of a Tethyan element in the fauna is based on the presence of species of the following subgenera, cach having close relatives int the European or English Eocene and also in the Recent or late- Tertiary Indo-Pacific fauna: Chlamys s. str. with the C. varia series in the Parisian Eocene, and also it the Miocene and Pliocene of ‘the Red Sea region and Zanzibar Protectorate (this series is fairly widely spread and would not in itself indicate a Tethyan clement, but is regarded as worthy of note in view of the presence of the other undoubted Tethyan subgenera); Lentipectest, repre- sented by L. cornens (Sowerby) in the English Eocene and L. borneajus (Cox) in the Pliocene of the North Borneo. Arcturellina, closely allied to the Parisian Eocene species aspernla, aigensis, prevosti, pulchra, ambigua, and serricata, all of Deshayes; Sportellu with S. dubia Defrance in the European Eocene atid 5. jubota living in North Queensland ; Monitilara s, str. represenved in the Parisian Eocene by M, clegans Detrance and the Australian Recent Peronian by M. ram- sayi Smith; Gibbolucina with G. ellipsoidalis Cozsmann and Peyrot in the Parisian Eocene, G. ca/losa (Lamarck) in the Indo-Pacific; Seliveina with B. ligata (Cossinann and Pissarro) in the Parisian Eocene, B. evcosma Dall in the Indo- Pacific; Semivertagus with S. unisuleatum Lamarck in the Parisian Eocene; Coxellaria (created below) related to C. cieve (Lamarck) and C. multispira (Deshayes); Globularia, very like Globularia sigaretina Lamarck from the Cal- eaite Grossier. There ate in addition the following subgenera common to the European Eocene, Adelaide Pliocene, and Recent Indo-Pacific which have not been studied in detail by the writer who accepts the authority of Wenz (Handb, der Palaozool, Gastropoda) that they occur in both the Tethyan Eocene and Recent Inde-Pacific taunas: Semibitiivm, Margineulima, Fusinus, Twdicla, Auticing and Gibberult. It is emphasised that, despite resemblances between certain elements in the fauna and elements in the Recent Indo-Pacific and the Tethyan Eocene moliuscan faunas, the total composition of the faunas in each case is very distinct and local ecological conditions tio doubt very rapidly produced divergent branches from a common stock. One of the most striking features is the general lack of specific resemblance between the Tertiary mollusea of the East Indies and Australia, although both appear to be influenced by a Tethyan Eocene element. As an example, of the mollusea described from the Pliocene of North Borneo (Cox, 1948) only two species may be regarded as showing any relation- ship to Australian Pliocene species; Lentipecten. horneanys (Cox), related to Lentipecten adelaidensis sp.nov., and Timoclea bataviana which from external features appears to belong to Verenrolpa and to be rejazed ta PY’. protomarica of the Dry Creek Sands and to . marica of the Recent Indo-Pacific, It is therefore surprising to: find so close an affinity between the Dry Creek Sands Pliocene and the Indo-Pacific Recent Furnas. C. THe AUSTRALASIAN ELEMENT Distinct from the tropical element which, as shown above, in some species represents a preservation of Tethyan features, is a large autochthonous element which has developed since early Yertiary times in Australia and which is not 53 represented elsewhere other than to a limited extent in New Zealand, No work has been done in Australia to establish the lineages of the subgenera comprising: this element, and it may at present be assumed to have arisen from a native stock. At this stage it is not possible to give the vertical stratigraphical ranges of the subgenera so that the horizons at which they separately first appear may be indicated, | The Australasian element, corifined fo Australia with the exception of those subgenera marked with an asterisk which occur also in New Zealand, is com- posed mainly of the subgenera Ennucula, Neotrigonia, *Cuna, Condylocardia, *Myllitd, Pseudarcopagia, *Tawera, Anapella, Horpetopoma, *Phasianotrochus, Euriclanclus, Starkeyna, Partubiola, *Munditia, Bellastraca, *Linewmera, Cteno- colpus, *Colpospira, *Zeacumantys, Ddnnevigena, *Evelynella, *Zeacrypta, Tylo- spira, *Ellatrivia, Notocypraed, : Umbilia, Conuber, Sigaretatrema, *Taniella, *Tasmatica, Hypocassis Antephalium, *Cymatiella (also in Pacific), *Muresxstel (also in the Pacific), Litosamia, Enattmene, Bedeva, +Pleia, Cupidoliva, *Austro- mitra, Tumitra, Axstroharpa, Amorid, Ericusa, Sydaphera, Inquisitor, *Filo drillia, Pervicucta. ‘The lineages of subgenera commor to Australia and New Zealand are not definitely established in Australia, although some are known in New Zealand at least from the Eocene and are not late Tertiary introductions with the Notonec- tian Immigration during the New Zealand Castlechfhan ( Marwick, 1929). There was some addition of Indo-Pacific units to the New Zealand fauna during the early Tertiary (Marwick, 1925), although the Indo-Pacific element is ve much weaker in the New Zealand than it is in Australian faunas, Australian elements may have been introduced during the early Tertiary also, D. CosMorouitaN ELEMENT ; The rest of the fauna is composed of cosmopolitan subgenera or those which have not as yet been sufficiently studied for any precise pronouncement upon their affinitics to be made, VII. AGE OF THE FAUNA The problem of dating the faunas of the Australian region and of correlating therm with the European time-scale has never been an easy one, and although much has heen added to the knowledge of Australian Tertiary stratigraphy during recent years by study of the mictofaunas, an accurate or reliable determination of the Sequence and comparable time relationship has still to be made In the absence of restricted zone fossils the most reliable method appears to be to correlate the total faunal assemblages with faunas of established age elsewhere in the Australian and neighbouring regions, There is no doubt that the Dry Creek Sands are post-Miocene. They rest with angular unconformity on beds not younger than Butdigalian and contain 110 restricted Miocene zone fossils, The mollusca, however, are almost totally unlike the Recent mollusca inhabiting the adjacent coastal waters, and atiy attempt to apply the method initiated hy Lyell of assessing the percentage of living species’ would give an entirely etroneotis result- The table (fig. 3) has been constructed to show the composition of the fauna from the best information available at present. The “stage” names hitherto employed for Victorian and South Australian pre-Phiocene Tertiaries are here us¢d only to give some indication of the length of range of the unrestricted species. They will be abandoned when acturate zoning of the strata is achieved. - Salient features of the analysis are: 1, The very low percentage (11) of Jemmy's Point (“Kalimnan") species. 2. ‘The very high percentage (57) of restricted spectes. 3. The 10% of Recent species not occurring at Jemmy’s Point, 54 This purely statistical evidence would suggest that the Dry Creek Sands are younger than the Jemmy’s Point Formation (“Kalimnan”). The latter being accepted as Lower Pliocene in age, the Dry Creek Sands could then be regarded as late Lower Pliocene or early Middle Pliocene, From the non-statistical viewpoint the exact correlation of the Jemmy's Point Formation and the Dry Creek Sands is limited by factors of distance and facies. The type section at Jemmy’s Point, Kalimna, Gippsland, is 650 miles east of Adelaide. The strata in that locality were laid down without stratigraphical break (Crespin, 1943) in a sedimentary sequence embracing stages frotn at least Oligocene to Pliocene. The Dry Creek Sands were deposited after a period of denudation with a break in the Miocene-Pliocene seqiience, There was during Pliocene times no connection by way of Bass Strait between the two areas. For this reason the term “Bass Strait Province” introduced by Crespin (1950, p. 423) is somewhat misleading,‘"’ since it implies the existence of Bass Strait prior to its foundering. The Jemmy's Point area was separated from the Pliocene seas to the west by the long peninsula of which Tasmania formed the southerly part, and diverse influences indubitably prevailed im the two areas. “Kalimnan” species recorded from the Dry Creek Sands are frequently not typical. Whether this is due to stratigraphical er environmental facies variation is 2 question which can only be answered by close study of all Pliocene faunules over the geographical range between Adelaide and East Gippsland. Were the personal factor permitted to operate to the extent of separating some of the South Australian examples from the typical species, the number of restricted moliusca in the Dry Creck Sands would be even higher and the number of “Kalimaan"” further reduced. On the other hand, as yet no detailed study similar to the present one has been made of the Jemmy’s Point mollusca or of mollusca from Pliocene localities elsewhere in Victoria to enable one to express a confident opinion that some of the restricted Dry Creek Sands mollusca do not occur in the Victorian Pliocene. Furthermore, the fauna of the Dry Creek Sands differs markedly from that of the estuarine Pliocene strata of the Murray River. One can only emphasise that much detailed work remains to be done before the Pliocene sequence in Southern Australia is definitely established, From the microfauna! aspect the only beds which have been correlated with the Dry Creek Sands ate limestones in north-western Australia and on the Nullabor Plains from which the foraminiferal assemblage of the Dry Creek Sands has been reported (Crespmn, 1950, p. 425).,‘?) The New Zealand Waitotaran is more closely related to the Dry Creek Sands than is the Nukumaruan, and if any significance may be attached to trans-Tasman correlation of climatic conditions, the similar conditions prevailing during the South Australian Pliocene and the Wattotaran, with sudden extitiction of tropical forms at the end of the period of deposition of the Dry Creek Sands may be worthy of note. The Nukumartian was marked hy a cold-water faunal immigration brought about by the advance and later retreat of subantarctic waters m the Middle Pliocene (Fleming, 1944, p. 209), It is certain that somewhat similat conditions existed in southern Australia where the Dry Creek Sands and their equivalents represent the last link with the tropical waters of the Indo- Pacife. The only suggestion of a gradual infiltration of colder water forms is provided by the presence in the Dry Creek Sands of the Flindersian fora- minifera Flintina triguetra (Brady), Crébrobulimina polystoma (Parker and Jones) and Nubecularia lucifuga var. lapidea Wiesner, and Flindersian 1 Tt is also liable to confusion with the term Basan Province in use for the land fauna of Tasmania. ) As Miss Crespin has identified the foraminifer Austrotrillina howchini frony what Fd be the same formation on the Nullarbor Plains, the second correlation requires con- Fmattan. 55 mollusca not related to tropical forms, including Nucula (Ennucula) beach- portensis Verco, Nuculana (Scaeoleda) verconis (Tate), Limopsis vixornata Verco, Lissarca rubricata (Tate) and Lissarca rhomboidalis Verco, Bornia irigonale (Tate), Mysella ovalis Tate, Hiatella angasi (Angas) Batilloria (Zeacu- mantus) diemenensis Quoy and Gaimard, B. (Batillariella) estuarina (Tate) Trophon (Litozamia) goldsteini Tenison-Woods, Mitrella (Dentimitrella) lin- colnensis Reeve, Retusa (Semiretusa) apiculata (Tate), and Volvulella rostrata (Adams). These are all species of autochthonous genera which have probably evolved from endemic Australian elements. 56 DISTRIBUTION. TABLE SPECIES , \ ; BORE a < . SSSLRSexae ew Es ' ‘ m= a “ ™ - a a A a a Nucula (Ennucula) kalinnae Singleton Hie tee geile ORE rm et Be et ee Nucula (Ennucula) beachportensis Verco .. seid cet > aati eS pan ae ate at. a Nucula. (Ennuciula) venusta N. H. Woods ni, wha Le es ber ee ee Pronucula morundiana (Tate) me ae jase weit Haji hb ee t= Ser. Nuculana (Scaedleda) woodsi (Tate) an) aes) Se ee ee SS Nuculana (Scaeoleda) crebrecostata (T. W.) ene. wre ae Roe SX Se ier 5 eo Nuculana (Scaeoleda) verconis (Tate) toe fae We Sahoo SS ee xl Arca negata (Cotton) .... Ae sng we tee) foe ae HE SB ea ee fee epee yo = Barbatia (Barbatia) epitheca Cotton a a i > es ee ee ee Barbatta (Acar) coma (Cotton) sg chen a Da SN ee dee get eet Se et Se Cucullaea cortoensis McCoy np ey! Oe tee Coes ee aa eo Cucullaea praelonga Singleton wi? cine fair bad ole Spe ee xx Limopsis beaumariensis Chapman wae eas Cs XK KH EH NEE HLH Limopsts macéoyi Chapman... ease aa OK XK KO Limopsis eucosmus Verco im O52. Fie las dee beet! oe A te mie Limapsis vixornata Verco aod wae ‘ste a x SS — Lissarca- rubricata (Tate) ates ste seve dap a eh ES ee Hh Ke Lissarca rhomboidalis Verco .... fang ass a we SX a eee eel att Glycymeris (Tucetona) convera (Tate) ae CXR KH UK XH K_X Glycmeris (Tucetilla) tenuicostata (Reeve Tn Paes ee Mee eee HE tye Glycymeris (Veletuceta) subradians Basedow wh gir do SRM Re Sa ee peep Pinctada crassicardia (Tate) sone tate ath ow O-XXxX--~_-x--—x__ Loapha hyotidoidea Tate a, Te a Se ne St. ee eel Pe a xox Ostreg urenicolaTate t.. icd aed tute te ae ee Ee SCO ee Neotrigonia trua Cotton np i | aS shh anh ome bo Le See coh te og LeuSe Chlamys (Chlamys) polyaktinos sp. nav... ee, we = EOL ee Be _Chlamys (Chlamys) antiaustralis (Tate)... nue KO KEK AK XK XEKE Chlamys (Equichlamys) consobrina (Tate) bite wah We = 2 ee Se en Ss Hs Chlamys (Mesopeplum) incerta (T. W.) ew ao & RE scecteaa lier x-- Lentipecten adelaidensis sp. noy. ti0 is jas Calliostoma (Laetifautor) oblsquicancellatum (Lud. ) Calliostoma (Laetfantor) stinicarinatum (Lud,) Calltastoma (Laetifautor) crebrinodulosum (Lud.) Calliostoma (Laetifautor) bicarinatun (hn, ) oh Astele (Astele) fanuticem Lud. a ete Astele ( Pulchrastele) planiconicum (Lud. > pate Astele (Pulchrastele) tuberculatum (Lud.) i. Cantharidus (Phasianotrochus) laxegemmatus (Lud) sabe Cantharidus (Phasianotrochus) subsimplex (Lud. ) Thalatia (Calthalotia) nitidissima (Lud.) f Thalotia (Calthalotia) fictitis (Lud, ) ae Clanculus (Euriclanculus) quadricingulatus Lud. Clanculus ( Euriclanculus) eucorinatus Lud. ante Isanda (Minolia) perglobosa (Lud.) ie abt Npectamen plantcarinatii Sp, NOV, ewer sued Spectamen praecursor sp. nov, east vo sees Gena incalia Cotton ss ase epee Tetnostoma depressultun ( Ch. and Gab. } aioe sore Starkeyna. pulcherrima (Ch. and Gab.) vis vue Tubiola (Pariubiola) depressispira (Lud.) 7 Tubiola (Partubiola) varihrata (Lud.) Ty! Crossea (Dokicrossea) cf. labiata T. Wi or, Collonia omissa sp, tov. ws ina wats Astraza (Bellastraea) hesperus Sp: nov. wie tee Liotina (Mundifia) tarmanica T. Woods... tone Phasianelladennanti Crespin 0.0 se tee seen Pellax jeyuma sp.nov... ve Phenacoletas tela Lud. sage mi Sos Cocculinella salisburyensis sp, nov... ans Tectarius (Nina) adelaidensis (Cott.)* BR FRE Pbrprdeutrerd sd we nwa ttiti Plt riwt tr tripe tet Pibeali ltt Awl aka | wat li Re lL a Al ai AMA | LAR ee mame ee Se ee He ee SPECIES BORE SSBERRSSAaSTS* SS —- oF - - - Amphithalamas (Pisinna) chrysahdus (Ch. pal Geb) ww ee eee ee Merelina (Linemera) varisculpta sp. nov. ... phe eM ae ee age ee eh cvs Turbvella praenovarensis sp.nov. eee KR ee Turboella elimatiag sp.noy, in, 0 wee sete Sannin ne Meee Paes HE eR ee rhe Kaurnella denotata Lud. Ted beet tape nif} ey ay SES ee HS SS Xs ee Pseudohiotia angost Crosse... en eee Soa” eee ee, enone wr ee Cingula (Pelecydium) eylindracea T: ‘Woods wh wos EOE BO Se oe SH xa--—- Rissomanivea Adams ... 0 om “i 2p bade ase a A ag a ene ee ed Swe em pces Rissoina élegantula Angas .... eos wile, dalle Se ee ee hae st Rissoina tinelo sp. nov. Ha sgt, cele Hue tee ey ee > er Diastoma provist Tate —XxXXXXxX-XX—XEX Turrifella (Haustator) acricula adelaidensis Cott. & Wds. — XxX--xXXKxX-xX¥---—-— Turritella (Haustator) subacricula Cott. and Wds. aii ee et ee ee i So Turritella (Ctenocolpus) triliz Cott.and Wds. _.... ve SOM oS ee oy OE Pe Turritella (Colpospira) platyspiroides sp. nov. abe Peg t oe OM ay eth Turriiella (Peyrotsa) murrayana subrudis ig & Was. ee NS en ee ee Glyptozaria spectabilss sp. nov. Pe we amet Se Archilectonica (Discotectomca} qoounonensis UT. Woods) WX Boo See oe tee Tenagodws australis (Q.& G.) wid dae ha mm oc x foe to eS xx Obtertio liratus Lud... ~~ te ae eRe Sea eee ew Batillaria (Zeacumantus) diemenensis., (Q. &G) divde tae na a eS Se tae as ee Batillaria (Zeacumantus) multilirata (Lud.) ee be SH He SS KEo--- Batillania (Zeacumoanius) bsvaricata (Lud,) wet cre ORK oe US xo-=- Batillaria (Batillariella) estuarina (Tate) .-. a. fa fins Ee me ep ee ee Manulona orrugosa Lud. at, Adelacerithium meruitun Lud. fot WT petp jee Ghent tae 2g SS es a Diala (Mereldia) incommoda (Lud.) fee —egh oe thoi ea oe Loo Ha te Rittium (Semibittium) subgranarium sp. nov. ee ag Se ge Se Be ge os oe Ee Thenciwm (subg. n. ov.) adelaidense How. and Crit e sauas PSE aban popended ee x-.x-+ Thericium (subg. n. nov.) pritchard: (Harris) oo. 0 wa Ke Thericiume (subg. n. nov.) fallax (Lud. ) ths weg ee IE Se le ae ee Se Sentvertagus capillaius Tate .... a Rie eal pee) en IG RE ee , Tlypotrochus semiplicaius sp.nov. ,,, we ee Oe ee ee Ke Cerithiella (subger. nov.) trigemmata Chap. ‘and Cres, im =e oS Se ee Cervithiella (subgen.noy.) perelongata (Lud.) wed | ee ES Kile ee ee Cerithiella (subgen. nov.) supérspiralis sp, nov. wu wm eH ee Triphora (Isotriphora) salishuryensis sp. nov. wm ee KIS eH ee Amaea (Amaea) triplicata (Tate)... eee ee KE ee Cirsatrema (Dannevigena) sp. By aed) eds > ote, eg BUR Se ea oe Scala (Hirtoscala) sp. .... vere ga See eee eee ee eae Melanella ( Margineulisna) longiconica (Lud. ,) veee eich. Qty Soe ce ee i ee Melanella (Margineulima} minuticonia (Lud.} we KH He ee Letosivaca (Leiosfraca) acutissima Sowerby |... wee ae ee ae Se x—-=+- Niso psilaT. Woods — ... syne Abate ASR ie” 6 PK ES Che lee — Syrnola (Syrnola) tincta ‘Angas. an leh OO, ER Se eet S ee he ely Symola (Agatha) praefasciate sp, nov. wi othe ee KH He Svrnola (Agatha) jonesiana (Tate) sb bet oe HE A ee ee ee - Syrnola (Agatha) infrasuleata (Tate) nn ant Cte gee es ep te ee x—-—-—a Syrnola (Pupasynnala) tasmanica T, Woods sk wah tee Sh RE ee, Sy ee en es = Syrnola (Puposynnola) acrisecta- Lud. nbs vo we ee Ko So eg oS Symnola (Euelynella) adelaidensis Lud. Mite aati ee I ee eh ee ee Kon -— Turbonilla ( Turbonslla) mariage T. Woods 0 un ae KH ey Turbenilla (Chemnttzia) mappingae sp. nov. mm me = X¥X---H------—-- Turbonilla (Chemnitsa) wurongae sp, nov, ap at ee Ee x-+-+-- Turbontile (Chemnitsia) subfuscaLud, — .... SPECIES BORE Turbonilla (Chemnitzia) adelaidensis sp. nov. 3 Turbonilia (Chevsnitsia) ourrongae sp. nov. Turbonilla (Chemnttzia) widningae sp. nov. Turbonilla (Chemnitzia) sp. .... Turbonilla (Pyrgalampros) vixcosiata Lud. Turbonilla (Pyrgiscus) “liraecostata” T, Woods... Turbonilla (Pyrgiscus) radtcans Chap. and Cres. .... Cheilea adelaidensis Lud. PUM ane Hipponys (Sabta) conica (Schum.) Cerithioderma cf. accrescens (Tate) Capulus circinatus Tate 7 ae ost Calyptraea (Sigapatella) crassa Tate’ ote ley Crepidula (Zeacrypta) immersa Angas odd ones Crepidula (Zeacrypta) dubitabilis Tate site ken Crepidula (Zeacrypta) hainswortht Jakins, _— Tylospira coronata marwicki (Fin.) fics thee Proterato (Cypraeerato) subaustralis sp. nov. Aes Ellatrivia wirrata Lud, tispe isi { | | I | | * ' | { | | * 4 | “ fl SPECIES BORE 63 Olivella (Cuptdoliva) nymphalis (Tate) Ancilla (Baryspira) tatei Marwick 10.0 sus Ancilla (Turrancilla) adelaidensis sp. nov, Austromitra angusticostata Lud. lustromitra mawsont sp. nov, ee ee veee Peery a = aes . a ee sae etse wes ome MO mes we ee aia i es ae wee a, _ os: —_—- Be — ee Ke Ke ee ee = rte otee we |= XS —-— —- — — NM a SS) as ie Perry peas anes eens — —- F-—-— ee — —- ee ee a a. nese suse wan = X X —- —- —- —- — — xx nee see esos = K— — | ee eS ei Se . ae asee i a rn eee i wees oe —~ Xe ee RH Ke —_ Ke ee — vase euee i x—_-—— = ny asee woos eaes oe — Xe — i i re ie ee ie Ee < wees ance oe = XXX -—- -—-— - — = xX—_w_=— = seep 24 owe =—- Xe — —-— —- — — x—--—--—- oy sane fore owe — X X —- — —- — — — Xe — = = a soe oven we — XS — ee eee + sen tore = =X see ese Se eee ew = = than those tabulated. *From borings other 63 ACKNOWLEDGMENTS © The writer is very greatly indebted to Dr. L, R. Cox of the British Museurn (Natural History) for most generous help and advice throughout the work; to the Director and Trustees and to Mr. W. N. Edwards, Keeper of Geology of the Museum, for permitting most of the work to be undertaken there; to Dr. W. J. Rees and Mr. G. L. Wilkins of the mollusca section and te the librarians in the general, geology, and zoology libraries of the Museum for assistance in the search for material and literature; to Drs. Thorson and Lemche of the Uni- versitetets Museum, Copenhagen, for the generous loan of type specimens; to Monsieur A. Chavan and Dr, Myra Keen for help with the classification of diffi- cult groups; to the Director of Mines, South Australia, for the loan of the typescript of portion of a bulletin im the press on the Hydrology of the Adelaide Basin; and to Dr. M. F-. Glaessner for the loan of additional material from the Tate Collection. REFERENCES Benson, W. N. 1911 Note descriptive of a Stercogram of the Mount Lofty Ranges, South Australia. Trans. Roy. Soc. S. Aust. 34, 108-111, pls. 20, 21 Cuapman, F, 1916 Cainjozoic Geology of the Mallee and other Victorian Bores: Rec, Genl, Surv. Viet, 3, (4), 327-430 Crapman, F., and Cresprm, IT, 1935 Foraminiferal Limestones of Eocene Age from North- West Division, Western Australia, Proc. Roy. Soc. Vict, 48, (1.s.), (1), 55-62 Cravan, A. 1949 Remarques sur la signification climatique des Mollusques marins fossiles. Bull. Soc. Geol. France, ser. 5, 19, (7-9), 507-512 Cortow, Th, C. 1947 Some Tertiary Molluscs from the Adelaidean Stage (PHocene) of South Australia. Rec. .S. Aust. Mus., 8, (4), 653-670 Cox, L, R. 1948 Neogene Mollusca from the Dent Peninsula, British North Bornes, Schweiz. Pal. Abhandl., 66, 1-70, pls, 1-9 Cresvin, J, 1943 Stratigraphy of the Tertiary Marine Rocks in Gippsland, Victoria, Comm. Aust, Dept. Supply and Shipping, Min, Res. Surv. Bull, 9 ¢ Pal. ser. 4). (Processed) Crespin, I, 1950 Australian Tertiary Microfaunas and their Relutionships 10 Assemblages elsewhere in the Pacific region. Journ. Pal., 24, 421-429 Cresprn, I and Corron, B, C. 1952 The Stratigraphy and Palaeontology of the Sub- surface Deposits of the Adelaide Plains, $, Aust. Dept, Mines Geol. Surv. Bull, 27, Appendix III, 227-238 Davies, A, M. 1934 Tertiary Faunas, 2 Fenner, C. 1930 The Major Structural and Physiographic Features of South Australia. Trans. Roy. Soc. S. Aust, 54, 1-36 Freminc, C. A. 1944 Molluscan Evidence of Pliocene Change in New Zealand. Trans, Roy. Soc. N,Z,, 74, (3), 207-220. Two text figs. Guagssner, M. F, 1951 Three Foraminiferal Zones in the Tertiary of Australia. Geol, Mar. 88, (4), 273-283 Han, T. S, and Prircwarn, G B. 1902 A suggested Nomenclature for the Marine Ter- tiary Deposits of Southern Australia, Proc. Roy. Soc. Vict, 14, (2), 75-81 Howcurn, W. 1914 The Evolution of the Physiographical Features of South Australia. Rep. 14th Meeting Aust. Assoc. Ady. Sci,, Melb., 1913, 148-178, pl. 3 Howeurn, W. 1923 A Geological Sketch Section of the Sea-Cliffs on the castern side of Gulf St. Vineet, from Brighton to Sellick’s. Hill, with Descriptions. Trans. Roy, Soc, S, Aust., 47, 283-315 Howenrm, W. 1928 The Building of Australia and the Succession of Life, pt. ii, Handb. Brit, Sci. Guitd Howcurn, W. 1929 Geology of South Australia, Ed. 2 HowcHin, W. 1935 Notes on the Geological Sections obtained by several Borins sitiated on the plain between Adelaide and Gulf St. Vincent.,, pt. i. Trans. Roy. Sec, §, Aust., 59, 68-102 Howcarn, W, 1936 Lt. i, Cowandilla (Government) Bore, Trans. Roy. Soc, 5. Aust, 60, 1-34 Howcuis, W., and Parr, W. J. 1938 Notes on the Geological Features and Foraminsferal Fauns of the Metropolitan Abattoirs Bore, Adelaide. Trans, Roy. Soc, 5. Agist., 62, (2}, 28?-317 Kremer, W. C, and Stoss, L. b, 1951 Stratigraphy and Sedimentation. Freeman & Co. San Francisco 64 Lupsroox, N. H. 1938 The Stratigraphical Position of the “Adelaidean” Beds of PHocene Age, beneath Adelaide, South Australia. Aust. N.Z. Assoc. Ady. Sci., 23, Auckland Meeting, 442-446 Luvsroox, N, H. 1941 Gastropoda from the Abattoirs Bore, Adelaide, South Australia, together with a list of some miscellaneous Fossils from the Bore. Trans, Roy. Soc. S. Aust., 65, (1), 79-102, pls. 4, 5 Martin, K. 1914 “Wann ldsste sich das Gebiet des Indischen Archipels von der Tethys?” Samml. Geol. Reichs. - Mus. Leiden, ser, 1 9, 337-355 Marwick, J. 1925 The Indo-Pacific Element in the Marine Tertiary of New Zealand Verh. Geol. Mijnb. Genvolsch (Geol. Ser.), 8, 369-377 Marwick, J. 1929 Geological Evidence of Past Land Connections of New Zealand. N.Z. Journ. Sci. and Technol, 11, (3), 202-206 Mawson, Ye Se R. C. 1950 Subdivision of the Adelaide System. Aust. Journ. Sci., 13, (3), 69-72 Mires, K. R. 1952 Geology and Underground Water Resources of the Adelaide Plains Area. S. Aust. Dept. Mines. Geol. Surv. S. Aust. Bull. 27 Parr, W. J. 1939 Foraminifera of the Pliocene of South-Eastern Australia. Min, and Geol. Journ. Vict, 1, (4), 65-71 Secnit, R. 1940 Geology of Hallett Cove and District with special reference to the Dis- tribution and Age of the Younger Glacial Till. Trans. Roy. Soc. S. Aust. 64, (1), 3-44, pls, 1-3, 1 map Srvcieton, F. A. 1941 The Tertiary Geology of Australia. Proc, Roy. Soc. Vict, 53, (1), (ns.), 1-125, pls. 1-3 Spricc, R. C. 1945 Some Aspects of the Geomorphology of Portion of the Mount Lofty Ranges. Trans. Roy. Soc. S, Aust., 69, (2), 277-302 Tarte, R, ewe Notes on the Tertiary Strata beneath Adelaide, Trans. Roy, Soc. §. Aust, 5, 40-4. Tate, R. figs On the Discovery of Marine Deposits of Pliocene Age in Australia, Trans. Soc. S. Aust., 13, (2), 172-180 ‘Tate, R. i800 The Stratigraphical Relations of the Tertiary-formations about Adelaide, Fite fxeal reference to the Croydon Bore. Trans. Roy. Soc, S. Aust, 13, (2), Tarr, R. 1889 On Deep-seated Eocene Strata in the Croydon and other Bores, Trans. Roy. Soc. §. Aust., 22, (2), 194-199 TATE, R,, and DenNANT, J. 1896 Correlation of the Marine Tertiaries of Australia. Pt. iii. South Australia and Tasmania. Trans. Roy, Sec, S. Aust,, 20, (1), 118-148 Unacrove,, J. 1], F. 1930 Tertiary Sea-Connections between Europe and the Indo-Pacific Area. Fourth Pacific Science Congress (Ratavia-Bandoeng), Wenz, W, 1938-1944 Gastropoda, Pts. i-vii, Handb, der Palaozool., 6 ANOTHER NEW SPECIES OF BOYDAIA (SPELEOGNATHIDAE; ACARINA) FROM AUSTRALIA BY H. WOMERSLEY Summary A second species of Boydaia (Speleognathidae) from Australia is described. It was found freeliving with cetoparasitic mites on a rat from Mount Glorious, Queensland. 65 ANOTHER NEW SPECIES OF BOYDAIA (SPELEOGNATHIDAE; ACARINA) FROM AUSTRALIA By H, Woscersiey * [Read 9 July 1953] SUMMARY A second species of Boyduiw (Speleognathidae) from Australia is described. It was found Sreeliving with cetoparasitic mites on a rat from Mount Glorious, Queensland. While my previous paper (A new gets and species of Speleognathidae (Acarina), from South Australia, Trans. Roy. Soc. S, Aust., 1953, 76, 82), was in the press, another new species of Boyduia was discovered amongst a lot of Trom- biculid and Laelaptid mites collected from a rat, Rettas asstmilis, from Mount Glorious, Queensland, on 6 August 1951 by Dr. F_ H, Derrick. Unfortunately it was represented only by a single specimen, but while being closely related to Boydaia striatus (Crossley), it is abundantly distinct in many characters. While all previously known species of Speleognathidae, except Speleognathus australis Wom, are parasitic in the nasal secretions of birds and frogs (S. australis will probably be found to affect birds also), the occurrence of this new species externally on a tat is probably accidental and not natural. Boydaia derricki sp. n, Descriplion—Female. Shape elongate ovoid, widest between coxae II and I1I. Length of idiosoma 780«, width 520z. Gnathosoma visible from above 104 long. Dorsum with longitudinal and transverse punctate striations as figured, with 20 short stout ciliated or bush-like setae, arranged one small one 5p tong in front of each sensilla, then two rows of 4 ta Su long, two rows of 2 and a row of 4 to 8n long. and then 2, 11p long. Sensillae filamentous, but ciliated, appearing slightly thicker distally, 282 long, On the anterior margin m front of each sensilla is a small but distinct lens. Palpi 3-segnrented, all segments free from gnathosoma; the basal segment dorsally on the inside carries a long slender apparently shortly ciliated seta, on the second and third segment a short bushy seta; ventrally the third segment carries three short bushy setae, The basal seg- ment of the chelicerae basally bears two short bushy setae and the apical segment appears as a lobe-like structure without teeth. Venter: sttiate punctate; coxae in two groups widely separated; with strong subcuticular reticulations; coxae I with two short, 5» bushy setae, I[-1V with one such seta, Between coxae II a pair of short 5, bushy setae and a similar pair between coxae III and between coxae IV, Genital slit 48» long, forked posteriorly and flanked on each side by three setae 5u long; on each side of anus a seta 8 long, and posteriorly a pair of setae 124 long. Legs stout, length including coxae but excluding claws, 1 520, IT 480n, ITT 430u, LV 455y, furnished with short bushy setae, which on tarsi reach 14 in length; claws strong and curved to 52 long, with a bushy hair-like pulvillus in between; segments of legs longitudinally finely striate punctate. Lecality and Host—One specimen collected on Rattus assimilis, Mount Glorious, Queensland, 6 Atigust 1951 by Dr. E. H. Derrick. Remarks—In the presence of distinct eyes and striated cuticle, this species is tlose to B, striatus (Crossley), It differs, however, in its more elongate shape, in having only three setae on each side of the genital opening, in lacking the fine simple setae on the legs as figured by Crossley for striatus and in relatiyely stonter legs. “South Australian Musetn pane Roy Soc, S. Aust,, 77, July, 10354 ry f CRON oe D TAK ys ae, IS) _« Boydaia derricki n. sp. A, dorsal view; B, ventral view; C, left eye and sensilla; D, dorsal view of gnathosoma and palps; E, ventral view of gnathosoma and palps; F, dorsal view of tibia and tarsus of leg I; G, ventral view of tibia and tarsus of Jeg I. REFERENCES Boyp, Evizaneto M. 1948 0-68 1-53 + 0-49 18-2 —28-1 22-4 — 25°2 65 PSB » 20-70-48 1*53- 0-49 16-1 —25-2 19-6 22-4 7+4 SD - 44-241-37 3+D7 + 0:97 35° —53-2 42-0 — 47-6 69 A-P - 28-0 No variation recorded AM - 27:4+0-56 1-25+ 0-40 23°65 — 31-15 28-0 —25-2 4-6 AL -~ 21°820-56 1-25 0-40 18-05 — 25-55 19-6— 22-4 5+8 PL - 40-34 0-68 1-53= 0-49 35:7 —449 39-2— 42-0 3-8 Sens. - 430-8 with head 16-8x 19-6, Only 1 determination Loc. and Host—Five specimens collected on Rattus assimilis at Mt. Glorious, Queensland, 6 August 1951 (coll. E. H. Derriclr). Remarks—Like precana sp.n., the above new species will also run down (0 couplet 39 containing cocrongense Hirst from which it differs in the differently shaped and very much smaller scutum, as well as having the seta on the palpal genu nude. From procana sp.n. it differs in the smaller number and different structute of the dorsal setae as well as having only the femoral seta of the palpi branched. In two of the four specimens the scutal margin runs inside of the PL seta base, which can ‘thus be said to be “off” the scutum. This incipient development again stresses the view that the off-scutal position of PL within the genus Euschéngastia should not be used to create other genera as has been done by some workers, Euschongastia procana sp. n. Fig. 7 A-E Description of Larvae—Shape oval. Length of idiosoma (unengorged) 273u, width 195y. Scutum as figured; posterior margin deep behind line of PL, and slightly concave medially; anterior margin sinuous; scutal setac long, tapering with slender denticles; AL the shortest, PL the longest; sensillae globose with setules. Eyes 2+ 2, on ocular shields, posterior the smaller, Palpi moderately stout; setae on femur and genu ciliated or branched; on tibia, dorsal and lateral nude, ventral branched; tibial claw trifurcate, Chelicerae simple with only the apical tricuspid cap. Galeal setae nude. Dorsal setae with slender denticules, 68. in nunber and arranged 2.10.14.18.12.6.4.2, to 53u long, except humerals which are 78 Fig. 7 Euschongastia procana sp. n. A, dorsal view; B, ventral view; C, scutum (x 500); D, palp; E, dorsal seta 62p long. Ventrally, a pair of ciliated setae on maxillae, one on each coxa, a pair between coxae I and between coxae III, and thereafter 12.8.6/8.6.4.2, to 28p long. Legs 7-segmented, I 299p, Il 247m, III 286 long; specialised setae on leg I, 2 genualae, 1 microgenuala, 2 tibialae, 1 microtibiala and on tarsi, 1 sensory tod, 1 microspur, 1 subterminala, 1 terminala; on leg IT, 1 genuala, 2 tibialae, and on tarsi 1 sensory rod, 1 microspur; and on leg III, 1 genuala, 1 tibiala. 79 Fig. 8 Euschongastia andromeda sp.n, A, dorsal view; B, ventral yiew; C, scutum (x 500) of type of specimen; D, scutum (x 500) of paratype specimen; E, tip of chelicera; F, palp; G, tibia and tarsus of leg IIL. 50 The Standard Data for the type and 1 paratype collected on card are :— Standard Theoretical Observed Coeff, of Mean Deviation Range Range Variation AW - 56:0 No variation recorded PW - 81-2 No variation recorded SB - - BO+0-99 1+4+0-7 23+8 — 322 26-6 — 29-4 5D ASB ~ 26:620-99 1-407 2274 —~30°8 25:52 — 28-0 53 PSB - 22-4 No variation recorded SD - - 46-0+0-99 1-4+0°7 44-8— §3-2 47-6 — 50-4 2-9 AP- - 280 No variation recorded AM - - 47-6 No variation recorded Al, - - 39-2 No variation recorded PI. - - 61-6 No variation recorded Sens. - 37-8+0-99 1-4+0-7 33*6 —A2+1) 4G+4 — 39-2 3-7 with head 22-4 5 19-6 Loc. and Host—Two specimens collected on card at Mt. Jukes, Queenstand, 6 September 1951 (coll, E. H. Derrick). Femarks—In Womersley’s key (1952, p. 236) this species runs down to couplet 39, along with coorongense Lrst, from which it differs markedly in the more denticulate scutal and dorsal setae, the much greater number of dorsal setae, and in having the ventral seta of the palpal tibia branched, as well as in the smaller scutum. Euschongastia andromeda sp.n. Pig. 8 A-G Descripiton of Larvae—Shape oval. Length of idiosoma (unengotged) 274p, width 182», Scutum as figured; nearly twice as wide as deep; posterior margin very shallow behind line of PL, and slightly concave medially; anterior margin sinuous; SB in front of PL; scutal setae long, tapering and ciliated; AL the shortest, PL the longest; sensillae globose with setules, Eyes 2+ 2, on ocular shields; posterior the smaller. Palpi moderately stout; setae on femur and genu branched or ciliated; on tarsi dorsal and lateral nude, ventral branched; tibial ¢law trifurcate. Cheliccrae simple with apical tricuspid cap, Galeal setae nude. Dorsal setae 44 arranged 2.8.8.8.10.4.2.2, to 36 long, except humerals which are 42, long, Ventrally, a pair of ciliated setae on maxillae, one on each of coxae I and JI, two on coxae [1I, a pair between coxae I and between coxae III, and thereafter 6.64/2.6.6.2.2, to 31 long. Legs 7-segmented; specialised setae on leg 1, 2 genualae, 1 microgenuala, 2 tibialae, 1 microtibiala, and on tarsi, 1 sensory rod, 1 microspur, 1 terminala; on leg II, 1 genuala, 2 tibialae, and on tarst i sensory rod, 1 micruspur; and on leg III, 1 genuala, 1 tibiala, also on tibia 2 very long but basally ciliated setae and two similar ones on tarsi. The Standard Data derived from the type and 1 paratype are:-— AW 74-2, 67:2; PW &86°8, 81:2; SB 29-4, 28:0; ASB 28-0, 28:0; PSB 11-2, 14-0; SD 39°2, 42-0; A-P 36°4, 36°4; AM 42-0, 42:0; AL 33:6, 33°6, PL 56-0, 56-0} Sens. 39-2, 39-2 with head 22-4 x 19-6. Loc. and Host—Two specimens collected on card at Mt. Tamborine, Queens- land, 14 May 1952 (coll. E, H. Derrick). Remarks—tIn having 2 setae on coxae [II this species is closely related to petrogae Wom., in couplet 29 of Womersley’s key 1952 on p. 234. It differs, however, in the fewer and different dorsal setae as well as the Standard Data, and the shape of the scutum. The setae on the palpal femur, genu and tibia ventral are only sparsely branched. However, more characteristic are the long but basally ciliated setae on tibia and tarsi of lee IEL The Standard Data of the paratype are somewhat higher in AW and PW than in the type, probably due to undue compression. THE ECOLOGICAL SURROUNDINGS OF THE NGALIA NATIVES IN CENTRAL AUSTRALIA AND NATIVE NAMES AND USES OF PLANTS BY J. B. CLELAND AND N. B. TINDALE Summary This paper describes the physical features and the vegetation of the region occupied by the Ngalia aboriginal people, some 200 miles north-west of Alice Springs. The native names and uses of various plants are recorded. 81 THE ECOLOGICAL SURROUNDINGS OF THE NGALIA NATIVES IN CENTRAL AUSTRALIA AND NATIVE NAMES AND USES OF PLANTS By J, B. Creranp and N, B. Tinpace {Read 9 July 1953] SUMMARY Tats paper describes the physical features and the vegetation of the region occupied by the Ngatia aboriginal people, some 200 miles north-west of Alice Springs. The native hames and uses of various plants are recorded. The Sixteenth Anthropological Expedition, organised by the University of Adelaide to study the natives, left Adelaide for Alice Springs on 10 August 1952. The Expedition was financed by a liberal grant from the Wenner-Gren Corpora- tion for Anthropological Research Incorporated (previously the Viking Fund) of New York, supplemented by substantial assistarice from the University of Adelaide and its Board for Anthropological Research and from the South Aus- tralian Museum, and by transport facilities granted by the Commonwealth and State Governments. On arrival at Alice Springs the Expedition proceeded by motor yehicle to Yuendumu, on the track to the Granites and situated 192 miles to the north-west of Alice Springs. During its stay at this Government Station for Natives, inten- sive work was carried out on many aspects of native life, including a study of theit sutroundings and the uses made of plant substances. This paper contains a general account of the country and is followed by a record of the native names for various plants and the uses made of ther. DESCRIPTLON OF THE COUNTRY NOW OCCUPIED BY THE NGALIA PEOPLE CENTRED ON YUENDUMU These people are still within their tribal limits and occupy the area where their mythical ancestors lived and were transformed into natural features. The country consists of extensive plains, traversed at intetvals by occasional water courses, now dry, which after heavy rain in Jantiary and February must be torrents almost deserving of the name of rivers. Such a one is Cockatoo Creek. These are fed by smaller subsidiary channels taking an irregular cotirse from the rocky hills and even rugged mountains which form irregular ranges breaking up the plains, sometimes into narrow stretches but often into areas of many miles in extent. The soil is a sandy loam, very boggy in places alter rains, some- times more sandy so that trucks dig in deeply, and covered with small pebbles as one approaches the hills. At the base of these hills the stones become larger and on their lower slopes become small or large boulders strewn irregularly up the sides and making climbing laborious. The flat countty known as. Ngalia plain, forming the southern portion of the tribal area, is a shallow synclinal basin filled with sand and loam, underlying which are quartzite beds containing rounded waterworn pebbles and other evi- dences of a shallow water origin. They outcrop along the northern edge of Butt Plain and at Central Mount Wedge with a northerly dip and appear again at Ngama near Mount Eclipse and at Cockatoo Creek with a southerly dip. These littoral beds are underlain by granites and metamorphosed old rocks. The granites form great domes at Mount Doreen and Mount Hardy, and associated igneous rocks form the many jagged hills around that area. The grain of the country is east and west but the streams tend to run across it. They are thus consequential, some passing through the grapite areas from ers Rey Soc. S, Aust,, 77, July, 1954 &2 south to north, including the Lander and Cockatoo Creeks, while others, includ- ing Gidgea Creek, which liey near the eastern boundary of the tribal area, cut across from north to seuth to fill a long series of salt Jagoons and salt marshes, which together form att ancient river valley on the Burt Plait: and trending away west towards Lake Eaton. These salt marshes form the southern boundary of the Ngalia tribe between Tilmouth Well and Mount Cockburn, On the plains occur the red kangaroo {Macropus rufus) whose young “fying does” are blue, the emu, and the bustard (“native turkey”); on the hills the euro (M. rebustus) and a wallaby. The yegetation on the plains consists essentially of mulga (Acacia ancura and A. spp.) in dense thickets in places, making progress between these small trees in a car a difficult matter, but usually in a more open arrangement inter- spersed with shrubs and small trees, and sometimes quite scattered, diversified hy grassy patches a few acres or a mile or so im extent, with or almost without scattered shrubs. The grassy patches often constst of Triodia, so-called “spinifex,” probahly m the poorer sol, or of various other species such as colonies of kan- garoo grass (Themeda eustralis) and the taller and more robust tussocky Th. evenacea (often in boggy places), and elsewhere smaller grasses such as species of Enneapogon, Aristida, Triraphis mollis and Eragrostis. The rocky hills show a wealth of species, commencing as the ground begins to mse near their bases and is covered with the tessellated smaller fragments of disruption, Native pines (Callifris) present a picturesque appeatance amongsi the rocks, native figs (Ficus platypoda) may scramble over many boulders, a hill type of mulga occurs, there are several Eremophilas, species of Aracia peculiar to the slopes or the rising ground at the base, one of which has phyllodes like a Lycopodium, a few small, often strongly scented and sticky composites, some with yellow flowers, and several species of Goodeniaceae, some quite handsome with blue or mauve or yellow flowers. Prickly Yriodia tussocks sparsely oveupy the intervals and may reach formidable proportions in the better soil round the base of the hill. The picturesque white boles of the ghost gum (Ewe. papwana) and the tessellated trunks of bloodwoods( Ettc, ternrinalis?) are scattered on the slopes or adjacent plains. The waters in this country consist of rockholes in the bills, or oecasional soaks on the plains, or waterholes left in the creeks and rivers after floods, Their presence is often indicated by flocks of chestnut-eared finches (a sure indication of their proximity) and by the relative abundance of other small birds. As rain may not fall for many months, as for instance between May and November, the smaller rockholes, and those unshaded and shallow, and the soaks tend to dry up and the natives become dependent on the larger more permanent supplies. This, of course, means that much of the larger game is also restricted to the neigh- hourhood of these remaining waters and so may be decimated, and that any vegetable and insect foods still available (such as roots and “witchetty’ grubs) tend to be eaten ont, The vegetable food supplies consist of fruits, of grains and seeds which are winnowed, pounded, and made into dampers, of roots and tubers, of occastomal leaves and pods (such as those of Marsdenia australis), of honey-bearing flowers as, for example, those af the corkwoods (Hakee spp.) of which there are four species, and of galls on Acacias. ; Of the fruits the most important are the native peach (Eucarya ceumeinala) which occurs in the area, the native plum (the pltim-coloured smaller fruit of Santalum lonceolatum), the currant-like Emits of Carissa Brownit {Apocytia- ceac) growing in little colonies near the banks of water courses, the currants of the broad-leafed Plectronta latifolia which occurs as scattered tall shrubs amongst the wulga, of the fruits of several species of Solatwm, native figs (Ficus ploty- foda) growing amongst rocky hills and having fruits like small Moreton Bay 83 figs, the fruits ef Capparis Mitchellii (native pomegranate} which species is widely distributed but not abundant, and the little cucumbers of Cicumis Melo var. agrestis (which we did not see), The little “tomatoes” of the various Solanums are much relished, We met with several species af which one, S. petrophitim, with Jarge blue flowers and upright detsely prickly stems which bear small yellowish to whitish tather dry fruits, is not eaten, Another spectes, S. ellipticum, rather like this in upright habit but with fewer prickles and with fruits becoming greyish-green is eaten, Near Mount Eclipse another very prickly species (S. phlomoides) with large fruits whose stalks become recurved has edible fruits and on rocky hills still another has its pale green tomatoes on the underside of the spreading almost prostrate stems, A common edible species on the plains with very few prickles may be a new species and another prickly species with prostrate stems and quite small flowers has sweet-tasting somewhat yellowish fruits. There are thus in this region five species at least of Solantin whose fruits are sought after as feod. Summed up, as regards the fruits available to these people, it may be said that some such us the native peach may yield a con- siderable amount of fruit capriciously and for a short time; that the two currants in season may supply a certain amount of food that requires time for gathering; that the fruits of Samtelwm are not numerous and the shrubs not in great quantity; and that the Solanums yield in their season a moderate amount of fresh fruit, The fruits in fact do not constitute an important source of food but are valuable adjuncts. The grains and sceds available are mostly small but in such abundance that enough can he collected to form a valuable addition to the diet. The grains seem to be derived from panic grasses, and as with other small seeds are winnowed by rocking to and fro in a wooden or bark dish. The common purslane (Portulaca oleracea) is a prolific yielder of minute seeds and so are some of the “mouse-tail” Chenopodiums of which we found one species. Various Acacia seeds are gathered and even the small seeds of the Coolabah (Eucalyptus microtheca) and of E, gamophylla may be utilized where these trees are available. The seedling shoots of the coral tree (Erythrina vespertilio), winch occurs in the district, are also eaten. Nearly 250 species of plants were collected and the following notes deal with about 60 of these of anthropological interest. GRAMINEAE Grasses Stich as Andropogon exaltatus (a lemon-scented grass) and Aristida sp., both tall species of similar habit, also Panicum decompasitum, native name ‘kalbal’bi. Seeds of the latter are termed wan:a wan:a-tatba = dish-gathered grain and are gathered, husked and ground between stone mills to make a damper bread. Nzgalia. Aristida, browniana (= stipoides), a small tussocky grass, ’jepere. No use. Enneapogon nigricans, "jepere. No use. Triodia pungens (porcupine grass, often called “spinifex”). from which “gun” was obtained, mana. 7. pungens is also catled ’mananknara, Ngalia. CYPERACEAE Bulb of Cyperits bulbosus, ‘jalka. Is eaten, Ngalia, CASUARINACEAE Casuarina decaisneana (desert oak). ’kurukara, jirkali (see Eucalyptus termina- lis), Grows in the desert sandhill country; yields a “honey,” wama jurukara (in hot weather), probably a species of lerp. Ngalia. PROTEACRKAR Hakea lewcaptera (neediebush), maro-okullba. Not used. Grevillea striata. (beefwood), ‘ildi:lba. Not of use to the aborigines, 84 Santalum lanceolatum (native plum), ‘marukiri, mokaki, me:kari, ‘merkari, The fruit is considered to be good food, Negalia, LORANTHACEAE Loranthus Exocarpi on Eremophila sp. and on Grevillea striata (beefwood), flowers red or yellow, the fruits which ate eaten red or black are called jamilbiri, L. maidenii probably, a hoary grey mistletoe on Acacia spp,, narankiri. The grape- like fruits are eaten. This is the food plant of the butterfly Ogyris hewitsoni parsonst, Angel, CHENOPODIACEAE Kochia sp., ’kaiparu. No use is made of it. Ngalia. AMARANTHACEAE Philotus (Trichinium) obovatum, wanaparnaba. Used to line a wooden dish when carrying a child. Ngalia, Pt. alopecuroides (or Pt, nobile), ’walpa’ralpuri. No use. Ngalia. Gomphrena brownn. The petianth segments, which are densely woolly outside, are used as “down” for ceremonial purposes. This downy material was identi- fied for us by Mr. R. V. Smith of the National Herbarium, Melbourne, PorTULACACEAE Portulaca oleracea, wakadi, also ’manjaru. The women gather the fine seed, ’wakadi ‘nula, for food and grind it between stones. Negalia, NycTAGINACEAE Boerhavia diffusa, ’waibi. The natives eat the root which may be large; it is a good food. LEGUMINOSAE Acacia notabilis, "mandala. A lerp scale on the leaves and stems is eaten. Ngalia. A, ligulata, ‘wardaruka. Not used. Ngalia. A. aneura, s. lat. (mulga), ‘mandja. Negalia. A, anewra, (mulga), ‘mandja, The seed ‘nuluparu. Ngalia; ‘wanari. The seed, ‘kaijura, Pintubi. A. kempeana (witchetty bush), ‘erepili, also ‘nalkiri, ‘nalkidi, ‘yalkiti. The seeds are eater and also grubs in the roots. A, cambagei (gidya), ’sidji. Al, cuthbertsoni, pi:li, pirlt. The seeds are sometimes eaten. A, sp., with long linear phyllodes, ’paykuna, also called jirkili and wakalberi. The ash from the burnt branchlets is mixed with the leaves of the native tobacco in forming the quid. Ngalia. The alkaline ash probably helps in liberat- ing the alkaloid, Cassia pleurocarpa, ‘ya:na. Children eat a small borer grub in the roots called "nalkiti ‘na:na. Ngalia. C. eremophila, ‘pundi, ’pundi ‘wari. No use. Negalia. A yam, the taproot probably of the pea Vigna lanceolata, is eaten. "Wapiti a rant species of yam, ?Vigna or an Jpomoea; galatji is also a yam and “jala. Negalia. Erythrina australis (bean tree), jinindi. The young shoot is steamed and eaten, Negalia. HKUPISORBIACEAE Euphorbia eremophila and Phyllanthus sp. have no native names, ManvackaE yam:uramjuri is a species of mallow with stellate hairs, No use made of it. Negalia. . 85 Sida sp., ‘maykur’maykurupa. Not used by the natives. Ngalia. Sida inclusa, java ‘man ja ‘man ja. Not used by the natives, Ngalia. MyrTACEAE Eucalyptus papuana (ghost gum), ‘wapinunga. The thick bark, yapiri, is stripped off and tsed in the process of making “spinifex” gum, as a yapiri pindi (bark dish). E. terminalis ? (bloodwood), tjambali, jirkala. Bark used for dishes. Negalia. E. pachyphylla, tjitilbara. The honey in the flowers is eaten. Ngalia. E. gamophylla, ’waralju, ’warilji ‘warilji. The flowers yield sweet honey, ‘qul:u ‘waralju. Ngalia. APOCYNACEAE Carissa browmii, mayari.'A prickly shrub up to six feet high, with a currant-like fruit which is eaten. Nealia, "Maninidji (manigidji) has also been noted for Carissa brownii but the description of its “plum-like brown fruits’ being good food suggests some mistake. Ngalia. ASCLEPIADACEAE Sarcostemma australis, kitjikitji. Not used. Ngalia, Pentatropis kempeana? ‘manilba, The long bean-like follicles are eaten. Marsdenia australis, 'jupali. The leaves and pods (follicles) are eaten and con- sidered good. Ngalia. CONVOLVULACEAE Evolvulus alsinoides, ‘marna. Not used, Ngalia. SOLANACEAE Solanum sp? nova (5 petals, few prickles), kararupa (Walpiri tribe), jakadjeri (Ngalia tribe). The tomatoes are good food. S. quadriloculatum (very prickly), warukalukalu. Kangaroo food, not tised by natives, Ngalia. S. sp. identified as S. ellipticum but probably a new species, eight miles west of Yuendumu, japindiri, has a pale sweet edible fruit. S. ellipticum, prostrate, with large fruits, grows amongst frocks, near Mt. Eclipse, naliljiriki, nalijiriki. Cooked, ripe or green, and eaten, also eaten by euros and wallabies. The Solanums and tobaccos were identified for us by Mr. R. T. Smith, of the National Herbarium, Melbourne. It will be seen that two Solanums which differed in habit and were given different native names were both referred to S. ellipticum., Later research will doubtless be able to separate these. S. phlomoides A, Cunn., fruits reflexed, near Mt. Eclipse, wanakitji. Tomatoes eaten. Negalia. S. phlomoides (referred to), upright about 2 feet tall, at foot of Wolfram Hill near Mt. Doreen, with big edible fruit, yandjawali. Ngalia. . Nicotiena ingulba (native tobacco), in sandy loam under Erythrina trees south of Mt. Eclipse. Used by the natives for chewing after wiltmg over a fire and mixing with the ash of paykima (Acacia sp-). N. occidentalis, near Mt. Doreen, ? yungarai. Not used. Duboisia myoporoides, a poison bush, growing on the sandhills, warkalba, Negalia, BIGNONIACEAE Tecoma doratoxylon, wenbiri or wanbiri. Wood used for spears. MyYororRAcEAE Eremophila longifolia (emu bush), galurupu. Not eaten by the matives but good emu food. Ngalia, 86 RvUBIACEAE Plectronia latifolia, tawaljurv. Fruits eaten, CAM PANULACEAE Tsotoma petraee, ’muldu. The plant may be used for chewing with ashes in the imatiner of native tobacco; is a substitute for tobacto; is a “strotig chew.” Negalia. This Jsotoma evidently contains some strong alkaloid(?), as it is spoken of by the hatives in the Musgrave Ranges about 500 miles south as “cheeky b--r". The Department of Chemistry, University of Adelaide, has been trying to obtain sufficient quantities for analysis, Tt is widely distributed in the dry interior, GooDENTACKAE Seaevold sp. and Goodenia ? sp., pala. Not used by the natives. Negalia, Geodenit ? sp., wadia, Not used. Negalia. LU nipentiFiep "Maruko. The fluffy pods (?) are used for decoration, Ngalia. Perhaps the hairy perianth segments of Gompirene brownii (see Amaranthaceae}. Kende, a large type of tree, one seen by an ancestral being iti a desert place. "Wadia, a tree. Ngalia (see Goodente sp, above, which has the same name but is a smalf undershrub). Though the localities mentioned in the following notes are widely separated from Ytiendumu and each other, this opportunity is taken of recording informa- tion about three other plants used by Australian natives, Pterocaulon (Compositae) as a substitute for native tobacco In 1940 the late Rev. J. R. BR. Love fotwatded ftom Kunmunya Mission, north of Derby, Western Australia, to the late Professor T, Harvey Johnston the leavés of a plant “used by the Worora tribe of aborigines as a substitute for chewing tobacco.” The plant has been identified as Pierocaulon glandulosum var. velutinum. (Compositae). Mr. Love goes on to say: “It is not a tobaced at all, nor is it regarded very highly by the people. It has a pungent smell, something like ‘penny royal,’ and is chewed, they tell me, when tobacco is not available. “The name of it is ‘njuni-uni. The wild tobacco, which the men tell me is to be procured in the sandstone ranges, I have never secured. It tiust be scarce there, not like the mingulba, which is so plentiful in the Musgrave Ranges. “My attention was drawn fo this yuni-yjuni by the unwillingness of ‘the women to root out a plant of it that appeared in a bed of pumpkins—seed cartied by the wind, J suppose.” “Tubers’ on the Roots of the Grass Poa drummondii In September 1952 Pastor Hoff, who was then looking after the natives recently transferred from Ooldea to Yalata, 50 miles west of Colona near the Great Australian Bight, forwarded us specitnens of grass, identified ‘as Poa Drummondi by Mrs. E. Robertson of the Waite Institute. The grass was grow- ing in a flat between sandhills and the native children dig out the “tibers” attached to the roots and eat them. These “tubers” are whitish swellings, 5 to 20 mm. long and about 3 mm. in diameter, along the course of the roots or attached to them (probably on rootlets), single or two or three separated by constrictions. The swellings are friable in textiite and have little taste but perhaps a slightly mealy one. Seeds of Stenapetalum lineare (Cruciferae) eaten Pastor Hoff also fotwarded from Yalata for (detitification specimens of Stenopetalum lneare, the seeds of which were eaten by the natives. A CARVED HUMAN FIGURE FROM THE DURACK RANGES, NORTH- WESTERN AUSTRALIA BY CHARLES P. MOUNTFORD Summary This paper records a carved human figure from an aboriginal ceremonial cave in the Durack Ranges of north-western Australia. A CARVED HUMAN FIGURE FROM THE DURACK RANGES, NORTH-WESTERN AUSTRALIA By Cuartes P, Mounrrorp * [Read 9 July 1953] SUMMARY This paper records a carved human figure from an aboriginal ceremonial cave in the Durack Ranges of north-western Australia. The fact that the Australian aborigines carve human figures in wood has been known for many years. Warner (1929) saw mortuary posts erected over the graves of the dead at Milingimbi on which “a series of incisions . . . . give it the appearance of a carved head with one or more necks.” Worms (1942) recorded carved human figures used in the Goranada ceremony of the Kimberley region of north-western Australia, Berndt (1948 and 1949) described wooden figures from Yitrkalla, north-eastern Arnhem Land, and Mountford (1953) a number of similar figures from the same locality, In 1938 the Rev. F. W. Chaseling presented a mortuary post, made by the aborigines of Yirrkalla, to the Australian Museum, Sydney. Mountford (1953) and three years later Mr. Roy Vyse presented another carved figure, from the Durack Ranges of north-western Australia (the subject of this paper), to the South Australian Museum. THE Carved FIcure Early in 1941 a drover gave Mr. Roy Vyse a carved wooden human figure which he had taken from an aboriginal ceremonial cave in the Durack Ranges, south-west of Wyndham, north-western Australia. He stated that the aborigines were rriost angry over the theft. In the same year Mr. Vyse presented this figure (A.31105) to the South Australian Museum. Plate I, B, C, and D, show the wooden figure of a woman. Her arms are part of the body, and her head turned sideways. There is a belt round her waist, and engraved body decorations across her chest, abdomen and back. These body decorations, although crudely executed and somewhat ott of position, are similar to those seen by the author on performers in the Central Australian ceremonies and those on a dancing aboriginal engraved on a baobab nut from Derby, north- western Australia (pl. i, fig. A), As there is little direct evidence associated with this specimen, the sole object of this paper is to record its existence, in the hope that it will stimulate inquiries for other examples of the carved human figure. REFERENCES Bernpt, Ronatp and CaTHertne 1948 Oceania, 18, No. 4, pl. 1, 2 Bernot, 1949 American Anthropologist, 51, No. 2, pl. 1-3 Mounrrorn 1953 “Myth, Art and Symbolism of Arnhem Land” (in press) Warner, Litoyp 1937 “A Black Civilisation,” 504 Worms, Ernest 1942 Annali Lateranensi. Vatican City. Pl. 4, 7 ne *Plonorary Associate in Ethnology, South Australian Museum. ‘Trans, Roy Soc. S. Aust., 77, July, 1954 88 rage Does I carvings. from north-western Australia. ‘ Aborigina Plate [, THE GENUS NEOTROMBIDIUM (ACARINA : LEEUWENHOEKIIDAE) I. DESCRIPTION OF THE OVUM AND LARVA OF NEOTROMBIDIUM BARRINGUNENSE HIRST 1928, WITH AN ACCOUNT OF THE BIOLOGY OF THE GENUS BY R. V. SOUTHCOTT Summary The genus Neotrombidium Leonardi 1901 has been known hitherto from only the adult and nymphal forms. This paper records the experimental rearing of the larva of the Australian Neotrombidium barringunense Hirst 1928 from eggs laid by adults. The ovum and larva of this species are described. From this larval description it is shown that the monotypic larval genus Monunguis Wharton 1938, with M. streblida Wharton 1938 as type, found parasitic on a Streblid (Diptera) ectoparasite on a bat in a cave in Yucatan, Mexico, belongs to Leonard’s genus, which has taxonomic priority. This correlation shows that the range of Neotrombidium includes Central America as well as the previously recorded South America and Australia. 9 THE GENUS NEOTROMBIDIUM (ACARINA ;: LEEUWENHOEKIIDAE) I. DESCRIPTION OF THE OVUM AND LARVA OF NEOTROMBIDIUM BARRINGUNENSE HIRST 1928, WITH AN ACCOUNT OF THE BIOLOGY OF THE GENUS By R, V. Sowtneorr [Read 9 July 1953] SUMMARY The genus Neatrombidiuin Leonardi 1901 has been known hitherto from only the adult and nymphal forms. This paper records the experimental rearing of the larva of the Aus- tralian. Neotrombidium barringunense First 1928 from eggs laid by adults. The ovum and larva of this species are deseribed. From this larval description it 1s shown that the mano- typic larval genus Monungeis Wharton 1938, with M. streblida Wharton 1938. as type, found patasitic on a Streblid (Diptera) ectoparasite on a bat ina cave in Yucatan, Mexico, helongs to Leonardi's genus, which has taxonomic priority, This correlation shows that the range of Neatrombidinn includes Central America as. well as the previously recorded South America and Australia, Further Australian records of the distribution of N, barringunense are given, the species being known from the eastern half of Australia. In the Adelaide region the adults and nymphs are found most commonly under the fresh bark of the bluegum, Eucalyplur leucorylon. Adult females lay 30-'50 eggs, average 40, at a time, and there appears to be orily one oviposition, Adult temales survive oviposition by 7-30 days. About three to four weeks is passed in the egg stage. Other aspects of the biology of the species are discussed. In 1901 Leonardi erected the genus Neotrombidium for N. furcigerum from Argentina. In 1912 Berlese added a second species to the genus, NV. ophtalmicum (sic), originally described as Trombidium ophtalmicum Berlese 1888 from Para- puay, Hirst added NV, barringunense in 1928, giving as locality iniormation, “Bar- rmgun, New South Wales, on the Queensland border, a single specimen Found by the author under the bark of a living Eucalypt.” In 1929 Hirst recorded the specics again, noting that “this species is very abundant under the bark of gum-trees on the banks of the River Darling at Menindie, New South Wales, July 1928.” In 1936 Womersley recorded this species from Long Gully, Mount Lofty Ranges, South Australia, 12 May 1934, and from Bathurst, N.S.W., 31 May 1934. In 1945 Womersley erected the family Leenwenhoekiidae for Leeuwenhoekia Oudemans 1911 and related genera, separating these trom the Trombiculidae Ewing 1944, and also from the old family Trombidiidae Leach 1815. G, M. Kohls and C. B. Philip, of the United States Typhus Commission, had succeeded in rearing three species of the genus Acomatacarus Ewing 1942 from New Guinea from larvae to nymphs, and this reared material was serit to Mr. Womersley for description. This showed that the genus Neotrombidiwm, whose larval form was unknown, had malare Fonns similar to those of Leeuwenhockia, Acomatacayus, cte., and should he placed in this family. For some years the present writer has attempted to correlate larval and adult Trombidiids (s,1,) as well as other mites, by rearing experiments, In the family Trombidiidae (s.1.) a number of genera have heen so correlated. In 1939 Womersley was permitted to describe the larvae of Chyseria and Caenothrombinm which the writer had thus reared during 1938. In 1946 the writer recorded that the ege of Microtrombidinm hirsulum Wom. 1945 hatches direct to the nymph, the larval stage being suppressed. Several other genera have been reared, these correlations at present awaiting description. From 1938 onwards the writer attempted to rear the larva of Nedtrombidium barringunense, which species is not Trans. Roy Soc. S. Aust, 77, July, 1954 0 uncommon in the Adelaide region, Technical difficulties however prevented success, and the studies were interrupted by the war. In 1948 these experiments were resumed with N. borningunense, and the larva was reared from eggs laid by adults in captivity (see later). Description of Egg. Fig. 1 A-C. Colour reddish-orange. Length 240,, width 145u. The eggs are in the deutovum stage when first laid, in fact in mounted gravid females the eggs show considerable development. When first laid the eggs are smooth and ovoid, but within a few days become very irregular from a number of protuberances, and it is this stage that is figured. This stage is more irregular than for most of the Trombidiidse (s.J.). Some of the protuberances can be identified as containing various parts of the larva. On the under-surface the projecting legs can he seen; protuberances I, II and II in fig. 1C correspond to legs I, Il and IIL. Fig. 1, A-C Neotrombidium barringunense Hirst, ovum. A,B: dorsal views; C; Sateral view. 1, I and III indicate developing legs I, If and TfL. Anteriorly the protuberances for the palpi and chelicerae are identifiable (see fig. 1. A,B), Further back on the dorsum is a large nasus, which appears to correspond to the tiastts of the dorsal scutum of the larva. Ranged around the Jateral sides and postetior pole are several blunt or pointed protuberances, of anknown function, Description of Larva, Fig. 2, 3 A-C. Colour orange. Body ovoid, as figured; length from tip of nasits of dorsal scutum to posterior end of abdomen 150, width 140, Dorsal scutum 92, long by 784 wide, roughly triangular, the apex of the triangle forwards, where the shield narrows to a blunt nasus which partly overlies the gnathosoma (capitulam), The anterolateral borders of the shield ate concave, the other borders are convex except that the posterior border is considerably flattened, Scutum with a pair of sensillary setae, long, fine, very faintly ciliated, 46. long, arising from large sensillary areolae in the posterior half of the shield; with three pairs of non-sensillary setae, the anterior (antero- median) arising on the nasus as shown, fine, pointed, ciliated, 224 long; the antero-lateral arising very close to the edge of the antero-lateral shoulders of the shield, comparatively slender, but thicker than the antero-median, with adpressed ciliations, and slightly tapering, blunted at the tip, 224 long; the postero- lateral setae similar to the aritero-lateral, arising at the postero-lateral angle of the shicld, 18y Jong. The scutum is porose over its posterior half, Eyes two an each side, sessile, situated alongside the lateral borders of the shield, the anterior eye the larger. Dorsum of abdomen with about 20 setae, similar to scutal non- | sensillary setae, only longer, 24-26« long, arranged in rows of 6,4,4,2,4, Ventral surface: attached to the posteromedial angle of coxa I is a long pointed sparsely ciliated seta 35a long; between coxae III is a pair of similar setae, 30p long; behind coxae II are three rows of setae, long, pointed, sparsely ciliated, 40+ \ ee ae SOUTHCOTT Fig. 2 Neéotrombidium barringunense Hirst, larva. Dorsal view, entire. long, artanged in rows of 2, 4, 2; in addition there is a shorter poitited seta, with a few similar pointed ciliations, 164 long on each side of the anus. Coxae I and II are contiguous on each side, with the usual stigmal opening (utstigma) betweén them. Goxaé I and III show a recticular porose patterning in their lateral halves, net present on coxa II. Toward the anterolateral angle of coxa I arises a long pointed strongly ciliated seta 40» long; on coxa II is @ similar seta 5a long; on coxa III similar, 424 long. Legs of norinal length, leg I 245p long, 92 TI 245,, III 265, (all lengths include coxa and claw). Each tarstis of the legs with a single strong falciform claw. Setae and spines of legs as figured. Tarsus I and II are provided on their dorsal surface with a solenoidal spine. Tarsi with- out Haller’s type organ. Tarsus I stout, 54p long by 23n high. Metatarsus I stout, sinuotis, 38. long. Gnathosoma (capitulum) compact. Basal segment of chelicera loop SOUTHCOTT Fig. 3, A-C Neotrombidium barringunense Hirst, larva. A: ventral view, entire; B: tarsus and tibia of palp, ventral; C: tips of cheliceral digits. elongated, ovoid, 40» long by 14 wide, cheliceral digit curved, with a minute external tooth. Galeal seta short, curved, pointed, ciliated, 14» long. No hypo- stomal lip present. Setae on basis capituli long, tapering, ciliated, pointed, 404 long. Palpi as figured. Palpal femur, genu, tibia, tarsus with 1,1,3,8 setae respectively. Claw of palpal tibia strongly bifurcate, as shown. 93 GEOGRAPHICAL DISTRIBUTION OF N. BARRINGUNENSE The follawing additional localities are recorded: —(Queensland: Dead Man's Gully, north of Cairns, 29 November 1943, 4 specimens under bark of Lucalyp- tus sp.; 31 December 1943, 1 specimen from similar habitat; 2 January 1944, 1 specimen {no further field notes). Irvinebank, 28 September 1944, | specimen from under hark Eucalyptus sp. South Australia: Adelaide region (see next section). {All specimens collected by writer.) BIOLOGY IN THE ADELAIDE REGION Around Adelaide, Sotith Australia (Glen Osmond and Heywood Park), adults or nymphs have been taken by the writer from May onwards to February, over 1938-1941 and 1948-1951. An occasional specimen has heen found in soil, or under the bark of Encalyptus camaldylensis, but practically all the specimens from the Adelaide region have been taken under the bark of the trunks of Excalyptus leucoxylon, in the splits between fresh layers of damp bark, and I have no doubt that in the Adelaide region at least there is a very strong associa- tion between this mite and Eucalyptus leucoxylon, By August or September the adult females ate seen to he, in mounted specimens, gravid with eggs which show a good deal of development, About 30-50. (average 40) eggs can be counted filling (he body in these mounts, Oviposition has occurred on six occasions with captive females, Only one oviposition has been observed with each female, up to 40 or perhaps more eggs being iaid. After oviposition mounted femules contain no eggs, On three cecasions I have succeeded in rearing larvae from eggs laid in captivity. Details of Successful Rearings {1} Experiment ACB 398, Two adults were taken from under bark of Eucalyptus lencoxylon at Heywood Park, South Australia 26 September 1948, and these were placed in a glass tube with some bark from the tree. On 14 No- vember 1948 the mites were healthy and no eggs were present in the tube. On 7 Decetnber the tube was re-examined. One adult mite was rather shrunken. Nine active larvae were running around the tube. No attempt at feeding these was made, and by 28 December all the larvae were dead. The adult was shrunken, hut otherwise appeared healthy, It appears from this experiment that the period from oviposition ta hatching of the larvae is less than 23 days. The eggs were fiot seen, except as egg skins present along with the larvae. (2) Experiment ACB 399, Two specimens of N. barringwrense, one adult, one nymphal, were captured in the same situation us ACB 398 on 26 September 1948, and confined in a damp atmosphere in a glass tube. Water was added periodically as droplets to maintain humidity. Eggs, of the same colour as the adult, were laid between 10-17 October 1948, a total of 19 being laid. On 17 Gcto- tober the eggs were recorded as “almost smonth," having heen laid in a little pit formed between the cork and the glass wall of the tube, ur else scatlered around over the surface of the cork or the glass. By J9 October the eggs were irregular, with the typical deutovum outline. The eggs hatched out initially on 12 November 1948, and continued to hatch ot:t on subsequent days. Hence the period between oviposition and hatching ranged from 29-5 + 3-5 days upwards. (3) Experiment ACB 400. Eight specimens of N. barringunense were cap- tured in the same situation as the preceding on 26 September 1948. These were Placed in a damp tube with some bark from the tree. The tube was kept humid hy the periodical addition of droplets of water, Some of the specimens were o damaged in capture, and by 14 Noverher it was recorded that five adults were alive but some were a little shrunken and that ten living healthy larvae were running around in the tube. The tube was then allowed to dry aut, but one adult survived until 2 February 1949 when it was extremely shrunken, ity ghdomen scaphoid across the dorsum. Hence the period from oviposition to hatching wag tess than 43 days, From these and other experiments one may conclude that in the Adelaide region eggs are laid in November or early December, and that three to four weeks is passed in the egg stage. Some of the larvae were placed on human skin to see if any attempt at parasitization would be made, but none was observed, I recorded with one batch of larvae that they appeared to be positively, though weakly, phototropic. Adults of this species can withstand extreme desiccation for weeks, and it is sometimes a cause for wonder how they can survive when so extremely shrunken. Usually Trombidiids (s1.) do not withstand desiccation well, The habitat of N. basringunense—under damp bark of Eucalyptus—is a yery unusual one, the majority of Trombidiids (sJ.} dwelling in damp soil, and presimably the power of this species to withstand dry conditions is necessary for survival with their choice of habitat. DISCUSSION ON THE AFFINITIES OF THE LARVA Wharton (1938) described as new Monunguis streblida, a remarkable larval Trombidiid mite parasitic on the batfies Plereliipsis araneae Coquillett and Trichobius dugesii Townsend (Diptera:Streblidae) from the Cinquo de Mayas Cave, Tekax, Yucatan, Mexico, This larval mite has a strong resemblance to the larva of Neotrombidium barringunense. Tt has one large claw to each tarsus, and the dorsal secutym is similar, except for a bizarre appearance or structure between the scutal genailla, sketched by Wharton, which has na comparable structure in N. barringunenss, and may be an artefact. In the two forms the dorsal scutum shows a strong resemblance in shape and chaetotaxy, Wharton states that the coxa J and coxa II of Monunguis ave separated, but unfortunately he does not figure this feature. In this latter feature Wharton compares Monunguis with the European larval mite Rohaxltia biungulem Oudemans 1911. Oudemans (1912) says of this latter species “coxae Il und II getrennt,” and comments on its “Hydrachnid,” especially Limnocharid, affinities. Vitzthum (1913) appears to have been responsible for considering Rohaultia biunguium as the larva of the previously described adult species Johnstonianu errans (Johnston 1852), although I can find no grounds stated by him anywhere for this correlation. It would appear from Willmann (1947) that the only grounds used by Vitxthum were that the adults and farvac were associated im the field. Similar considerations have led other students of the Acarina into error. Thus Womersley (1934) accepted the species now known as Sphaerotarsus womersteys Southcott 1946 as the nymph of Cagculisoma ripicola Womersley 1934 on what appeared to be a stroug association in the field. Oudemans (1912) classified the larvae now grouped under Trombicula and related genera under the genus Microtrombsdium, quite erroneously. Unfortunately Wharton does not, in his very brief description, comment or the presence or otherwise of the “urstigma.” but as he places the larval Monunguis in the Trombidiidae as against the Erythraeidae one may assume that it is present. The only serious point of difference in the descriptions of Monunguts and larval Neotrombidianm lies in the contiguity or otherwise of coxae I and H, in which possibly Wharton was mistaken. There are so many resemblances between these larvae that there appears little doubt that Monunguts and Neo- trombidium are congeneric, and as the latter genus has priority it must take 55 precedence over Monunguis. NeStrombidinm streblidwa {Wharton 1938) is undoubtedly specifically distinct from the only other known Jarval species of this genus, Neotrombidiwm barringunense Hirst 1928. These species differ in the stricture of the non-sensillary setae of the dorsal scutum, the number and arrange ment of the dorsal setae of the abdomen, and in various other characters. DISCUSSION ON THE BIOLOGY OF NEOTROMBIDIUM Previously the genus Neotrombidivm has been known as the adult forms from Australia and South America. The correlation recorded in this paper extends the known range to Central America. Wharton states that the farvae (NV. streblidum) “were found to be parasitic on the streblid flies which imfest the bats” in the Yucatan caves. The species ef hats concerned are not mentioned by Wharton, but from other articles in the accourit of the fatina of the Yucatan caves (Pearse 1938 a and b, Pearse and Kellogg 1938) it appears these flies were obtained from two specimens (male and female) of the fruit-eating bat Artbeus jamaicensis yucetamcys (Allen) on 29 July 1936, It is reasonable to assume that the larvae of the Australian A’, barringunense have the same type of host as does the American species, aud we may expect to find the larvae in Australia parasitic on the Streblid flies parasitic on Australian bats. The genus Artibexs is not represented in Australia (Troughton 1943), hence any further stiggestions as to what bais may be concerned must remain conjectural. In fact, only a few fruit hats have been recorded from South Aus- tralia, and these appear to have heeti stragglers (Wood Jones. 1925). Of the dipterous family Streblidae no species appears to have been described from Australia, and they certainly appear to be far from common. Tillyard (1926) states that one undescribed Streblid has “been taken by Dr. Illingworth in north Queensland.” A few other dipterous bat parasites (Nycteribiidae) appear to occur in Australia, and one species has been described (Tillyard 1926, Rainbow 1904, Speiser 1905), The larvae of the Trombiculidae and Leeuwenhoekiidae are parasitic on vertebrates, only a few exceptions to this rule having been recorded. On one occasion the writer captured a larva of Tragardhula pentagoxa Womersley 1952 running freely over the black fur on the thorax of a female Troides priemus (butterfly) in rain forest eight miles east of Wondecla, north Queensland, on 20 October 1943 (not August, as recorded by Womersley). Audy (reported in Womersley 1952 and tm fit.) has found the larval Trombicula rara Walch 1923 parasitic on the pill-millipede Sphaegropacus globus-magicus Jeekel 1951, as well as Trombicula frittst Wharton 1945 parasitic on the scorpion Heterometrus longi- manus in Malaya. André (1943) recorded Leenwenhoekia paradoxa André 1943 parasitic on the scorpion Ruthus gibbosus Brulé on the island of Gavdos (south oi Crete). These findings arc exceptional, hut demonstrate that such larvae may utilize an arthropod host. It is difficult to imagine how in the open forest situations in which Nea- irombidium borringunense is found in Australia the numbers of adults of this species are maintained if only the apparently rare Streblid flies may be used as hosts by the larvae. In the cases observed in captivity the adult female lays a number of eggs, either in a Ivose cluster, or scattered singly, the batches observed in the tubes numbering between 20-40 eggs, Only one oviposition has been observed in each female, Gravid females contain 30-50 eggs (average 40), which frequently show considerable differentiation of the contained embryo, although the egg is inittally smooth on being laid, After oviposition the females are devoid of eggs in mounted specimens, which is confirmatory of the suggestion that there 96 is only one ayiposition. Oviposition ig not immediately lethal to the female; in Neotrombidium barringunmense 1 have observed the female ta survive 7 - 30 days after oviposition, which usually leaves it very shrunken, (With other Trombidiid mites I have.on occasions. obseryed the female to survive months after oviposition, under suitable conditions, which aré easier to maintain than those required for Neotrombidium). The slight disparity between the numbers of eggs observed after oviposition and the number within the ovaries of the gravid female may be due to experimental errors—e.g., the mites tend to lay their eggs in any minute crack in the bark provided, or in the corks sealing the tubes, etc. Presumably the larva of Neotrombidium barringunense hatches out under the bark of Eucalyptus leucovylon or some similar habitat, runs up the tree to find a suitable host, either free in the tree or parasitic on a bat, and after feeding pupates, presumably after falling to the forest floor, and finally reaches its Eucalypt habitat asa nymph, and remains there to complete the remainder of its life cycle, It is worthy of investigation whether the flies of the related Dipterotis family Hippoboscidae, which occur on birds in small numbers, might serve as 2 host for the larval mites. Although such 2 life history as outlined may appear fantastic, it is not more so than for example Fabre has recorded in his classic researches on the life of the anthrax fly. REFERENCES Anprt, M. 1943 Une Espéce Nouvelle de Lecuwenhoekia (Acarien), Parasite de Scorpions. Bull. Mus. Hist. Nat. (Paris), 2e Série, 15, (5), 294 Beeresz, A. 1888. Bull. Soc. Ent. Ital., 20, 179 Bertese, A 1912 Redia, 8, 50 Hirst, §. 1928 On some new Australian Mites of the Families Trombidiidae and Erythraeidae. Ann, Mag. Nat. Hist., Ser. 10, 1, 563 IDest, S. 1929 Additional Notes on Australian Mites of the Family Trom- bidiidae, with Descriptions of New Forms, Proc, Zool, Soc., London, 2, 165 Jones, F. Woon 1925 Mammals of South Australia, Pt. 111. The Monodelphia, Adelaide Leonarpr, G. 1901 Zool. Anz., 25, 17 Ovpemans, A.C. 1912 Die bis jetzt bekannten Larven von Thrombidiidae und Erythraeidae. Zool. Jahrb., Suppl. 14, 1-230 Pearss, A. S. 19383 Fauna of the Caves of Yucatan, Carnegie Inst., Wash., Publn. 491 Pearse, A, S. 1938b Insects from Yucatan Caves, Article XVIII, page 237, in Fauna of the Caves of Yucatan. Edited by A, S. Pearse (see Pearse 19382} Pearse, A. S., and Kentoce, R. 1938 Mammalia from Yucatan Caves, Article XXIV, page 301, in Fauna of the Caves of Yucatan, Edited by A, Ss. Pearse (see Pearse 19382) Rainnow, W. J. 1904 A New “Bat Tick.” Rec. Aust. Mus., 5, (2), 78 Sourxeorr, R- V. 1946 Studies on Trombidiidae (Acarina). Some Observa- tions on the Biology of the Microtrombidiinae. Proc, Linn. Soc, N.S.W., 70, (5-6), 312 Seemser, P. 1905 Literatur-Referate. Z. f. Wiss, Ins.-biol., I, 349 Trtyarn, R. J. 1926 The Insects of Australia and New Zealand, Sydney, page 378 TsovgHton, E, 1943 Furred Animals of Australia, Sydney Wauarton, G, W. 1938 Acarina of Yucatan Caves, Article X in Fatina of the Caves of Yucatan, Edited by A. S. Pearse (see Pearse 19384), p. 137 97 Wittmann, C. 1947 Trombidiidae. Lfg. 71 b. Das Tierreich, Berlin WomersLey, H: 1934 A Revision of the Trombid (sic) and Erythraeid Mites of Australia with Descriptions of New Genera and Species. Rec. S. Aust. Mus., 5, (2), 179 Wowmerstey, H. 1936 Additions to the Trombidiid and Erythraeid Acaritie Fauna of Australia and New Zealand. J. Linn. Soc. London (Zool.), 40, (269), 107 Womerstey, H. 1939 Further Notes on the Australian Trombidiidae with Description of New Species. Trans. Roy. Soc. S. Aust., 63, (2), 149 Womersitey, H. 1945 Acarina of Australia and New Guinea. The Family Lecuwenhoekiidae. Trans. Roy. Soc. S. Aust., 69, (1), 96 Womersiey, H.. 1952 The Scrub-Typhus and Scrub-Itch Mites (Trombicul- idae, Acarina) of the Asiatic-Pacific Region. Rec. S. Aust. Mus., 10, pts. i and ii, 1-673 DESCRIPTION OF A NEW GENUS AND SPECIES OF LARVAL TROMBICULID MITE FROM NEW GUINEA BY R. V. SOUTHCOTT Summary A new genus and species of Trombiculid mite, Babiangia bulbifera n. gen., n. sp., is described from New Guinea. One specimen was captured free on the forest floor, but 11 specimens were taken froma single small skink, Lygosoma (Homolepida) forbessii? The engorged specimens parasitic on the lizard were parasitic beneath the body scales, an unusual form of parasitization for a Trombiculid mite on a lizard. The engorged larvae showed a general convergence in body shape towards that of the Pterygosomid mites, which are obligatory parasites of lizards. The morphological affinities and biology of Babiangia bulbifera are discussed. 98 DESCRIPTION OF A NEW GENUS AND SPECIES OF LARVAL TROMBICULID MITE FROM NEW GUINEA By R. V. Soorrcorr [Read 9 July 1953] SUMMARY A new genus and species of Trombiculid mite, Babiangia bulbtfera un. gen, nm sp. is described from New Guinea. One specimen was captured free on the forest floor, but I1 specimens were taken from a2 single small skink, Lygosoma (Homolepida) forkesuf The engorged specimens parasitic on the lizard were parasitic beneath the body scales, an unusual form of parasitization for a Trombiculid mite on a lizard. The engorged larvae showed a general convergence in body shape towards that of the Pterygosomid mites, which are obligatory peraiies of lizards. The morphological affinities and biology of Babsangta bulbifera are discussed. In this paper a new genus and species of larval Trombiculid mite from New Guinea is described, Babiangia n. gen. Definition—Dorsal scutum quadrangular, broader than long with two sen- sillary setae placed anteriorly; with five non-sensillary setae, an anterior median seta, two anterolateral and two posterolateral setae. Dorsal scutum extends posteriorly beyond the posterolateral setae. Palpal claw bifurcate. Cheliceral fang (digit) simple, without accessory teeth, Galeal seta simple. Eyes two on cach side, the posterior eye the larger. Posterior ventral setae of abdomen with expanded bulbous bases, All legs with seven segments (including coxa, basi- and telo-femur. Empodium of tarsi thickened, equal to the tarsal claws. No whip-like setae on legs. When engorged the larva is of Pterygosomid facies. Babiangia bulbifera n. sp. Fig. 1-3 Description of Larva—Colour light pink. Length (including mouthparts) of unengorged type specimen 255,, width 175» (engorged specimens measure 300), Jong by 350% wide). Shape roughly globular when unengorged. Engorged speci- mens are flattened dorsoventrally, and then of Pterygosomid facies, with a distinct posterior notch (fig. 3 shows a specimen in which the posterior notch is not a marked feature). Dorsal scutum quadrangular, wider than long, 72« long by 97 wide, widest anteriorly, with sides almost straight. Anterior edge slightly concave, anterolatera! corners flattened, lateral sides straight except for a slight conyexity in the region of the posterolateral non-sensillary seta. Shield with two sensillary setae, ciliated in their distal halves, 69 long, arising toward the antero- lateral corners of the shield. Inter-sensillary distance 72». Scutal non-sensillary setae slender, pointed, faintly ciliated distally, the anterolateral arising as shown at the junction of the short anterolateral border with the lateral border of the shield, 37 long. Anterior median seta similar, 54» long, arising a short distance (9x) behind the middle of the anterior border. Posterolateral non-sensillary setae similar but very slightly swollen at proximal end, 2% long, arising a little behind the middle of the lateral border of the shield, close to the edge, which is there a little convex. The shield shows the normal slight porosity. 99 Standard seutal data for the type specimen are {in micra) : AW PW SB ASB PSB SD A-P AM AL PL Sens. 95 72 72 18 60 78 34 54 37 29 69 Eyes two on each side, mounted on a distinct shield. In unengorged specimens the eye-shield is close to the lateral border of the scutum. The posterior eye is considerably larger than the anterior. a Aik we"\ N=. \ vi \ ’, a | f " \ Be oh SOUTHCOTT Fig. 1 Babiangia bulltfera n.gen., n. Sp. Dorsal view, entire, unengorged, Dorsum of abdomen with 20 setae, long, pointed, slightly thickened in their proximal halves, ciliated, 33 - 63» long, arranged as figured. Ventral abdominal surface: a pair of pointed ciliated setae, 26m long, between the fused coxae 1 and IJ; a similar pair 21h long between coxae III. Behind coxae IIT and anterior to the anus is a group of pointed ciliated setae with bulbous bases, 25-27 long. Lateral to the anus are four long strong ciliated setae, thickened proximally, medial pair 47 long, lateral pair 60 long. Legs of normal length, leg I 295 long, IT 245, III 295p (all lengths includ- ing coxae and claws). Coxae normal, as figured. Each coxa with a single long curved pointed ciliated seta; that on I arises towards the posterolateral angle, is 46p long; on LI arises close to the posterolateral angle, 35, long; on IH arises 160 near the anterolateral angle, 63» long. Chaetotaxy of legs as figured. Setaé of legs mostly strong and heavily ciliated, No long whip-like setae on legs. Metatarsus I 48u long, On metatarsus III, neat its distal end, is a long strong tapering pointed ciliated seta, 53 long, with a bulbous proximal part. Tarsus I and I] with the normal solenoidal spine, not present on IJI. On tarsus III the claws are reinforced by a strong curved ciliated seta arising distally on its posterior aspect. On all tarsi the empodium is thickened and is as strong as the claws, Tarsus I 76p long by 24y high,. SOUTHCOTT 200; ff Fig. 2 Babiangia bulbifera n, gen, n.sp. Ventral view, entire, unengorged. Chelicerae and palpi stout and compact, Cheliceral digit strong, curved, simple, without apical cap. Galeal seta short simple curved pointed, 15y long, Seta on basis capituli long, strongly and unilaterally ciliated, 40 long. Palpi as figured. Palpal femur, genu, tibia, tarsus, with 1,1,3,8 setae respectively. Femoral seta ciliated, genual seta simple, tibial setae simple. Claw of palpal tibia bifurcate, the axial prong being internal. Locality—Babiang, Aitape region of New Guinea. (1) a single specimen, Type, free, unengorged, from the rain forest floor, 22 December 1944 (R.V.S.) (ACB 582). (2) 11 specimens parasitic under the body scales of a lizard (Lygo- 101 soma (Homolepida) forbesii?) (identified by J. R. Kinghorn, Australian Museum), same situation, 24 December 1944 (R.V.S.) (ACB 258 A-K). (All specimens in author’s collection.) Fig. 3 Babiangia bulbifera, n. gen., n.sp. Dorsal view of an engorged specimen, DISCUSSION ON GENERIC CLASSIFICATION In keys offered in standard classifications of the family Trombiculidae, ¢.g., those of Wharton e¢ al, (1951) and Womersley (1952) this form would be classified as Trombicula. Structurally Babiangia differs from Trombicula in the shape and chaetotaxy of the dorsal scutum, and in having the posterior eye larger than the anterior, Babiangia has a resemblance to the genus Novotrombicula Womersley and Kohls 1947, having the dorsal scutum similarly produced posteriorly, but in the latter genus the shield so extended takes in two of the dorsal abdominal setae. Babiangia differs also in having the empodium thickened and similar to the claws; in Novotrombicula and normally in Trombicula the empodium is long and slender. DISCUSSION ON BIOLOGY The specimens of Babiangia bulbifera taken parasitic on the lizard appeared to show a good deal of adaptation to their host, The specimens were completely hidden under the scales, and were only found because it was noticed that some of the scales of the trunk and tail showed a little tenting, and that there was a slight gap under their free edge. The flattening of the body of the mite, and 102 general resemblance to the shape of the Pterygosomid mites, in the engorged specimens is remarkable, showing a strong convergence. Parasitization of lizards and other reptiles by Trombiculid mites is well known, but mostly the reptile is merely one of a number of possible hosts, no particular adaptation being shown, and the Trombiculids are not found under scales but clustered as is normal in mammals and birds on some suitable soft patch of skin, e.g., in the axillae, groins and external auditory meati, with the bodies of the mites projecting free above the surface (Michener 19464 and b, Southcott 1947, Hyland 1951), REFERENCES Hyianp, K, E. 1951 Observations on the Chigger Mite Trombicula (Eutrom- bicula) splendens Ewing (Acarina:Trombiculidae). Ann. Ent. Soc. America, 44, (3), 297 MicHeEner, C. D. 19462 Observations on the Habits and Life History of a Chigger Mite, Eutrombicula batatas (Acarina:Trombiculinae), ibid., 39, (1), 101 MicHener, C. D. 1946b Taxonomic and Bionomic Notes on Some Panamanian Chiggers (Acarina, Trombiculinae), ibid., 44, 411 SoutHcotr, R. V. 1947 Observations on the Epidemiology of Tsutsugamushi Disease in North Queensland, Med. J. Aust., 2, 441 Wuanzton, G, W., Jenkins, D. W., BRENNAN, J. M., Fuuver, H. S., Kouts, G. M., and Pup, C. B. 1951 The Terminology and Classification of Trombiculid Mites (Acarina:Trombiculidae). J. Parasit., 37, (1), 13 Womerstry, H. 1952 The Scrub-Typhus and Scrub-Itch Mites (Trombiculi- dae, Acarina) of the Asiatic-Pacific Region. Rec. S. Aust. Mus., 10, Pts. 1 and 2, 1-673 Womerstey, H., and Kouts, G. M. 1947 New Genera and Species of Trom- biculidae from the Pacific Islands. Trans, Roy. Soc. S. Aust., 71, (1), 3 STRATIGRAPHY AND STRUCTURE OF THE NORTHERN TERRITORY OF AUSTRALIA BY PAUL S. HOSSFELD Summary The Northern Territory of Australia covers an area exceeding 520,000 square miles. Very large areas have not been examined geologically. The existence of formations of most of the major geological divisions has been recognised. Those not recorded, or doubtfully so, are formations of the Silurian, Triassic and marine phases of the Tertiary Period. 103 STRATIGRAPHY AND STRUCTURE OF THE NORTHERN TERRITORY OF AUSTRALIA By Paut 5. Hossretp * [Read 10 September 1953] CONTENTS Page Sum MARY - - - - - 3 - “ TL. Inprropucrion - - - - - “ - = - 104 II. Georocy - - - - - - - = « - 104 A. GENERAL - - - = - “i = ~ - 105 B. ArcHAgOzOIC - - - - - - - - - 105 The Musgrave Block - - - * e £ -~ 106 The Arunta Block - - - - - - - ~ 107 C. Prorerozoic - - - - . - : " - 110 Lower Proterozoic - - - - - = é - 112 Middle Proterozoic - - - - m > 7 - 115 (a) The Hatches Creek Group - = . - - - 115 (b) The Carpentaria Group - - - - - - We The Newer Granites and Metallogenesis - - - - - 120 Upper Proterozoic - “ ~ “ 7 - 3 - 124 Ages and Correlation of the Lower to Middle Precambrian Rocks ~ 126 Correlation with Queensland and Western Australia - - - 127 Structures and Trend Lines of the Precambrian Rocks - - 128 D. Late Prorerozoic AND CAMDRIAN - - - - * - 131 The Buldivan Series ~ - - - - 4 - - 431 (a) The Buldiva Quartzite - - : 2 E ~ 433 (b) The Daly River Group or Upper Buldivan Series - - 134 (c) Volcanics - - - - - ~ - - 136 The Amadeus Geosyncline - - - - - - - 137 Age and Correlation - - - - = - - - 140 E. Orvovictan - - - - a - = - - 142 F, Sicuaian ~ - - - - - - - - 144 G. Devonran - - - - ~ = is ri ~ 145 The Collia Series - - - - - - - - 145 H. Carsonrrerous - - - & « « = - 146 I. Permian - - - - - - - - - 147 The Port Keats District - - e - “ + - 147 The Burt Range Basin - . - = = - 147 Other Areas in North Australia - - - - ~ - 147 The Finke Series - - - - 4 = - 148 The Elliott Creek Formation - - - = = - 148 J. Trtassic ~ = - “ - = = 4 - 149 K. Jurassic - - - - - - - - - 149 L. Creracrous - - - - re = = s ~ 149 The Great Australian Artesian Basin - - - - - 152 The Burt Trough = - - - - - - - - 152 M, Carnozorc - - - - - - we « - 155 TI. ReFerences AND Braviocrarny - - - - - - - 156 IV. IeLustrations - rs = SUMMARY The Notthern Territory of Australia covers an area exceeding 520,000 square aniles. Very large areas have not been examined geologically. The existence of formations of most of the major geological divisions has been recognised. Those not recorded, or eoubthiily so, are formations of the Silurian, Triassic and marine phases of the Tertiary eriod. The rocks, structures and succession of events are discussed from the oldest, the Archaeozoic, ta the close of the Mesozoic Era. The incompleteness of geological mapping and great extent of recent surface accumulations, have necessitated the use of inferred occurrences and boundaries to a large extent in the compilation of the * School of Geology, University of Adelaide. ‘Trans. Roy Soc. S. Aust., 77, July, 1954 04 geological map and discussion of the history of the region. The use of all published works, together with the extensive observations made by the author, have made it possible to arrive at a number of conclusions, even though some be tentative, regarding the structure and geological evolution of the Northern Territory, Where practicable, correlations have been attempted with formations in Oteens- land, Western and South Australia. I. INTRODUCTION The Northern Territory of Australia has an area in excess of 520,000 square miles and occupies therefore more than one-sixth of the total area of the continent. Reference will be made to its two divisions, Central and North Australia, which had short-lived separate administrations from 1927-31 (Sec General Map). ; It is a frontier province to this day. Except for mining camps, mission centres and pastoral holdings, the few settlements are confined to the Over- land Telegraph Line and to the two unconnected lines of railway. There are ¢normous areas tin which roads and eyen tracks do not exist, and water supply is temporary and precarious. Wide expanses of sand-plain, the large areas of closely spaced sand dunes as well as the rugged topography af many sectors make access difficult and hazardous. It is not surprising there- fore that much of the Territory is not mapped and considerable areas have nat been explored. Geological examinations have been made of numerous areas, but the greater portion of the region has Leen traversed by very widely spaced reconnaissance suryeys and many areas have not been examined at all by gtologists. From 1935-41, the Aerial, Geological and Geophysical Survey of North- ern Australia (A.G.G.S.N.A.). sponsored jointly hy the Governments of the Commonwealth, Queensland and Western Australia, conducted investigations in the above two States and the Territory. The writer was the Senior Geolo- gist in charge of the Northern Territory Geological Party of that Survey, which will be referred to generally in the text by its abbreviated title of Northern Australia Survey or as N.A.S., but bibliographic references will be given as A-G.G.5.N.A, During the course of this survey, the writer con- ducted extensive ground and air reconnaissance surveys over large parts of the Territory, and selected areas for aerial photography. Of the numerous Jarge areas selected and photographed, many were examined and mapped subsequently with the aid of the aerial photographs. A number of reports were written by the present writer and his assistant geologists; the majority have been printed and are listed in the attached Bibliography. The titles of others, not printed, will be found in the A.G,G,S.N.A. reports. Where ‘possible the rocks and minerals characteristic of each area examined were collected int triplicate; the chief collection was forwarded to the Bureau of Mineral Resources at Canberra, the others were sent to the Mines Branch at Alice Springs and to the Department of Geolugy at the University of Adelaide. The termination of field activities by the N.A.S. in 1941 ended systematic geological examimation in the Territory during the remaining war years Since then geological work has been carried out chiefly by officers: of the Commonwealth Bureau of Mineral Resources, Canberra, and the contribution of aerial photography of large sectors of the Territory is rapidly advancing our knowledge of largely unknown areas. The writer gratefully acknowledges the assistance by the Council of the University of Adelaide in making research grants during 1949 and 1950, and to the Professor of Geology, Sir Dauglas Mawsou, for the use of facilities in the investigation and compilation of the material presented herein. 105 Through the courtesy and co-operation of the Commonwealth Survey Tiirectorate. the writer was able to examine Jarge numbers of aerial photo- graphs of areas not covered by the N.A,S. photography. Reference must be made also to the great value of the pioneering work of early explorers and geologists, especially H. Y. L. Brown, Davidson, Maurice, Streich, Tate, Tictkens and Winnecke, and to numerous more recent contributors. . The writer desires to place on record his appreciation of the work done in the Territory by the Assistant Geologists of the N.A.S., notably that of A. H, Voisey, A. W. Kleeman, C. J. Sullivan, V. M, Cottle and T. V. Lewis. Il. GEOLOGY A. GENERAL The geological record includes formations of nearly all the maio: divisions, the Silurian and Triassic being the only ones whose presence has not been proved. (See General Map.) Some formations have received no definite age determinations as yet, but a tentative classification has been made where this appeared reasonable. Such formations include the Collia Series and Elliott Creek Formation of North Australia, the Post-Ordovician Can- glomerate and the Finke Series of Central Australia, Despite the large amount of detailed mapping that has been carried out in the last thirty years, little except highly generalized information is avyail- able of the greater part of the Territory. Large areas are unexploréd geologically and many of those traversed at very wide intetvals by carly explorers have not been visited since, Enormous areas are deyoid of solid outcrops and the subjacent rocks have been classifed on indirect evidence stich as vegetation and soils. topography, scattered wells and bores and isolated outcrops. The absence of solid outcrops over large areas is the result of various factors such as: 1. Extensive duricrust with or without sand-cover. 2. Large areas of parallel sand-dunes. 3. Large planed areas produced, some by marine, some by aeolian action, 4, Large areas of alluvium and lacustrine deposits. 5. Horizontal or sub-horizontal sediments, many in areas of graded internal drainage. A very large proportion of the otiteropping rocks are Precambrian in age and their correlation depends on structural and lithological features, lt is possible therefore, except in limited sectors, to deal only with the broader features of geological structure and succession, All available publi- cations and observations were examined and considered, but specific refer- ence in the text to cach one was impracticable. The interpretation, and tn a number of instances, modification of widely divergent views were facilitated by the writer’s extensive knowledge of the Territory obtained during the N.A. Survey and on other occasions. As a result, the writer found it possible to extend considerably, boundaries of formations from areas examined on the ground te others examined from the air or on aerial photographs. B. ARCHAEOZOIC The oldest formations known in the Territory occur within the areas accupied by the Arunta Complex (Mawson and Madigan, 1930, p. 417). Descriptions of the rock types, their location and mineralization are to be found in many reports of the early explorers, but predominantly in those of H, Y. L. Brown, to whose pioneering investigations we vwe much of our 106 earlier knowledge of the geology. Of the more recent investigators, the more important contributions are those of Chewings, Hodge-Smith, Hossfeld, Mawson and Madigan, Voisey, Wilson, and Ward. The investigations of the N.A. Survey showed that determination of the stratigraphical sequence and chronological succession, while laborious and difficult, is possible; but as is to be expected, will require much detailed field and laboratory work, The formations of the Arunta Complex outcrop in two distinct areas separated by a great thickness of younger sediments. The two areas are known as the Musgrave and Arunta Blocks (Pitjentara and Arunta Shields, respectively, of Chewings, 1935). The intervening area occupied by younger sediments was named the Amadeus Geosyneline. (Amadeus Sunkiand of Chewings, 1935.) Although formations of the Artinta Complex outcrop over Jarge continu- ous areas in some sectors such as for example in the Harts Ranges, the Arltunga District and other areas east, north-east and west of Alice Springs, there exist on these blocks numerous outcrops of younger sediments of several periods. Many of these indicate by their attitudes and location that they represent the eroded remnants of deposits which formerly covered large portions of the old blocks. Over very large areas also, no solid outcrops exist and the surface consists of recent aeolian deposits as a veneer over the older rocks. In many instances information obtained from bores and wells has proved the existence at shallow depths of Archaeozoic rocks. There are a number of areas, however, in which the presence of the basement rocks at shallow depths is inferred. For the purpose of the general map deposits of alluvial or aeolian origin where they serve merely to obscure the ancient rocks, have been ignored. Some areas such as the Burt, Hale, and Plenty Plains, are down- faulted blocks on which sediments ranging from Mesozoic (?) upwards, have been deposited. It is possible teat other downfaulted basins exist within the Arunta and Musgrave Blocks, THE Muscrave Bleck This black occupies the extreme south-western part of the Territory. It extends westwards into Western Australia to the Warburton Ranges, and southwards into South Australia where it forms a large area in the north-western corner of that State and outcrops as a number of Inselberge such as the Musgrave, Everard, Mann, Tomkinson and other Ranges. The greater part of the Musgrave Block in the Northern Territory, Western and South Australia, is included in a native reservation in which non-aboriginal settlement is prohibited and access illegal, except by an official permit. Ft can be understood, therefore, that tracks and water supplies are scarce and access in general is possible only for well-equipped and organized parties. The importance of the search for radio-active minerals is expected to stimulate exploration of these areas of ancient rocks. A considerable amount of information its available of the Western Australian sector (Streich, Talbot, Clarke, et. a!.), and of the South Austra- lian portion (Streich, Brown, Basedow. Jack and Wilson). The Territory sector has been explored geographicalty but ihe rocks and structures of the Archaeoseic formations are not well known. More attention has been given in the past to the more prominent topographical features most of which are residuats of rocks considered to be of Proterozoic age. Such information as ts available both from the literature and the writer's limited observations, indicates that the Territory sector contains a continuation of the rock types 107 and structures noted in the South Australian portion, The extensive develop- jient of metamorphosed basic igneous rocks—greenstones—recorded in the western part of the Western Australian sector of the Musgrave Block (Tal- bot and Clarke, 1917), is not repeated either in South Australia or the Northerm Territory. Similar altered basic rocks (dolerites and gabbros chiefly) do occur but are of less importance. The adjacent parts of Western Australia (Talbot and Clarke, 1917) and of South Australia (Wilson, 1947) contain large areas of acid rocks, many of which appear to be of rgneous origin. The oldest rocks recognised in these areas and of the Northern Territory sector of the Musgrave Block are in- tensely altered sediments now consisting chiefly of gneisses in which garnet, cordierite, spinel, biotite and sillimanite are developed. Some outcrops of schists, conglomerates and guartzites, mylonitized in part, are recorded, but are scarce. It is probable that the vast aeclian deposits which obscure the outcrops over so much of the area, cover to a large extent the more easily eroded rocks. The known tock types as recorded, probably do not give a true picture of the types and relative amounts of the Archaeozoic rocks of the region. In the ancient metasediments there are numerous, predominantly con~ cordant, masses of granite gneisses; many of them of great size. The recognition, both in Western and South Australia, that these acid “ortho- gneisses” include many hypersthene-bearing rocks similar to the Charnockite Series of India, suggests that such may exist also in the Northern Territory, both in the Musgrave and Arunta Blocks, Subsequently to the intrusion of these acid rocks or their formation by granitization, there appears to have occurred a period of igneous activity marked by intermediate to basic in- trusions, (Wilson, 1947), As these are non-gneissic except in localities of marked dynamic metamorphism, they appear to be separated by a consid- erable time interval from the gneissic rocks, and are correlated tentatively herein with the basic intrusives of later Precambrian age—Lower to Middle Praterozoic—of Central and North Australia. Subsequently, acid intrusions took place on a grand scale, producing very large bathyliths of granitic rocks of which the Everard Ranges Granite may be regarded as typical. These granites are predominantly non-gneissic, but exhibit gneissic structure in parts near their margins. These “Newer Granites,” too, include Charnockitic types. (Wilson, 1947), The gneissic structure exhibited by these granites near their margins in some localities and the apparent transition from granite to invaded rock noted in some out- crops, suggests that some granitizaltion accompanied or was produced by the intrusion of the acid magma. Finally, there appears ta have come the introduction of basic rocks, dolerites, gabbros, norites, etc., which exhihit little alteration and which have been assigned to various ages by different observers. To the Archaeozoic Era are referred those igneous rocks which exhibit predominantly concordant gneissic structure on a regional scale and those metasediments and igneous rocks into which they are intrusive. Subsequent sediments and igneous intrusions, though they may have been subjected to severe deformation, do not show the degree of stress and metamorphism so characteristic of the older rocks, and are referred to the Proterozoic Era. Tur AsuntTa Biockn This block extends from the vicinity of Alice Springs (lat. 23° 45’ 5. approximately), northwards to a short distance beyond Barrow Creek (lat. 21° 15’ S. approximately). Its greatest east-west extent is approxmmately 108 450 tiles, and it approaches both the Queensland and Western Australian borders, Further explorations may extend the known outcrops to the east and west, hut are not expected to result in material changes of the outline as presented herein. As in the Musgrave Block, the Precambrian formations of the Arunta Block consist predominantly of rocks assigned to the Archaeszoic Era, but include also a considerable proportion of younger rocks of sedimentary and igneous origin, An enormous time-interval appears to separate the two age- divisions, and the younger is therefore assigned to the Proterozotc Era. The oldest known rocks of the Arunta Complex consist of intensely metamorphosed sediments and igneous rocks. No evidence is available of the basement on which they rest or of the terrain from which the sediments were derived. These very ancient rocks have been affected by regional, dynamic, thermal and contact metamorphism, injection of igneaus materials. metasomatism and granitization, with regional metamorphism the dominant feature. Some formations have experienced more than one type of meta- morphism and in numerous instances variations in type or intensity can lie observed in a formation or in a bed along its strike. In many instances it is impossible either to determine the nature of the material from which the present rock is derived or even to decide whether its origin was sedimentary or igneous, Detailed observations show, however, that included in the criginal rocks were conglomerates, arkoses, grits, sand- stones, mudstones, limestones and volcanics (tuffs and flows), as well as transgressive igneous rocks such as aplites, pegmatites, basic dykes and probably sills. The rocks consist of gneisses and schists in great vanety and include large formations of augen-gneisses and schists. Gneisses range from acid to basic in composition, including a lustre-motiled hornblende-gneiss, and represent both ortho- and para-gneisses. Schists have been produced by the metamorphism and recrystailization of all types of sediments and vol- canics and have developed a great variety of minerals, including sillimanite. cyanite, micas, chlorite, talc, garnets, sphene, spinel, hornblende, diopside, scapolite, epidote and many others. ( Garnets occur in gneisses and schists over very large areas and in immense numbers, Most of them are small, but their numbers so great that for miles the sand and soil are red. and consist predominantly of that mineral. However, crystals over an inch in diameter are plentiful. The largest seen by the writer had a diameter exceeding 3 inches. Hadge-Smith (1932) records one of nearly 11 inches diameter. The garnetiferous rocks and some gurnet reck occur in many parts of the Arunta Block but mainly in the area to the cast and north of the River Hale, where gem quality stones occur in large numbers. Mylonitization was intense in some areas. Conglomerates were trans- formed ta gneisses and in some instances the original pebbles stretched to thin. Alms. Calc- and quartz-schists, sheared basic rocks and other recards of dynamic metamorphism occur plentifully, but tn restricted areas. Injection of igneous materials, both acid and basic and the granitization and contact metamorphism of these ancient rocks add to the immense variety of rock types, developed as stated earlier, in some instances at intervals along the strike of a bed or a formation. In addition, subsequent silicification, either selective or general, has increased the difficulties of determining the original material. The recognition of originally igneous material depended in many fn- stances on observations in the field rather than on microscopic determination. There were instances, however, where the latter confirmed the field evidence- 109 Acid igneous material invaded or was formed in the ancient sediments and igneous recks which form the basement rocks of the Arunta Complex, Geth in the Arunta and Musegraye Blocks, enormows areas shaw outcrops of granite gneisses and related rocks (Pl, IJ, 1). In most instances the gneissic structure 1s parallel to er concordant with thal of the invaded gneisses and schists. These “older granites” occur on a vast scale not only in the Northern ‘Territory, but also in South and Western Australia. They were invaded by basic rucks, priginally dolerites or gabbros and probably some ultra- hasic types. which rocks haye been metamorphosed and recrystallized to umphibalite gnetsses and schists. These anciet( acid and basic igneous rocks have been subjected gener- illy to the regional and specific types of metamorphism which were experj- enced by the invaded rocks, The concordance uf many of the granite gneisses and approach to concordance of others, suggesis that the original rocks had been subjected to diastrophism, some of a severe character and therefare, chat some metamorphic activivy, chichy of a regional type. had occurred before the formation of the granite-gneisses. It is probable that the acid igneous activity follawed closely upon and was partly synchron- ous with w period of seyere orogeny and that the final phases were marked by the introduction of basic igneous material. The severe folding and Taulting which are such marked features of the Archaeozoic formations of the Arunta Complex have affected the ancient formations, the “older granites” and “older basie intrusions” and it is impossible at this stage ta determine the amount of deformation prior to the period of igneous activily. Modge-Smith (1932, pp. 423-431) proposed a tentative age classification wf the formations of the Arunta Complex. The present writer agrees with the reference to the Froterozoic Era of the Everard Range Granite and the Molgarna Acid Intrusives. Hodge-Smith, however, went Further and sug gested a division of those rocks which are predominantly of sedimentary origin into the Huckitta and Ambalindum Series, the farmer being the older. In view of the marked lithological differences between his “Huckitta Series” and racks cuteropping in the Arltunga District, a division af these -\rehaenzoic rocks is tempting. It 1s difficult, however, to decide whether Hodge-Smith regarded the rocks of the Arltimga District as members of his “Ambalindum Series.” Voisey (1938) appears ta take this view but includes with them the White Range heds, which Hodge-Smith, following Chewings (1928), defimitely though mistakenly, correlates with the Perta- knusra or Upper Proterozoic beds. The present writer disagrees with both the above views, and considers the White Range Quartzite and associated beds as Post-Archaeozuic and pre-Pertaknurra, and probably of Middle Proterozoic age. It is possible that detailed structural mapping will «lemon- strate the existence in the Arltunga District of unconformuble groups of metasediments within the Archaeozoic rocks, but sit present this must be merely an interesting speculation and they will he referred te collectively us the Aruntan Series. Examination of the Harts Ranges shows that these ranges consist chiefly of a group of highly metamorphosed rocks apparently of sedimentary origin, which are folded against and dip away from the gneisses, schists and granite gneisses of the Aritunga Distecit, and appear ta be ancomformable to them. Some fault boundaries were observed, but the greater portion of the contacts appear to be unconformable. The northern continuations of these rocks are cut aff sharply by the fault boundaries wf the Plenty Trough which contains sediments probably of Mesozoiw and Cainozoic ages (Fig. 2). The Harts Range rocks consist of schists and gneisses intruded by very 110 rumerous, muscavite-hearing pegmatites of probably Middle Proterozoic age. The metamorphism of the original sediments was intense, but in those sectors examined by the writer, the range of original material appears 10 have been much less than that of the adjacent and presumably older racks of the Arunta Block, and they do not appear to comtain the granite gneisses so plentiful elsewhere. It is suggested that the Harts Range metamorphics may represent a younger division of the Archaeozaic Era. They are classifiee! tentatively as Upper Archavozoic and will be referred tu as the Riddock Series. The Archacozoic rocks ag defined in this paper are those referred to as the Lower Precambrian by David and Browne (1950). The metasediments of the Arunta Complex with their sheared ton glomerates, sheared and reerystallized busic tutis, flows and possibly sills, as well as the great thickness of other associated rocks. of clastic origin, are referred to the Warrawoona Series of Western Australia and the Argylla Series of Queensland, ‘There appears to be little doubt of the correlation of the granite-gneisses with those of other parts of Australia at or near the top of the older Arch- aeozoic. (Kalkadoon Series of North-Western Queensland.) The effect of Archacozoic igneous activity on the introduction of metallic minerals in the Musgrave or Arunta Blocks has not been determined, The intense metamorphism and deformation of the rocks as well as the wide spreaul mineralization during the Proterozoic Era, but especially the enor- mous depth of material removed by erosion, make such a determination dificult, There are a few octeurrences including gold, copper and tungsten which have no apparent connection wilh Proterozoic mineralization, and are regarded tentatively as of Archacozaie age. All these occurrences, however, are sinall and of little economic value. As 15 to be expected in a region of intense deformation, the Archacoavic rocks exhibit structures which may vary widely in direction within very short distances, Despite these expected irregularities, however, there 15 a remarkable tendency, as noted by previous observers, for westerly to north- westerly strikes ta persist or recur over long distances in the central portians of the Arunta Block. Towards the western extremity, however, as for example at Mount Doreen, the strikes change to a north-north-westerly trend (Hossfeld in A.G.G.S.N_A., 1940b), (Hills, 1946), In the eastern half of the block, westerly to north-westerly strikes persist, except for loc! variations, as far as the Jervois Ranges Mineral Field. The writer, while surveying this field (Hossfeld, 1931), noted a marked change of strike at the southern end of the field; the swing from east-west to north-north-west exceeds nitiety degrees, This northerly strike may represent merely a local departure from the general trend or it may coilinue, as suggested by Hills (1946), lo the Cloncurry Region in North-Western Queensland. The exten- sive jitervening cover by the Trldivan Series of Cambrian age. made +) determination impossible, Cc. PROTEROZOIC Trom Darwin in the north to the vienity of Alice Springs in the south, and froma the Western Australian to the Queensland border there outerop at intervals, groups of sediments which have been metamorphosed, inteudesd! by acid and basic igneous rocks, and in most areas contain metallic anineral deposits. Their metamorphism varies considerably in severity, but except in a few restricted localives, does not approach in intensity or completeness the metamorphism exhibited by the Archaeozoie formations, Farther, where- 111 as the Archaeozic rocks include acid and basie igneous rocks which are regionally gneissic, as well as predominantly non-gneissic intrusions, it is the latter only which invade the younger, and less metamorphosed rocks. With the exception of stich areas as the White Range, Jervois Ranges, McArthur River District, etc, to which some observers have assigned mare recent ages, these newer metamorphic rocks and their associated igneous intrusions. have been and are regarded generally as being comparable in age with the Mosquito Creek Series of Western Australia (David, 1932), (Hossfeld, 1936-40), ((Matheson and Teichert, 1945), (Noakes, 1949). This series is regarded by some as Upper Archaeoznic, hy others as lower Proterozoic. For reasons which will be given below, the latter is adopted by the present writer. The detailed mapping of the Brock’s Creek District carried aut by the N_A-S. during 1939 and preceded during 1935-38 by detailed surveys of many smaller areas in North Australia, indicates that all the mineral-bearing rocks of the Darwin-Katherine region and beyond (which includes the Brock’s Creek District), belong tao one confarmalile Series and represent continuous deposition to a thickness of at least 17,000 to 18,000 feet. These sediments exhibit marked variations in intensity wf metamorphism in different Jocalities but cannot be separated into age-groups on that score. The views expressed by some observers, and hased apparently on the variable degrees of metamorphism exhibited by the sediments, that unconformable age-groups exist in the mineral-bearing sediments of the Darwin-Katherine region, have not been confirmed. Further to the south-west, south and sotith-east, however, there is evidence of the existence of at Jeast two unconformable divisions af miner- alized sediments of Precambrian but Post-Archaeozoic age (Fig. 1). LOWER PROTEROZOIC MIDDLE PROTEROZOIC (ACICOND) SERIES) (BAVEN PORT SERIES) Lx =e ~ . 2 RN (A RP 1 QUARTZITES VDLCANICS AMPHIBOUITES ACID TuTES © SUATES € SANDSTONES ESHWALES INTRUSIVES Woe 2 %& ‘ the & WILE H~2 Piz. 1 Sketch Section at Hatcbes Creek. As far as is known, the only recorded straligraphical break in the con- tinuity of these formations is that revealed by the detailed mapping during the examination hy the N.A. Survey of the latches Creek area, in the eastern portion of the Davenport Ranges of Central Australia. Near the southern limits of the mapped area, schistose and sheared porphyries, tuffs, and related rocks with some slates, are overlain unconformably by the group of sediments of the Hatches Creek Wolfram Field, In the report, (A.G.G.S.N.A., 1941), the lower group was referred to by the present writer as the “Bottom Series.” It is not proposed here to give these rocks a formal name, as they are being correlated tentatively with similar rocks at Tennant Creek, The Granites, Tanami, ete., which are being correlated with the meta- forphosed sediments of the Darwin-Katherine Region. As the survey which 112 located these rocks in the Davenport Ratiges was primarily an economic one it was impossible tu carry the stratigraphical investigations further at that lime. The group which lies unconformahly alve the "Bottom Series” was Wamed the “Llatehes Creek Series.” Together with the former “Top Series” it will be referred to as the Hatches Creek Group which is being included in a division being named the Davenport Series. Still higher in the sequence, lying unconfarmably an ali of the Pre- cambrian formations so far discussed, there occurs at intervals oyer a large part of North Australia a formation of massive arenaceous sediments pre- dominantly quartzites, but including sandstones, grits and couglumerates. The age of this formation, which was named the Buldiva Quartzite, has heen given variously as Upper or Late Proterozoic or Lower Cambrian. Most observers, including the present writer, correlated it with similar furmations of the Nullagine of Western Australia. However, the writer cansidered it to he the basal formation of the Buldiva(n) Series (Hossleld 1937 ¢ et al), a series which it was stated continues without interruption into the Cambrian Period and includes the Cambrian sediments of the Daly River area, Barkly Tableland, etc, To this opinion the present writer adheres, but now regards the Buldiva Quartzite as considerably younger than the Nullagifie Series with which it was correlated previously (Fig. 3)- While it is possible that deposition of the basal members of the Buldiva Quartzite tay have begun at the close of the Proterozvic Era, the whole ef the remainder of the Buldivya(n) Series is of Cambrian age. That Series will be discussed therefore, in the section dealing with the Cambrian Period. In the Atnadeus Geosyncline, situated between the Arunta and Mus- grave Blocks, deposition appears to have begun in the Upper Proterozoic and to have continued throughout the Cambrian and Ordavician Periods and probably inte the Silurian, These divisions will be referred la in the sections dealing with the respective Periods. The area between Borroloola and Wollogorang af which little ts known, appears to be covered largely by quartzite outcrops which in the western sector exhibit enormous, long sub-parallel gashes resulting possibly from the erosion of dyke formations. On the evidence of limrted investigations along the margins and apparent relationships ta the Cambrian formations above, and to the Carpentaria Group of adjacent areas, these rocks are being regarded provisionally as of Upper I’roterozoic age. Lower Proterozoic The formations assigned to this age division were correlated with the Mos¢jtiita Creek Series of Western Australia (David, 1932), (TLossfeld, 1936h), (Voisey, 19392), (Noakes, 1949). As will be shawn later, it is suggested herein that the formations which have been mapped as Mosquito Creek Series in Western Australia, may belong to twe uncantormable Fre- cambrian divisions. It is probable that those formations of North Australia previously correlated with the Mosquito Creek Series, will be found to be the equivalent of the older formations of that Series in Western Australia. A definite correlation is impossible at present. They will be referred to here- under as the Agiconili Series, after the native tribal name of the district (Cummanwealth of Australia Bulletin No. 191, in which the Pine Creek and Union Groups outerop (Hossfeld. 1936 and c), The Agicondi Series outernjis over a large part af North Australia. It includes the greater partion uf the rocks outcropping in the triangle formed bby Darwin, Oenpelli and Maranbuy, and extends southwards to Callia (Wty, 143 3), In this region the sediments have been given the formal name Brack’s Creck Group (Noakes, 1949), Members of the Series outcrop at intervals in the valleys and along the dissected edges of the western part of the Arnhem Jand Plateau. Same at least of the formations traced into the western part of North Australia [ram the Ord River in Western Australia (Mattheson and Teichert 1945), appear to belong to the Agicondi Series. In Central Austrahia similar formations have been recorded at widely separated Iwealities and are being correlated with it. These include the head- wuters area of the Winnecke Creek, Tanami and adjacent area, The Granites Goldfield and vicinity, the Tennant Creek Goldfield and surrounding areas. the “Boltom Series” of the Hatches Creek Woliram Field and a number of other areas indicated on the General Map. All of these are regarded as members of the one series and because of the above correlation, will be referred to herein as the Agicondi Series. aRTG aes BYAREL SAVEN POAT PEESPNEL EL No ; Sas +5 SS S CROOVICLAN TEATIARY am G te MESOZOIC e [a] te = a * 45 Se MILES @ACHAEDZOIC PROTEROZOIC tae Uppar lower’ Midulte Fig. 2 Siretch Section across the Hart’s and Davenpart Ranges, As stilted aliaye, outerops correlated with this Series are well distribwied in the Territory. Many are relatively small inliers and do not provide good outcrops. The lirgest and most ¢emtinuons area and exhibiting the best outcrops as well as being exposed in many mine workings, is that occurring within the Darwin-Oenpelli-Maranboy triangle. In the Rrock’s Creeley Dis- trict, and supplemented by detailed mapping of numerous additional areas, the N.A. Survey was able to determine the existence of a thickness of 17,000 to 18,000 feet of sediments. This figure is a minimum as neither the top nor hase af the Series was determined. The present writer believes, however, thal the Galden Dyke Group as described in the official report (Hossfeld, 19364) contains the oldest known sediments of the Agicondi Series (Voigey, 1939a, per contra vide). The shallow water facies af some of the lower mem- liers of the Golden Dyke Group, chiefly conglomerates and sandstones, suggests that the hase of the Series may be at a shallow depth in this area. As a result of surveys during 1935, the present writer divided the sedi- ments In the vicmity of Pine Creek, into the Pine Creek and Union Groups with somewhat ill-defined transition beds. (Hossfeld, 1936b and c)}. The former consists predominantly of greywackes and other sandstones with some grit and slates. Many of the beds are tufts or partly tuffaceous. The Union Group consists chiefly of slates with subordinate sreywackes and grits. The slates weather to a distinctive red colour, which has Leen used in 4 tentative correlation of slates of other areas as for example those north of the Daly River (Ilossfeld, 1937c¢), Voisey (1939a) divided the Mosquita Creek sediments of that region inta three series, tle Golden Dyke, Pine Creck and Muldiva Series, While there was some justification for the initial division of the sediments by the present writer in 14933 and 1936 into the Pine Creel, Union, Golden Dyke Groups and the Daly River and Muldiva stages, at a time when little was known vf the suceessign, their division at a later date by Voisey inte three series appedirs to have been quite Uinevessary. T 114 The original field terms Pine Creek, Union and Golden Dyke Groups ete,, have last their importance and are being retained here merely for convenience of reference and description. The Agicondi Series of the Northern Territory consisted originally of arcnaceous and argillaceous sediments with a considerable amount of tufface- ous mitterial and very few calcareous deposits, Subsequent metamorphism has transformed the shales to slates, phyllites and schists. the greywackes aril other sandstones to schists and quartzites, and the few limestones to marbles. Tatts and prophyriecs have become schistose, grits and conglomerates have heen sheared and their components fattened in some localities, and a auceole of hornfels surrounds wholly or in purt many of the granite intri- sions. The degree of metamurphism varies in ditferemt localities and this induced some of the earlier observers to suggest the existence of different age-groups, and the possible occurrence of rocks of Archaeozuic age in North Australia. No break in cantinuity has been diseevered there, and the metamorphisin dues not approach in severity in any of the «reas examined, that which 1s sa vhuracteristic of the Archaeozoic formations of the Arunta Complex. The writer regards his “Bottom Series” of the Hatches Creek Wolfram Field as belonging te the Agicondi Series (Fig. 1). Tt 1s possible, of course, that these rocks which exhibit marked metamorphism, and consist as fur us examined of sheared amphibolites, porphyries and tufts, chloritic and quartz mic sthists, slates and amygdaloidal rocks, probably tufts, represent a group intermediate in age between the Archaeozoic rocks of the Arunta Complex and the Agicondi Series. However, similar formations outerop at intervals to the north-west in the cores of eroded anticlines until the Tennant Creek Goldheld is reached, Here they outcrop over a large area, forming the country rock of that poldfiell, and have been correlated by other workers with the Mosquite Creek Series. There is a close resemblance between the rock types of the scattered Central Australian areas such as Tennant Creek, The Gran- ites, Tanami and adjacent areas, Winnecke Creek and many other smaller outcrops, and those occurring in the Darwin-OQenpelli-Maranboy triangle of North Australia. This resemblance includes not only their dominant arenaccous-argillaceous character, but also the large proportion of tuffaceous materials, the paucity of limestones and the degree of metamurphism. The predominantly shallow-water facies sugyests that they were laid dewn in slowly subsiding basins, These appew ta have formed in a large mobile region extending aver most of, and beyond the Territory, Offshore and marginal volcanocs appear to have been numeruus, The composition of those tuffs in the Pine Creek District whith were examined microscopically stg- gests original lavas of intermediate composition, dacites or andesites, but probably the latter, Subsequently to the deposition of the sediments, a period of igneous activity resulted in the introduction wf basic material. This appears to have been chiefly doleritic or gabbroie and was introduced largely in the form of sill. Dykes and bosses have been mapped but are rare. In some areas such as the Golden Dyke, some thermal metamorphism resulted, particularly where relatively thin sediments were lacated hetween two sills. Asa result of subsequent uralitization and similar processes, these racks have been altered to amphibolites, The occurrence of similar amphibolites is not confined to rucks assigned to the Agicondé Series. Phey uccur im racks of Archaeozoie age in many parts cf the Arunta Block but are of DPost- Archaegavic age, They occur also in the Hatches Creek Group in the Daven- port Ranges, and are reported from similar formations in the adjacent Mar 115 chison Ranges. These amphibolites therefore, aceur at intervals throughout the Northern Territory, intruding formations considered as ranging from Archaeozoic to Middle Proterozoic (Figs. 1, 2 and 3), and prabably helong la two distinct periods. Subsequently to the basic intrusions but possibly contemporaneous in part, the regian experienced severe deformation. Folding af the sediments ant basic sills, resulted eventually in the development of structures of great variety. In many areas as, for example, in the Brock’s Creek District, but by no means confined to that area, dome and basin folds were developed. Tightly folded and overfolded structures occur in many localities and shear- ing, some of it of severe character. is recorded from numerous areas, Dynamic metamorphism of the sediments resulted in the formation af schists, cherts, quartzites and sheared rock types and the development of metamorphic minerals. This was followed by the introduction on a grand scale of acid igneaus racks chiefly granitic in composition but including some more calcic types The writer considers that the available evidence indieates that this 1tneous activity took place during the closing stages of orogeny of a later, anil uncunlormable series, the Davenport Series, and chranologically therefure helongs to a later section of this paper. Mippie Prorerozuic All formations believed to be of this age are being included in a division which is being named the Davenport Series. The name is derived from the Davenport Ranges which consist predominantly of these formations. Further, they were studied in detail in this area at Hatches and Wauchope Creek, and in the former locality were shown to lie unconformably on rocks correlated with the Agicondi Series which is regarded as of Lower Protero- zole age. The formations included in the Davenport Series are referred to two groups: (a) The Hatches Creck Group, (b) The Carpentaria Group. (a) Tue Tlarcues CREEK Grover Representatives of this group were mapped and examined in detail in the Hatches Creek Wolfram Field near the eastern extremity of the Daven- port Ranges of Central Australia. As a result the writer divided the forma- tions Into two and possibly three proups which were named the ‘“Rottom," “Watches Creek" and “Top Series,” with some doubts of the validity of separation of the last two. The “Bottom Series'’ has been correlated with the Agicondi Series, The “Tlatches Creek’’ and "Top Series” are now con- sidered to belong to one conformable sequence and are now named the Hatches Creek Group. In the area where they were first examined, these two divisions are lithologically dissimilar and separated by a major fauli. Extension of the examination to other areas of the Davenport Ranyes has shawn that they belong to one conmformalile sequence. The decision that the beds previously designated the “Hatches Creek Series” and the “Top Series” farm a small part only of the total conformable succession, as well as the occurrence of other groups regarded as of similar age, necessitates the restriction of “Hatches Creck’’ to a group, and the use of the wider geographi- cal term “Dayenport Series” for the whole successiuti. The basal members of the Hatches Creek Group consist of massive qtiartzites with some coarser beds, lying unconformably on the schistase formations. of the “Bottom Series.” At and near the unconfermable junction 116 they are sub-horizontal, but dips steepen markedly within a short distance to the northward and exhibit steep felding and overfolding to the north (Fig. 1). The repetitian by folding of the lowest formation, the quartzites, unt their resistance to eresion, have produced the characteristic landscape of the area which is dominated by sub-parallel ridges of quurtzites with less resistant! rocks outcropping tn the valleys. As a result access parallel to the strike ig easy, but difficult across tt. As one proceeds northwards across the strike, the repetition of hard and soft formations continues until an outerop of armphibolite 1s reached, This term ts used in a general sense to include tacks originally of various basic types bul predominantly doleritic, which have been altered to amphibolites. Once the amphibolites are reached the aspect of the country changes suddenly and becomes one of “islands" of sediments, sandstones and seméquartzites, outcropping as inliers in a “sea"’ of arnphibolite. The seilimenis ate folded, but do not exhibit the same intensity mor the same degree of metamorphism as do the arenacceus rocks to the south which have been transformed to dense quartzites, many of them glassy in appearance. The sequence appears te consist of a thick arenaccous formation af the base. originally mainly sandstones with some grits and conglomerate, succeeded by shales, tuffs and lava flaws, some of which may be sills, and containing thin beds of sandstone in their upper portions. The explanation submitted is that, since both are folded, the inlers of the north portion must have undergone this deformation befare the amphibolite bathohth was inuiwiled, The partial conformity of the margins of the amphibolite, and the somewhat less severe folding of the sediments now embedded in it, suggests that the intrusion occurred during the folding and probably during the later stages. The existence of this mass of basic material protected the inliers of sediments from further diastrophic effects and fram the dynamic metamarphism the results of which are evident in the southern half of the field and elsewhere in the region, (ligher mernbers of the Watches Creele Growp are exposed in a synclinal structure separated from the formations just described, by a major fault, The ares is in the north-western part of the Hateles Creel Wolfram Viele and the formations were previously referred to as the “Top Series.” The rocks , Lower Proterqzaic Outcraps _Archaeozoie = Osos Sod ge aso olan 3 20% d bo Boose So ° loo 200 300 MILES SS EE nae Fig. 5 Observed and inferred trends of the Davenport Series (Middle Proterozoic) of the Northern Territory, 131 it is essential to refer to differences of opinion held by the present writer as a result of additional evidence collected by himself. No evidence was obtained which would indicate the existence of a ¥ pattern in the Pine Creek-Darwin area. Although there are very numerous divergences due to deme and basin folding, the general trends range frotn west-northwest to north-northwest as far ta the south-east as Maranboy and the Yeuralba District in the western part of Arnhem Land, but exhibit a ponerse change ta the north and north-north-east towards and beyond enpelli, The generally concordant structure lines around the Brock’s Creek granite intrusion are due to a dome-shaped fold, of which there are a number, the Golden Dyke (Hossfeld, 1936a). being a good example. It can be stated definitely that the Brock’s Creek intrusion does not mark the location of a permanent change in strike of the sediments. It was demonstrated in the preceding section that the present writer disagrees with Jensen in the latter's reference of the McArthur River lime- stones and the Redbank deposits (Jensen, 1940) to the Cambrian and Post- Nullagine mineralization respectively as quoted by Hills (op. cit.), Madigan’s reference (1937) to post-Cambrian unstressed granites also is contrary to the observations ta date of the present writer and consequently so are the conclusions derived from that correlation by Hills (op. cit.}. The present writer's observations and all other available evidence indi- cates that the Agicondi Series continues throughout the western part of the Arnheim Land region and that the Davenport Series constitutes the eastern sector. The Buldivan Series, capped by residues of the Lower Cretaceous Mullaman Group, forms a relatively thin cover, but of sufficient thickness to give the Arnhem Land Plateau its comparatively high elevation. This interpretation supports the previously supposed existence of festoons of ancient rocks which Wade (1924) found difficult to explain. D. LATE PROTEROZOIC AND CAMBRIAN Deposits previously referred to this age-grouping are widespread in the Northern Territory. Differences of opinion have been expressed regard- ing the ages of the oldest deposits of the sequence, but there is general agree- ment that the formations occur in two distinct geographical divisions. One, outcrops to the north of the Arunta Block, the other occurs in the Amadeus Geosyncline to the south of the above block, THE BULDIVAN SERIES Although the deposits of this series had been recorded previously by' several observers, they had received no formal name until 1946 when they were named the Buldiva Series by the N.A. Survey (Hossfeld, 1937g). The term was derived from the Buldiva Area, the first locality where they were mapped and examined by the above organization. The name is being changed herein to Buldivan, as suggested by the Australian Code of Stratigraphic Nomenclature (Raggatt, 1950). Attention was directed to the deposits of this series during the economic. survey of the Buldiva Area, because they and younger rocks were found to act as blankets, obscuring in many areas the mineral-bearing Proterozoic formations. The deposits to which the term Buldivan Series was applied, rest with 4 violent unconformity on the métamorphosed, highly folded sediments of the Agicondi Series and on the intrusive granites and basic igngous rocks. (Fig. 3.) In most instances where the contacts were examined in the type 132 area, they were found to be faulted against the older rocks. However, good contacts showing the unconformable junction, were observed subsequently outside the type locality. The existence of the unconformity was confirmed by the regional mapping and the consistent differences in lithology, structure and degree of metamorphism between the Buldivan Series and the underlying SY a 190 200 309 MILES Es a | __p-—n__ Approximate N's S™ Limits of Ordovican Transgression N'™ of Avunta Block Fig. 4 Approximate limits of Cambrian, Ordovician and Lower Cretaceous Submergences of the Northern Territory. 143 rocks. In general, the members of the Buldivan Series exhibit gentle dips and minor folding only, except near fault contacts where dips of up to 30° and several local crumplings were abserved. The region occupied by this series is divided partly hy a narrow, elevated area of older rocks, many of them quartzites, which belong to the Davenport Series, This feature extends from the vicinity of Newcastle Waters in a southerly direction to a short distance north of Tennant Creek. The resulting geographical divisions of the Buldivan Series are being named the Buldiva-Wiso and the Barkly Basins, (Fig. 6), and the dividing area the Asburton Peninsula. The Buldiva-Wiso Basin extends from the Douglas River in a southerly direction probably as far as the sector west of Tennant Creek. The Barkly Basin extends in a south- easterly direction into Queensland, The occurrence of inliers of older rocks in the Victoria River region suggests the existence of other smaller basins such as were mapped in the Western Austrlian border areas, (Mattheson and ‘Teichert, 1945), As the map will show, the boundaries, many of them necessarily inferred. are irregular and there are some outlying areas. Some of these irregularities are believed to be due to differential uplift by folding or faulting, and the subsequent removal of the less resistant deposits. The vast continuous region over which these sediments exist, the out- liers as well as sttuctural considerations, suggest the former continuation of these sediments over almost the whole of the Northern Territory, north of the Arunta Block (Fig. 6). (a) Tue Burpiva QuartziTR In the northern sector of the Buldiva Basin, the Buldiva Quartzite is the basal formation of the series, (Hossfeld, 1937g), (Voisey, 1939a), (Noakes, 194%), It consists predominantly of massive arenaceous sediments which have been altered in most localities to a dense, hard quartzite, but consists chiefly of quartzose sandstones in others. The sequence includes some grits, thin conglomerate bands and some shale. The original report of the type area of Buldiva (Hossfeld, 1937p) states: “The quartzites exhibit well developed ripple marks, worm-iracks, rain prints, sun cracks and bands of weathered inclusions which may have been either fossils or mud galls. These features are evidence of the shallow water deposition of the quartzite, These features are not restricted to any one sectian of the sequence, but have been found through a thickness of several hundred fect of quartzite, and over a length of forty miles northwards from Buldiva," The Buldiva Quartzile Formation is strongly jointed and the dominant trends are north-westerly and north-easterly. Actual averages of numbers of joint directions measured gave bearings of 320° and 57° for the Buldiva area, and 315° and 63° respectively for the Arnhem Land area. A third trend in the Buldiva area is approximately east-west; in the Arnhem Land area. the third joint direction is variable, the observed bearings being between 27° and 42°. The jomting is predominantly vertical and together with the prevalent low dips, is responsible for the rugged topography, much of it inaccessible. No accurate measurements of the thickness of the Buldiva Quartzite in the Ruldiva area or the possible variations in that thickness elsewhere, as for instance, in the Arnhem Land Region, are available. In the type area it appears to be of the order of several hundred feet, and the present writer has seen no evidence to suggest any marked departure from that estimate in other parts of the Territory. The estimate of more than a thousand feet (Noakes, 1949) in folded areas (apparently the Arnhem Lind area) appears lo the present writer excessive. 134 Outcrops of massive quartzite are well distributed in the north-western sector of North Australia. They are responsible for the formation of trémen- dous cliff faces along the dissected western edges of the Arnhem Land Plateau and along the western sector of the southerly margin. Though some may be older, they are correlated provisionally with the Buldiva Quartzite. The quartzite outcraps which occur at intervals along the north aad east coast of Arnhem land and on Groote Eylandt may represent beds of the Davenport Series. Where observed, the Buldiva Quartzite and other formations of the Buldivan Series together with members of the “Lower Cretaceous” Plateau sandstones, form the cover rocks on the Agicondi and Davenport Series over a large part of the Arnhem Land Plateau, The former are continuous with the Agiconili Series of the Darwin-Oenpelli triangle and the latter continue across the Roper River to the Carpentaria Group of the McArthur River Area. It is largely due to the presence of the later cover rocks that the plateau owes its relatively high elevation, There is no evidence to suggest that the easterly dips of the Buldiva Quartzite at the western margin indicate the existence of a synclinal structure over the plateau. All of the observations made, indicate rather a number of gentle flexures and suggest the existence of some cross-folding with resultant dome and basin folds. Wherever the valleys and dissected margins of the plateau have been examined, members of the Buldivan Series or of the Mullaman Group, or both, occupy the upper sections and form cliff-faces, exposing in the lower sections and on the Aoors of the valleys rocks of the Agicondi or Davenport Series or igneous rocks intrusive into them, The Buldiva Quartzite outcrops extensively between the Finniss River and Collia, and extends southwards. Outcrops at Tanami, in the Gardiner Range and at intervals to Winnecke Creek may be its equiva- lents. The absence over large areas of metamorphism, mineralization and imarked deformation from same quartzites belonging to an older series, makes correlation of widely separated outcrops difficult and in many instances impossible. It may well be that some outcrops labelled Buldiva Quartzite belong in fact to the older, the Davenport Series. As the Buldiva Quartzite is the basal sedimentary formation of the Buldivan Series in the type area, the northern sector of the Buldiva-Wiso Rasin, its age and correlation will be discussed with the rest of the Series. At intervals between 16 and 18 degrees South Latitude, along the border area of Western and North Australia, Mattheson and Teichert (1945) have mapped a great thickness of basic fows with agglomerates. They consider that these volcanics form the basal portion of the Cambrian sequence in that region, The volcanics are succeeded by calcareous and argillaceous sediments the oldest of which is regarded as Late Lower Cambrian, and is probably the equivalent of the base of the Daly River Group. The volcanics extend eastwards ito North Australia into the Wave Hill District, Their extent and positions in the sequence have not been determined in that region. The existence of volcanics at the base of the Buldivan Series has been suggested byt not proved so far in other parts of the Territory. Ta the southern portion of the Buldiva-Wiso Basin, and in the Barkly Basin, the lowest members in most localities are relatively thin arenaceous beds or limestones of variable types, (b) Tue Daty River Grove ox Upper Bucpivan Series The deposits aboye the Buldiva Quartzite were described in the NLA. Survey Report (Hossfeld, 1937g) as follows: “overlying the quartzites .. . are limestones, argillaceous limestones, slates and fine-grained sandstones. 135 On a hill to the north-west of Collia, and near the western edge of the area, well preserved stromatoliths and cryptozoa were found in limestones ittter- bedded with purple slates. The rocks are considered tm be near the base of the beds overlying the quartzites. Similar structures were found near North- ern Creek alongside the new road to Daly River, On what is probably a higher horizon Girvanella was located between the Fish River and Collia on the Buldiva-Collia track.” No formal name was given fo these sediments as all of them were included in the Buldiva(n) Series. They were divided merely into the Lower Buldiva Series (Buldiva Quartzites) and the Upper Buldiva Series. Votsey (19392) used the term “Daly River Limestones,” which Noakes (1949) suggests be named the Daly River Group, The adoption of the latter tert by the present writer does not imply agreement with Noakes (op. cit.) that the name “Buldiva Series” should be eliminated. . Lying conformably above the Buldiva Quartzite in the type area, and forming a continuous series without an erosional break (Noakes, 1949, per contra vide), there follows a transition zone of irregularly alternating, relatively thin beds of limestones (some of them cherty) and quartzites. These pass upwards into fossiliferous limestones of the Daly River area, and are succeeded by the other members of the group, Some fossil localities have been referred ta above. Others are given in the description of various areas by several authors. The additional localities examined by the present writer are on the Douglas River where pteropod limestones (Biconulites “Salterella" hardmani) and Girvanella limestones outcrop, and near Chinaman Creek south-west of Katherine, where Girvan- ella-like remains weather from the sediments in immense numbers. There is general agreement in regarding the lower members of the Daly River Group as Upper Lower Cambrian. Sediments of Cambrian age outcrop, or are obscured by a thin veneer only of younger rocks, over very large areas in the Northern Territory. They extend from Western Australia into the Territory on the Ord River Region and continue apparently without a break, but ohscured in many places by younger rocks, ta the Daly River Region. They continue eastwards across the Overland Telegraph Line, forming the Barkly Tableland, and thence into Queensland. The large, unmapped area bounded approximately by Newcastle Waters, Wave Hill, The Granites and Barrow Creek, is believed to be urnder- lain at shallow depths by Cambrian sediments. The eastern portion, west of Tennant Creek was named by the writer the “Wiso Area” in 1937. (A.G.G.S.N.A. 1938a) and the natie Wiso Tableland is proposed herein for the whole region. The Buldivan Series was defined in the publication referred to earlier {Hossfeld, 1937g). The writer, in this and subsequent references, included in that term not only the basal formation, the Puldiva Quartzite, but also the remaining beds of the sequence, the limestones, shales and associated sedi- ments of recognized Cambrian age. (Hig. 3). Since then, Noakes (1949) has eliminated the term, and “Buldivan Series” has been used for the Buldiva Quartzite alone (David and Browne, 1950). The present writer is convinced from his field observations in the area to the east of Collia-Buldiva where good sections exist, that in this area at least, the sequence represents can- tinuous deposition from the base of the Buldiva Quartzite into the Daly River Group. Statements to the contrary by Noakes (1949) notwithstanding, the present writer adheres to his previously published opinion that the Bulvida(tt) Series includes the whole of the above sediments. 13 Noakes (1949) cites as his main argument the observation that in many parts of the Brock’s Creek District the Cambrian limestones rest directly on the Agicondi Series. In this connection Noakes did not refer to the known existence of fault boundaries in this region, an area in which dislocation by faulting is recognized as severe and extensive. The prevalence of such fault junctions and the apparent stratigraphical anomalies which they have pro- duced along the western and eastern margins of the Cambrian basin, make it highly probable that they are responsible wholly as they are known in part to be, for the apparent anomalies quoted by Noakes. The discovery by the présent writer of a continuous section above the Ruldiva Quartzite into the Daly River Group, and the juxtaposition and upparent conformity of the two units over such a large portion of the Northern Territory, make it improbable that the erosion interval, postulated by Noakes, exists except perhaps as a local feature, which may have occurred as a fesult of transgressive deposition in such a large area as the Buldiva Basin, The twa units then, constitute the Buldivan Series. As stated earlier. it is generally agreed that deposition of the Daly River Group commenced in the upper portion of the Lower Cambrian and it follows that the formatian which is now the Buldiva Quartzite. was deposited during the earlier part uf that epoch. Deposition may be wholly Cambrian or it may have commenced during the last stage of the Upper Proterozoic and continued into the Lower Cambrian, {c} Votcanics Numerous exposures of extrusive rocks of great variety are known to occur in North Australia. Jensen (Cwlth. Aust. 1915c) records dolerites, diabases, basalts, ande- sites, rhyolites, phonolites, trachytes and calci-trachytes as weil as tuffs of the above, and porphyries. In view of the wide tange of composition it is suggested that they may belong to more than one epoch. However, Noakes (1949) while acknowledging the incompleteness of field evidence, Suggests that the volcanics are of Lower Cambrian age, overlie the Buldiva Quartzites and underlie the Daly River Group, and correlates them apparently with the Lower Cambrian voleanics of the Kimberley Tegion of Western Aus- trlaia, Opinions expressed by previous observers show wide divergences. There are several areas to which special reference is required at this stage. These are the Edith River, Maude Creek, Collia, Tipperary-Daly River Road, and Victoria River. THE EDITH RIVER VOLCANICS The observations (Noakes, 194%) of fault boundaries and the resultingr juxtaposition of the volcanics to the Agicondi Series, to the Buldiva Quariz.- ite, and the Daly River Group, make a defininte determination impossible at this stage, The present writer considers, however, that in view of the recorded occurrence of numerous tuffs and tuffaceous sandstones. in the Agicondi Series in that locality, the recorded folding of the deposits, and metamorphism of some of the racks, their reference to the Agicondi Series appears logical. They ate regarded therefore, by the writer as tentatively of Lower Proterozoic age, THE MAUDE CREEK VOLCANICS The examination of the goldfield of that name (Cattle, 1937b) showed that the tuffs and porphyries of this area can he correlated with reasonable certainty with other deposits of the Agicondi Series. A section by Gray (Cwlth. Aust., 19154) and the accompanying text indicates, hawever, nov only his recognition of the existence of Precambrian tuffs, but also the 137 occurrence of small deposits of volcanics in the Cambrian sequence. If sub- sequent work confirms the existence of volcanics of two ages in this locality, it will explain to sotme extent the differences of opinion expressed in the past, and will indicate the extension eastward even though perhaps inter- mittent, of the volcanic accumulations at or mear the base of the Buldivan Series near the Western Australian border. Other volcanics such as the Collia and East Victoria River areas and possilly the Tipperary-Daly River road occurrence are regarded by the writer as Post-Cambrian and, as will be shown later, tentatively as Devonian, The work of Mattheson and Tetchert in the border areas resulted in a threefold division of the Cambrian succession, at the base a great thickness of basaltic rocks including agglomerates, followed by the Negri and Mt, Elder Series of Cambrian sediments. Their extension fnto North Australia was demonstrated but until detailed mapping is done in the extensive Victoria Riyer drainage basin, these divisians cannot he carried through. The whole area in which these three groups are believed to outcrop, is shown on the geological map herein, as Cambrian without any attempt at differentiation. An exception is made of the volcanics mapped by earlier workers in the eastern marginal areas of the Victoria River drainage basin. On the evidence of other observers together with the writer's own obseryations, it is sugpested that these could be Post-Cambrian and correlated provisionally with the Collia Series, which is being regarded tentatively as Devonian, Tue AmMaDEUS GEOSYNCLINE The Archaeozoic rocks of the Musgrave and Arunta blacks are separated by the geosynclinal sediments of the Amadeus Geosynicline. The maximum width of this feature how ranges from 100 to 160 miles. (Fig. 6), 1t is known to extend for more than 300 miles in a general east-west direction, but is stated to continue for at least another 150 miles towards and into Western Australia, (Ellis, 1936). Its northern margin probably lies near the southern end of Lake Mackay. Hf the postulated continuity of the Amadeus with the Flinders-Mt. Lofty Geosynecline is accepted, there exists a known length of at least 1,000 miles with unknown extensions to the west. The sédiments which rest with violent unconformity on the Arunta Complex (PL. 11, 1) have been investigated by a number of workers, especially Brown, Tate and Watt, Chewings, Ward, Mawson and Madigan, Reference must be made here to the remarkable opinion expressed by Ellis (1936), that there is no unconformity at the base of the Pertaknurra Quarttzite and that this formation is part of the Arunta Complex, The exist- ence of the nonconformity has been established by regional mapping, in- dividual sections, as well as by the discovery of exposed contacts, One of these 1s visible in a small quarry south of Alice Springs in Heavitree Gap. Here, soft argillaeeous beds rest unconformably on massive porphyritic pranite and are overlain by the Heavitree Quartzite dipping to the south away from the contact. In a paper by Mawson and Madigan (1930), the Pre-Ordovician racks above the Arunta complex were divided in ascending order into the Pata- knurra and Pataoorrta Series. Madigan (1932a) subsequently changed the prefix Pata to Terta as being the cotrect spelling of the native word used, In the above paper Madigan subdivided the former Pertalknurra into Perta- knurra A and B and an unconformable series above, which he named the Pertatataka Series. Above this follow the Pertaoorcta (Cambrian), the Lara- pintine (Ordovician), and finally the Pertnjara {Post-Ordovician) Series, a total thickness of sediments as measured along Ellery's Creek in the West- 138 ern MacDonnell Ranges of nearly 25,000 feet, In the detailed description and measurements of the Post-Archaeozoic and Pre-Ordovician sediments of Ellery’s Creek, Madigan gives the total thicknesses of the series from above downwards as follows: Pertaoorrta Series - - - 3,151 feet Pertatataka Series - - - 3,24 feet Pertaknurra Series B - - 1,909 feet {Heavitree Quartzite) A - 1,440 feet However, in the area fram Alice Springs westwards to the vicinity of Finniss Gap, tt can be seen that Madigan's Pertaknurra A or Heavitree Quartzite does not rest directly on the Arunta Complex but is underlain hy soft argillaceous beds ranging in thickness probably from 12 to 20 feet. During his examination of these sediments in the Eastern Macdonnell Ranges, Madigan (1932b). discovered a bed of limestane three feet thick, vontaining numerous well-preserved Archaeocyathinae, Biconulites (Salter- ella) were found in this formation, and thus the tentative determination of the Pertaoorrta Series in the western Macdonnell Ranges as Cambrian, was confirmed. The division by Madigan (1932a) of the Pre-Ordovician rocks into three series, the Pertaknurra, Pertatataka and Pertavorrta, ts based chielly ett lithological and palaeontological evidence. No stratigraphical nor struc- tural break has been discovered from the base of the sequence to the highest members of the Larapintine Series, The sole evidence of any break in deposi- tion appears to be supplied by the conglomerates near the buse of the Perta- tataka Series. “The boulders included granite and granite-gneiss, bioctite- gneiss, biotite schist, quartzite and many stromatolith fragments, chiefly silicified nodules from the limestones, all recognizable at once as from the immediately underlying Arunta Complex and Pertaknurra Series.” (Madigan, 19322}, The possibility that the assuciated breccia bands were of the nature of crush lines connected with overthrusting was suggested but discounted by the long continuation (at least thirty miles) of the quartzite formation of which they form a part (Mawson and Madigan, 1930), The severe deforma- tion of the sediments in this and other areas marginal to the southern borders of the Arunta Block, and especially in the type areas of the Jay and Ellery’s Creeks, indicates the necessity for a re-examination of the evidence for Madigan’s sequence and thicknesses. The sediments of the Amadeus Geosynctine have been folded and faulted extensively. Many closed structures have been recognized. Some appear in the various published papers referred to, but the majority were delineated by the present writer. A generalized representation of the structura! features appears on the attached gevlogical map. It is to be noted that the average trend of the folding axes approximates to a sigmoidal curve bearing in a north-westerly south-easterly direction at the two observed limits of the geosyncline, Severe deformation is exhibited by the sediments marginal tu the southern borders of the Arunta Block over a distance from east to west of approximately 250 miles. In the southern portion, marginal to the northern borders of the Musgrave Black, outcrops are widely separated and little is known of the structure. Sufficient outcrops are available to indicate the existence of a highly disturbed area to the east and south-east of Lake Amadeus, in which area the faulted Kernot Range, the basin fold of Mt, Connor, and the subvertical sediments of the Ayers Rock Horst, form prominent outcrops. The most disturbed area, however, is that to the east and south-east of Alice Springs. Intense folding and fracturing exists in this sector, where the trends appear to change their direction to the north-west south-east in a relatively sharp curve (Fig, 6). 13 Here overfolding, overthrusts and faulting generally are so severe that, even with the aid of aerial photographs, the structures are difficult of imterpreta- tion, ‘The greatest horizontal displacements cbseryed, and measured approxi- mately, appear to have been produced by a relative lateral movement along a shear plane, of about 7,000 feet. This highly disturbed sector of the basin is in the area where the generally east-west trends swing to the south-east. Such a change of direction ig. ta be expected if the Amadeus Geosyncline is a virtual continuation of the Fiinders-Mount Lofty Geosynciine and forms a part of the former deposi- tional basin marginal to the ancient landmass of Yilgarnia, (Andrews, 1937; Mawson, 1947}, Towards the border of Western Australia the folding appears to decrease pradually in severity. The geosynclinal structures may continue to the north-west into Western Australia, but to the north the beds occur as large residuals over a wide zone and appear to pass gradually into the less disturbed sediments of the southern continuation of the Buldiva trans- gression, In the northern marginal areas ol the geosyncline, the Pertaknurra (Quartzites have suffered severe deformation and dislocation, Reversed dips are common along the unconformable junction with the Arunta Complex, overriding of the older racks on a large scale, fault displacements and block faulting have produced very complex structures. An anticlinal structure was formed on part of the southern segment of the Arunta Block. The northern limb can be recognized by the existence of beds identified with the hasal formation, the Fertaknurra Quartzite, in elevations such as Simpsan’s Gap (Hossfeld, 1937¢), Chewings Range, etc., to the west of Alice Springs, Block faulting has broken the continuity and resulted in the occurrence of numerous isolated outcrops of this quartzite. In the mest distorted sector, the area east of Alice Springs, the resulting structures are exceedingly complex. Out- liers of the Pertnaknurra Quattzite occur in close proximity to much older (juartzites, and such contiguity has misled some observers inte correlation of beds, of different ages. The conclusions drawn from such erroneous correla- tions have been far-reaching, and, quoted by subsequent workers, have pro- duced considerable confusion, It will be necessary, therefore, to discuss at length the correlation of the Pertaknurra Series and deductions drawn from such correlations. The incompetent beds, chiefly limestones und shales immediately above the Pertaknurta Quartzite, have been distorted so thoroughly in many areas including Ellery's Creek, that measurement of this part of Madigan’s type section (1932a) appears impracticable. Nevertheless, sections were observed in the region where the local thicknesses and sequence can be determined, The quartzite (Mt. Blatherskite}, Madigan’s No. 2 Quartzite and re- garded by him as the base of his Pertatataka Series, which outcrops to the suuth of Heavitree Gap, is considered by the present writer, on the basis of its outcrops, overlying sequence and lithology, to be a repetition of the Tertaknurra Quartzite of Heavitree Gap, Madigan’s No. 2 Quartzite in the Ellery’s Creek Area which contains the conglomerate and breccia bands referred to earlier and which was regarded by Madigan {1932a) as the basal member of his Pertatataka Series, appears toa be very localized in its occur- tence in the Western Macdonnell Ranges, and has not been recognized in the Eastern Macdonnell Ranges, (Madigan. 1932b). It is true that the con- wzlomerate bands could indicate discontinuity of deposition, but this could have resulted from local uplift by folding or faulting and not of the sequence as a whole, Deposition except for positive ar negative movements of the land, resulting in non-deposition or in overlap in some localities, is con- shiered unbroken from the base int the Ordovician and Post-Ordovician eds. 140 Madigan himself admits that no unconformity or break in deposition has been discovered, Nevertheless, he states (Madigan, 1932b, p. 106) “The Pertaknurra has definitely been intruded by granite, and is aunferous, None of the later series have been so intruded and no remains of them have been found inside the berders of the ranges. The orogenic movements which dis- rupted the Pertaknurra and engulfed part of it in ihe Arunta Complex. preceded the deposition of all younger formations . . ." “the Pertaknurra is placed amongst the oldest of Australian sediments and assigned to the Older Proterozoic, and correlated with the Mosquito Series of Western Australia . . .” “Pertaknurra time closed with the greatest revolution which has ever affected the Macdonnells . . .” “This was a time of great granite intrusion in Central and Western Australia, and a most important metallo- genetic epoch,” The above premises and conclusions are not in accordance with Madigan's statement that na unconformity had been discovered, and is completely at variance with the opinions held and expressed by the present writer (Hossfeld, 1937), and subsequently by Voisey (1939b). Reference tu granitic intrusions and metallogenesis earlier in the present paper indicate the writer's views on those aspects. Madigan's conclusions appear to have been based on several features. 1. The observed overthrust faulting of the Pertaknurra Quartzite and the severe crumpling and folding of the overlying sediments, which as Voisey (1939b) has shown is of Post-Ordovician age. 2. The assumption following Chewings (1928) that the White Range and the Bald Hill-Winhecke Quartzites are down-faulted metamorphosed remnants of Pertaknurra Quartzite, and the conclusion therefrom of a tremendous orogenic upheaval, with subsequent granitic intrusions ant mineralization. 3. ‘lhe existence of limestones in close proximity ta some of the older quartzite outcrops, thus affording a correlation with the lower portion of the Pertaknurra sequence. As pointed aut by Voisey (op. cit.) once these errors of correlation by Matigan are realized, there is no need to postulate a marked time break above the Pertaknurra Series. It is no longer necessary to ignore the over- whelming evidence not only of regional continuity of deposition, but alse of Post Ordovician orogeny. The present writer agrees with Voisey that the term Pertatataka Series is superfuous, and the original division pf the sequence by Mawson and Madigan into two series, the Pertaknurra and Pertaoorrta should be retained. AGE AND CORRELATION The Pertaoorrta Series has been determined on palaeontological evidence as of Cambrian age. Browne (David and Browne. 1950) regards the upper- most members of Madigan’s Pertatataka Series and consisting of 930 feet of purple fissile slate with green bands, calcareous slates and reddish sand- stones, as equivalent to the Purple Slate Stage (Adelaide System) and placed in the Lower Cambrian, This sequence has been named the Marinoan Series by Mawson and Sprigg (1950), who regard it as the uppermost division of the Proterozoic. In view of this published opinion, the age-grouping by Mawson and Madigan of the Amadeus Geosyncline sediments is being retained at present. This implies that the Pertaoorrta Series is of Cambrian age, and that the earlier deposits (Pertaknurra and Pertatataka Series) are Proterozoic, 141 The main divisions of the Adelaide System are the Para, Narcnota (Hossfeld, 1935a, pp. 46, 61-63) and the Marinoan Series (Mawson and Sprigg, 1950), The Para and Narcoota Series were subsequently called the Torrensian and Sturlian respectively by Mawson and Sprigg in 1950 (op. cit.)- Attempts have been made by some authors to correlate the Precambrian sequence of the Amadeus Geosyncline with the Adelaide System. Such correlations are tentative at present, partly because the Sturt Tillite which is such a marked feature of the Narcoota Series of the Adelaide System, has not been recognized so far, in the Amadeus Geosyncline. At what stage during the Proterozoic Era deposition commenced cannot be decided at present. The writer can see no grounds except the mistaken correlations of Madigan discussed abaye, for regarding the Pertaknurra Series as Older Proterozoic and equivalent in age to the Mosquito Creek Series (Agicondi Series), or even to the Middle Proterozoic {Davenport Series), The Pertaknurra A and B and the former Pertatataka Series will be referred to collectively as the Pertaknurra Series and are regarded as of late Middle to Upper Proterezoic age. No contemporary volcanic activity has heen recorded from the sediments oj the Amadeus Geosyneline which is classified as a miogeosyncline. The available evidence indicates that the orogeny of the Amadeus Geo- syncline took place after the deposition of the TPertnjara Series (Post- Ordovician). No igneous intrusions nor mineralization due to igneous activity have been observed by the writer. The only references to igneous intrusions are those of Madigan, most of whith deal with beds older than the Perta- knurra and mistakingly correlated with it. In the Jervois Range area Madi- gan refers to granite intrusive into Cambrian beds, but does not show this in his sections. Wherever in that sector the present writer observed outcrops of Cambrian age in close proximity to granite, they were separated by major faults. Until some definite evidence of Cambrian intrusions in that area is produced, the present writer maintains that the sediments of the Amadens Geosyncline and adjacent areas were, in that district as elsewhere, completely free of igneous activity. The earliest known deposits of the Buldivan Series, the transgressive deposition of which probably began from the north-west, are believed to belong to the base of the Cambrian. Deposition in parts of the basin apparently conlinued into the Upper Cambrian and with a possible time-hbreak, into the Ordovician. Since depositian apparently began carlier and continued longer in the Amadeus Geosyncline, and communication probably was established with the Cambrian basins to the north, transitional areas should exist to the north-east and north-west of the Geosyncline. Those to the east are buried beneath the Mesozoic sediments of the Great Artesian Basin. In the west where such transitional deposits may exist. gealogical outcrops are scarce in the large region covered almos{ completely hy recent sand dunes (Hossfeld, 19404), Such outcrops as do exist are covered to a large extent by durterust, which in those peneplaned areas has not been removed by denuda- tion and hence renders identification difficult. However, the dissected regians of the Kimberley District af the north-west of Western Australia, and the Victoria River Downs and Wave Hill Districts offer considerable prospects of adding io our knowledge of the Late Proterozoic—Lower Palaevzvic succession. The classification, as Pertaknurra remnants, of numereus gutliers of arenaceous. sediments on the Arunta Block by previous. observers, has not been established beyond reasonable doubt, That such do occur is shown by the recognition of such a remnant at Simpsen’s Gap (Hossfeld, 1937) 142 and by the correlation of part at least of the Chewings Ranges and others, However, the quartzites of those areas are lithologically and in other respects so similar to those of definite Pertaknurra age in the vicinity, that there is littie doubt of their correlation, Although some of these quartzites have been faulted into the Archaeozoic rocks of the Arunta Complex, they exhibit none of the metamorphism nor mineralization observed in the White Range or other similar quartzites. They have not “been absorbed into the Complex,” but retain their original characteristics. The Amunurunga Series (Tindale, 1933} and numerous other outliers on the Arunta Block Have been discussed earlier. These beds which are lightly metamorphosed are violently unconformable on the Archa¢ozoic rocks and are overlain unconformably by beds (predominantly quartzite) corre- lated with the Pertaknurra Series, At the eastern extremity of the Arunta Block, notably in the Jervois Ranges, the arenaceous and argillaceous sediments lying unconformably on the Arunta Complex have been correlated by Madigan (1932b, 1933, 1937) with the Pertaknurra Series. As stated earlier, the present writer regards this as improbable, and has correlated them provisionally with the Daven- port Series, E. ORDOVICIAN Rocks of Ordovician age outcrop at intervals over large areas tn Central Australia, They have not heen recognized so far, from North Australia, but such sediments may exist in the largely un-mapped region of the narth- west, between Barrow Creek and the Lower Victoria River. Ordovician sediments form a portion of the deposits of the Amadeus Geosyncline between the Musgrave and Arunta Blocks, Extension of these beds into Western Australia in the Robert Range, Walter James Range and others is suggested by Ellis (1936). Eastwards, their outcrops have been recognized as far as the Todd River, and again, in the vicinity of the Queensland border, where they out- crap in the Toko Ranges which are practically unexplored, [t is believed that the Archeaozoic rocks of the Aranta Complex and sediments of the Amadeus Geosyncline outcrop in that region and ta the suuth-east, until they are obscured by the Mesozoic sediments of the Great Artesian Basin, and ly recent atolian deposits. From the Toku Range, deposits of Ordovician age have been recordril westwards at intervals, on and near the northern margin of the Arunta Riock probably to a short distance west of Barrow Creek (Pl. III, 1). Definite fossil evidence has been obtained from the Toko, Tarlton and Dulcie Ranges and their continuity further to the west is based on lithological and strati- graphical features, In the region on the northern flank of the Arunta Block they do not form part of the thick range of sediments developed in the Amadeus Basin. They appear to form part of the Barkly Basin succession, but may be separated by an unconformity from the Cambrian sediments. In the Barrow Creek District and adjacent areas they overlap the Cambrian beds and rest unconformably on the Arunta Complex. Such an overlap is suggested also for a part at least of the Tarlton Ranges. Deposits of Ordovician age in the western part of the Amadeus Geo- syncline were inyestigated in 1894 by Tate and Watt during the Horn expedition and the results published in 1896. Fossils collected at that time and those collected earlier hy H. Y. L. Brown, were identified as of Ordovi- cian age, and the series received the name Larapintine , It was demonstrated later (Mawson and Madigan, 1930), that the stratr graphy of the region as described by Tate and Watt (1896) and Ward (1925) 143 required correction, but this did not alter the recognition of the Larapintine Series as Ordovician. Subsequent investigations by Madigan (1932a) added considerably to our knowledge of the stratigraphy, lithology and fossil contents of the series, The Larapintine portion of the Ellery’s Creek type section (Madigan op. cit.) shows a total thickness of 5,986 feet, chiefly arenaceous beds with thin bands of highly fossiliferous limestones and some shales, nearly midway in the sequence. Variations in thickness of some of the recognized beds have been recorded in other areas of the Amadeus Geosyncline. Thus the thickness of the lower quartzites was found by Tate and Watt to be approximately 6,000 feet in the Levi Range with a decrease of and absence of some beds, making the total thickness in that area approximately 7,000 feet, South of the Eastern Macdonnell Ranges the Larapintine deposits, where examined, appear to be relatively thin. Too little is known of this region, however, for definite statements of the original thickness of the series. North of the Eastern Macdonnell Ranges, the existence of sediments of Ordovician age was reported first from the Dulcie Range (ITossfeld, 1931; Tindale, 1931; Madigan, 1932h). Extensions to the eastward towards thé Queensland border were investigated by Madigan in the Tarlton and Toko Ranges (Madigan, 1937). Sub-horizontal sandstones, grits and conglomerates ta the east of Barrow Creek were correlated tentatively with the Ordovician (Hossfeld, 1937i). The limited vertical exposures of the sub-horizontal sediments to the north and east of the Arunta Block make an estimate of their total thickness impossible at present. The maximum observed appears to be about 800 feet, recorded from Mt. Ultim in the Dulcie Ranges by Tindale (1931), They will be referred to as the Dulcie Series. In the Amadeus Geosyncline the Larapintine Series exhibits predominantly a littoral or shallow water facies, indicating that throughout the deposition of about 7,000 feet of sediments, sinking of the floor of the basin kept pace approximately with the rate of deposition. Calcareous beds are few and thin in the greater part of the region, but become increasingly numerous to the east and towards the Queensland border (Madigan, 1937} indicating greater depths in that direction. The recorded occurrence in the central part of the area of pscudomorphs after sodium chloride crystals, suggests the existence of temporarily land-locked arms of the sea and their evaporation. Within the great thickness examined, recognizable fossils exist in a zone of less than one hundred feet thick, in the western part of the region. Further to the east, however, indications are that fossil remains are distributed through a wider zone of deposition. The sediments of the Larapintine Series to the south of the Macdonnell Ranges form many large, continuous oulcreps, but occur also as numerous, scattered residuals, or as long, continuous beds along the strike. Such dis- continuity of outcrop is due, not only to folding and faulting, but also tea removal by erosion and to their burial by later deposits. The Dulcte Series sediments to the east and north, which are sub- horizontal or gently flexured, form mesas, some of very large extent, resull- ing from the dissection of a former continuous elevated region. Whereas in the Amadeus Basin the Larapintine sediments represent portion of an apparently uninterrupted sequence from Late Proterazoic or Early Cambrian times, the corresponding Ordovician deposits on the east and north of the Arunta Block are of the transgressive type, 144 The geosynclinal deposits of the Amadeus Basin have undergone com- pression and now exhibit many closed folds, and numerous faults with resulting repetition of beds, whereas the transgressive beds exhibit little deformation (Fig, 2). The gentle folding north of the Amadeus Geosyneline is exhibited both by the Cambrian and Ordovician sediments. The two periols may be separated by an unconformity, but none has been proved as yet. Even if such were established, it probably would disclose discontinuity of deposition without deformation. On present evidence, the folding of the Buldivan Series appears to have taken place in Late- or Post-Ordovician times, both in the Barkly and the Buldiva-Wiso Basins, increasing probably ii severity to the north-east, in the Arnhem Land Region. The general sub- horizontal attitude could result, as the writer believes it did resuli, in the removal by erosion of the Ordovician, and much of the Cambrian sediments It is suggested therefore, that remnants of Ordovician age may exist in the largely unknown terrain to the north-west of Barrow Creek, which the writer named the Wiso Region or Tableland. There may be remnants also of such deposits in the Victoria River Region and even further to the north- west. The great extent of the Buldivan transgression and the transgressive nature of the Ordovician sediments, suggests a former much greater extent of the fatter than that of the scattered dissected remnants of today. F. SILURIAN No formations of this pertod have been identified in the Northern Territory, The possibility exists that such may be found among the sedi- ments of the unmapped Wiso Region, or im the terrain still further to the north-west towards the East Kimberley Region. In the Western Macdunnell Ranges a remarkable conglomerate overlaps the Ordovician Larapintine Series without an angular unconformity, Macli- gan (1932a) named this conglomerate the Pertnjara Series, and estimated a minimum thickness of 9,000 feet. As far as is known at present, this forma- tian referred to elsewhere as the Post-Ordavician conglomerate, ts restricted to the western segment of the Amadeus Geosyncline where much of it is obscured by Cainozoic sands and gravels. Near the base, the boulders include fossiliferous Larapintine rocks, Pertaknurra limestones and Archaeozoic rocks up to three feet in diameter, Higher up in the sequence the percentage of boulders derived from Archaev- zoic rocks increases. Although examined [for such features, no evidence of facetting or glacial striation was discovered, and it appears that the con- glomerate was formed of water-worn material. No contemporaneous fossils were observed in the conglomerate, the only fossils recorded being those derived from older sediments. No definite évidence is available of the age of the Pertnjara conglomerate. Madigan (19324) suggests its correlation with the Finke River Series, good exposures of which exist between Horseshoe Bend and Yellow Cliff along the Finke River, and regards the conglomerate as of Permo-Carboniferous (Permian) age. This tentative correlation by Madigan must be rejected since the Finke Series are not folded and rest tinconformably on the eroded surfaces of the folded Amadeus geosyncline sediments. The absence of an angular unconformity suggests continuity of deposi- tiun in the Amadeus Basin after the Ordovician Larapintine Series. Wherever examined by the writer, the Pertnjara Series participated in the oregeny of the Amadeus Geosyncline and exhibits severe ditatrophistn, closed folds und reversed dips in some areas. There appears to be no reason at present to postulate a long time interval such as the currelation by Madigan would 145 require between the deposition of the Larapintine and the Pertnjara Series. Local uplift of part of the western portion of the Arunta Block and a part. of the geosynclinal basin, could have produced the features described by Madigan. The present writer agrees therefore with the tentative correlation by Andrews (1937) of the Pertnjara Conglomerate with the Silurian. G DEVONIAN The only area in which rocks of definite Devonian age have been recognized in the Northern Territory is the continuation eastwards from the Wesiern Australian border of the Burt Range Basin in the Ord River District, where they have been mapped and described. (Mattheson and Teichert, 1945; Teichert, 1947). The deposits uf this synclinal basin were found to contain Upper Devonian, Carboniferous and Permian (?} sediments. The Devonian succession as determined by Teichcrt is a follows: Upper Sandstones - - ~ - - - ~ 14,000 feet Limestones with interbedded shales and Caleareous Sandstunes - - - - - 4000 _,, Cockatoo Sandstones and Conglumerates - 4,800 _,, Total 9,800 ,, The Cockatoo Sandstones and Conglomerates rest on basalt which has a thickness ef at least 100 feet, and lies unconformably on Precambrian quartzites, The age of the basalt has nat been determined, but Teichert suggests that despite its similarity to the Lower Cambrian basalt of the Argyle Basin, etc., it may well be of Devonian age. The lower sandstones are strongly current-bedded. From fossiliferous horizons in the middle group, Camarotocchia- Productella assemblages were found identical with those of the Productella . limestone (Stage IV) of the West Kimberley District. Teichert considers that deposition commenced early in the Upper Devonian and continued to the close of that epoch. Tue CoLiia SERIES Asa result of the examination by the N.A. Survey in 1936 of the Buldiva- Collia Area, south of the Lower Daly River, a group of lavas and tuffs with some sediments was described and named the Collia Series. A description and map of the area was published (A.G.G.S.N.A., 1937a, and Hossfeld, 19372). (Fig, 3). The basal beds in some places, notably just west of Collia, are quartzites containing beds of arleose. Grits are present also, The arkose appears io have heen derived from the Soldier's Creek Granite which forms large outcrops in this area. The Collia Series consists mainly of lavas and tufs. Gencrally these rest unconformably directly on the sediments and intrusives of the Agicondi Series or on the tilted sediments of the Buldivan Series. The lavas and tufls range from basic to intermediate types, and some of them contain appreciable amounts of copper minerals. Despite the sceplicism expressed by Noakes (1949) and the difference of opinion indicated by Browne (David and Browne, 1950, p. 23) in amend- ing the section in the published report (Hossfeld, 1937g) the opinion ex- pressed in that report by the present writer is being adhered to. This is supported by Voisey (1939a) who as Assistant Geologist of the N.A. Survey was responsible for a large proportion of the geological mapping of the Buldiya-Collia Area. There is no douwht that the Colfia Series which is horizontal or nearly so, rests unconformably on the eroded, upturned edges of the sediments of the Buldivan Series. It is, therefore, of Post-Cambrian K 146 age, It is overlain by sediments which Were named the Plateau Sandstune Series (Hossfeld, 1937g) and on the evidence of the discovery of Otozamites bengalensis, were regarded as of Jurassic age. Later, the age determination was allered ta Lower Cretaceous, and the formal name changed to Mullaman Group by Noakes (1949). The Cullia Series, therefore, is Post-Cambrian and TPre-Cretuceous, No other evidence of its age was discovered. The report, however, by Teichert (op. cit.) of the existence at the base of the Cockatoo Sandstones of basalt with an observed thickness of 100 feet, which is being regarded as possibly of Devonian age, and perhaps at the base of the Upper Devonian, suggests a possible currelation between the Burt Range drea of Teichert and the Buldiva-Collia area about 150 miles to the north-east. Voleanics have been recorded from many localities in North Australia. Some of these were listed by H. Y. L. Brown, Woolnough and Jensen. As was to be expected in a region of which so little was known, interpreta- ‘tions of the ages and correlation of these deposits varied very widely. A region in which the ancient sediments of the Agicondi Series contain Jarge amounts of tuffs and tuffaceous material and probably lava flows, a region jn which volcanics occur in some localities in the Cambrian sequence, and which experienced Post-Cambrian vulcanism, regional reconnaissance did nut supply in many instances the information necessary for the age deter- inination and correlation of widely scattered outcrops: The evidence accumulated over many decades has shown, however, that there are a very large number of discontinuous outcrops, some widely scattered, occupying both large and small areas, which are volcanics that appear to occupy a stratigraphical position above the knowa Cambrian sediments, Their mode of occurrence varies widely. In many instances they form: the higher sectors of the landscape as in the Willeroo-Victoria River Downs-Wave Hill region, in the Nutwood Downs area and others. Accord- ing to Brown and Jensen in sotrie areas they appear to occupy “erasion hollows” in the Cambrian limestones. There are large ureas where they outcrop along the escarpments only of mesas and tablelands, the scarps being due to the younger “Lower Cretaceous sediments.” Even today when they have been denuded from very large areas, they outcrop and probably occur beneath younger sediments over a large part of North Australia. I is improbable that they were ever continuous over the major part of North Australia, but they covered apparently a very large terrain. Some of the occurrences may be identified eventually with the Cambrian deposits, but many are regarded tentatively as of Post-Cambrian age. The intense volcanic activity in Eastern Australia during the Devonian Period may well have extended to a less degree into North Australia. The classification of the Collia Series and its equivalents in North Australia as Middle to Upper Devonian is a tentative onc, but at present no evidence ts available for an earlier or later time. H. CARBONIFEROUS Recks of this period are known only from the Burt Range Basin where they cross from Western Australia into the Northern Territory. Nothing is known of their further extension eastward, but the total area within which they outcrop is likely to be small, unless other basins are discovered. The Carboniferous sediments of the Burt Range Basin in West- ern Australia have not been examined in detail and at present only 350 feet of Bryozoan limestone is known. As this limestané eaverlics the sandstones believed to be the highest members of the Devonian, and by inference, the Carboniferous sediments are conformable, the latter probably are of Lower Carboniferous age. 147 I. PERMIAN Permian rocks are known from the north-western part of ihe Northern Territory and in other areas some sediments are assigned tentatively to that period. Tue Porr Keats Districr Fossils were found first at Fossil Head, on the northern shore of a creek estuary north of the mouth of the Fitzmaurice River, by Commander Stokes in 1839. The outcrops of this and adjacent areas were examined and described later by H. Y. L. Brown (1906), According to Brown, the Fossil Head outcrop ‘exhibits the most typical section of Permo-Carboniferous beds to be seen along the north-western coast of the Northern Territory.” The beds consist of sandstone, shale and sandrock. Current bedding and ripplemarks were observed in some of the heds, and the fossiliferous portions are lenticular, The lower beds are richly fFossiliferous and the fossils are pseudomorphs of limonite. The beds are practically horizontal with a very low dip to the westward. The area was tested for coal by several bores. One bore penetrated 1,500 feet of sediments, and was presumed to be in Permo-Carboniferous (Permian) beds at that depth. The obesrvation by Brown that some of the beds in the lower part of the sequence were cal- careous or limestones, suggests the possibility of the bore having entered pembtisg beds of the Buldivan Series or the still older beds of the Davenport eries. The fossil assemblage indicates affinity with Permian heds in the Desert and North-west Basins of Western Australia. The Permian beds of the Port Keats District were given the formal name of Port Keats Group by Noakes (1949). The bores did not succeed in proving the existence of workable coal seams, but in view of the penetration in one bore of a little coal, such a discovery is not impossible. The recent work of Mattheson and Teichert (1945) along the Western Australian border towards the Keep River in the vicinity of latitude 16° S., strongly suggests the extension of beds of this age towards. the mouth of the Victoria River. The areas where they may occur have been indicated bv the present writer on the geological map, Much of this region consists of swampy alluvium beneath which the Permian sediments probably continue. The presence in the Victoria River region of rocks believed to belong ta the Collia Series, and also of sediments of the Lower Cretaceous Epoch, and the absence of marked deformation in any Post-Cambrian rocks, will necessitate detailed field and palaeontological work to separate and map the different groups. Tur Burt RANGE BaAsIn Mattheson and Teichert (1945) discovered in this area a sequence separated from the Carboniferous Bryozoan limestone by a very slight un- conformity. The beds consist of conglomerate at the base, succeeded by coarse-grained sandstone and several hundred feet of higher beds which could not be examined on that occasion, They are being regarded tentatively as of Permian age. OrHer Areas tn Nortu AUSTRALIA A. wide-spread group of sediments occurring in North Australia from the virinity of the Western Australian to the Queensland border which hail been named by the writer “The Plateau Sandstone Series,” have been given the formal name of Mullaman Group (Noakes, 1949), They were regarded hy H. ¥, L. Brown (1908) in part at least as Lower Cretaceous. Jensen and 148 others considered them.as probable Permo-Carboniicrous beds, but Brown’s original age classification was confirmed by later palacontological evidence, and they will be discussed therefore, in a later section. The oceurrence in North Australia, within the Proterezvic Kimberley Basin, of very gently inclined sediments of Permian age, the Port Keats Group, suggests that possibility also in the similar Proterazoic basin, the Carpentaria Basin, This suggestion receives some support from the existence in the coastal region of the Gulf of Carpentaria, of horizontal or gently in- clined sediments which differ from the “Lower Cretaceous beds” of the adjacent tablelands. Brown (19084) reports the discovery in a shaft of black carbonaceous shale similar to that obtained from a bore in Permian beds at Port Keats. Jensen (Cwlth, Atst. 1914a, Bull, No, 10) reports fossil wood resembling Calamites and some specimens resembling Lepidodendron. The present writer Suggests therefore, the strong possibility that Permian deposits exist in the coastal region of the Gulf of Carpentaria and continue eastwards into Queensland beneath rocks of Lower Cretaceuus age, THe FInKe SERIES Near the central portion of the southern border of the Northern Territory in approximately Lat. 254 S., terrestrial deposits containing glacial sediments exist in the vicinity of and along the River Finke. They have been described by yarious authors including Brown (1905), David and Howchin (1923), Ward (1925) and Chewings (1935), They outcrop along the slopes of many buttes and mesas, some of the Jattcr of very large dimensions. Their occur- rence ig that of residuals of a former continuous formation, now reduced by dissection and lying unconformably on the folded sediments of the Amadeus Geesyncline, Their outcrops extend probably from the southern flanks of the James Range south to the South Australian border and beyond, They dip gently in a south-easterly direction beneath the Mesozoic sediments of the Great Artesian Basin, and are generally believed to act as intake beds of that basin, The area in which they may occur, has a length from north-west to south-east of about 15 miles. Their knawn lateral extent is very variable, but may be estimated at an average of 50 miles. Continuation much further to the west than is indicated on the accom- panying map is unlikely. The observation, however. of the gradual merging eastwards of these mesas with the sands of the Simpson Desert, indicates that the Finke Series may continue to the east much further than is generally believed. The lower members consist of glacial tills and sands with thin lenticular beds of conglomerate and argillaceous sandstone, a total thickness of at least 100 feet. and are overlain by at least 2,000 feet of porous sandstones. The terrestrial glacial origin of the lower beds is undoubted, but in the absence of fossil evidence there exist differences of opinion as to their age. Browne (David and Browne, 1950) considers them to be Carboniferous or Permian, Talbot and Clarke (1917) considered a possible correlation with the Wilkin- son Range Series of Western Australia and of the supposed Lower Cretace- ous glaciation of Northern South Australia, However, it is generally believed that they are of Palaeozoic age, and tu be carretated, even though tentatively, with glacial depositis of Lower Permian age in Southern Australia. THE Evuiotr Creek Formation In the Elliott Creek area, north of the Daly River, Noakes (1949) mapped sediments to which he gave the above formal name. The beds con- sist of thin beds of sandstones, shale and limestone, which lie horizontally 149 in most of the few available outcrops examined, No fossils were found, and a minimum thickness of 500 feet is suggested. On general grounds these heds are regarded as of late Palaeozaic age, J. TRIASSIC No rocks of this period have been recognized in the Northern Territory: Browne (David and Browne, 1950) suggests that the porous sandstones which aggregate the total of at least 2,000 feet above the glacial beds of the Finke Series may be Triassic (?) and Jurassic. In several localities to the west of the railway line, especially in the area west of Charlotte Waters, a number of buttes and small mesas consist of horizontal or nearly horizontal sediments lying on the Finke Series. They are almost certainly Mesozoic and may perhaps be regarded, in part at least, as of Triassic age, with possibly Jurassic beds above. K. JURASSIC Outcrops of Jurassic Age have not been recognized definitely anywhere within the Northern Territory. Their existence, however, is known in the south-western sector, as aquifers of the Great Artesian Basin. Outecrops of Jurassic rocks of the Great Artesian Basin are known lo the south of the Territory border in South Australia, but haye not been identified with certainty to the north of that border. Sands‘ overlying the glacial beds of the Finke Series at Yellow Cliff may be Jurassic in part, and some of the sandy beds to the west of Charlotte Water may be of that age. The existence of Jurassic sediments has been proved at depth by water- bores deilled in the Artesian basin. j The greatest thickness recorded from a water-bore which, however, did fot penetrate the complete sequence, is 860 feet (Ward.1925). The sands are of lacustrine origin and contain lignitic material. The total thickness in the Territory sector of the basin is not known, but on the evidence of the few bores, chiefly near the margin of the basin, appears to be somewhat variable as would be expected of marginal deposits. Although surface outcrops have not been recognized, the available evidence suggests that the limits of the Jurassic sediments, at or near the surface are marked approximately by the north-western margins of the extensive aeolian sands and sand-dunes of the Simpson Desert (Madigan, 1938) which may, however, cover also large expanses of the Finke Series. On Paddy’s Hole Plain, south of Arltunga in the Eastern Macdonnell Ranges, the silicified stems of osmundaceous plants have been recorded as weathered out from isolated flat-topped hills (Madigan, 1933, 1937). These are regarded generally as belonging to the Mesozoic Era, and may belong to, or he derived from Jurassic or Cretaceous outliers of the Artesian Basin. IL, CRETACEOUS The existence of marine sediments of Mesozoic age at Point Charles near Darwin, was recorded as early as 1895 and further work was done in that and adjacent paris of the coast in subsequent years. (Brown, 1895 and 1906). The occurrence of rocks of similar age was recorded also from the southern parts of Bathurst and Melville Islands north of Darwin, To these sediments, Noakes (1949) has given the name Darwin Formation, At some distance inland, sediments forming mesas and bultes and very extensive tablelands occur at intervals over a large portion of North Aus- tralia, They have been recognized as far south at Lat, 18 5., and extend 150 almost from the Western Australian border across the Northern Territory to the Queensland border. These sediments were referred to in the past by various writers as the Plateau Sandstones and were assigned a Permo- Carboniferous age (Jensen and Woolnough) and a Lower Cretaceous age (Brown), They were given the formal name of Plateau Sandstone Series (Hossfeld, 1937), This name has been changed to Mallaman Group by Noakes (op, cit.) who included in it the Point Charles beds and related sediments of the coastal region (Darwin Formation), The terms and correla- tion adopted by Noakes are used in the present paper for the sake of con- venience, but such use does not imply compicte acceptance of his conclusions. Far too little work has been done on the group, and the few localities from which fossiis have been collected are too widely spaced for the formation of general conclusions of what is admittedly a difficult group. The maxtmum recorded thickness of this group appears to be about 200 feet, but a total of 100 feet is probably nearer the average. The proun appears to vary considerably in thickness, and within short distances in some localities; in others it appears to be very uniform. Much of this varia- tion in thickness appears ta have been due to deposition on a slightly irregular landscape. That the land surface on which the group was deposited was one of predominantly low relicf is unquestionable. However, that some rejief existed in restricted areas at feast is shown by various features which will be referred to in the discussion which follows. The sediments of the group were examined in detail in the Buldiva-Collia area and extracts from the report on that area (Hossfeld, 1937g) are quoted herewith: “In the Buldiva-Collia area the Plateau Sandstone Series consists of sedimentary rocks lying almost horizontally on an uneven surface af the older rocks. Erosion has exposed the older rocks in many places, the Plateau Sandstones standing above the getieral level as mesas and buttes in the intérvening area. The characteristic topography of the mesas and buttes is due ta the horizontal bedding and vertical jointing of the sandstones. The level surfaces of the mesas and buttes may indicate a former continuous peneplain, The basal beds of the Plateau Sandstone Series vary considerably in texture, composition and thickness according to the nature of the underlying rock and the former surface relief heneath and adjacent to the area. of deposition.” “The plant remains referred to above, and on the evidence of which a Jurassic age is assigned to the Plateau Sandstone Series, were collected in a fine-grained white sandstone or siltstone immediately overlying the tin- bearing conglomerate, These white sandstones and siltstones have been transformed in places to porcelianites and ribbon stones. They form a per- sistent horizon and supply good marker beds, The underlying beds cannot be used for this purpose as they vary in thickness, owing to the irregular surface on which they were deposited, and in composition which is dependent on that of the underlying rocks.” At Buldiva, plant remains were collected by the N.A. Survey and identi- fied as Otozamites bengalensis by Dr. A. B. Walkom, who suggested a Jurassic age for the sediments. The determination of radiolaria from the Darwin Formation and the examination of the macro-fossils collected, has resulted in the classification of that Formation as probably of Albian age, Since, according tc Noakes (op. cit.) the Darwin Formation overlies con- formably the other members of the Mullaman Group and in which the’plant remains were found, the age of the latter suggested by him is Lower Cretace- ous and not Jurassic, Duting 1938 and again in 1939, marine fossils were 181 collected by A. W. Kleeman and the writer in the Mullaman Group from Yeuraiba, a locality within the Arnhem Land Region. The fossils were too pnorly preserved for delermination. It is possible that future investigations will support the division by Noakes of the Mullaman Group into a lower, lacustrine facies and an upper marine facies. Within the present writer's knowledge, hawever, plant remains have been collected from only three pr four localities and from horizons which cannot be correlated stratigraphically. Marine fossils have been recognized at a few places only. Obviously no such generalizations as are put forward by Noakes can be supported on a few isolated occurrences over such a wide area. The examination of the sequence in the Buldiva-Collia area, at Yeuralba, Pine Creek and south of Birdum by the present writer suggests that the whole of the group may well be of marine origin, and that sma!l estuarine and fluviatile deposits were responsible for the few remains of Otezamites, the only plant identified from these beds. Because of overlap, terrestrial deposits. and a few durable plant remains would be preserved near the base of the group, but in successively younger beds. Conditions at Buldiva where high level cassiterite-bearing gravels occur near, but fot at the base of the sequence, indicate fluviatile deposits, possibly resorted by wave action. The plant remains were discovered just ahove this horizon, It is suggested here that the group was deposited as a result of a gradually transgressive epeiric sea which finally extended over the whole of North Australia at least as far south at lat. 18. S. Deposition probably commenced in late Jurassic times and continued inta the Lower Cretaceous. It was continuous apparently with the Lower Cretaceous sea of Queensland and the adjoining States, in the region which was to become the Great Australian Artesian Basin. Emergence of North Australia from the Lower Cretaceous sea probably by negative moverient of sea-level, left the sedi- ments in a horizontal to sub-horizontal position, in which they are today over very large areas. The region therewpon became a plain, old at birth and without experiencing the very long continuous erosion which was necessary ta produce the peneplanation of diverse rock types and structures over the greater part of Australia during the Mesozoic Era. The region formed then a part of the Great Australian Peneplain, The porosity of the sediments ensured the absorption of the greater portion of the rainfall then as it does today, and the gradua) loss by evaporation of the greater part during the long dry seasons, The porosity of the sediments is shown by the existence of the exceedingly numerous springs which issue from the beds of the group wherever they and the basement rocks have been exposed by dissection. . One very marked feature observed concerns the vegetation developed on the sedimeuts of the Plateau Sandstones, It js sbvious that the poor and very porous soil and sediments would develop a flora specially adapted to such an environment. It is rematkable, however, that over a very large proportion of the region the only tree which will grow on these rocks is Lancewood. This occurs as @ thick forest cover and in pure plant communi- ties. There are many areas it is true, where the existence of the Mullaman Group is regarded as certain beneath the surface soil, but where Lancewood does not exist, These are areas where for various reasons soi] cover is ton deep or unsuitable for the growth of Lancewood, No areas were observed, however, where Lancewood does exist, which could not with reastnable certainty be regarded as underlain by the Mullaman Group, The above remarks apply to the region south of approximately the laticude of Maranboy. 132 Further north, the average rainfall apparently is too high for the ascetic Lancewood, To the north of Maranboy and other areas of similar rainfall, Lancewood is still associated with these beds but instead of growing on the level summits of the mesas and tablelands as it does further south in the drier region, it grows only on the scree slopes beneath the sandstone escarp- ments. The observation and confirmation of this predilection of Lancewood for the sediments of the Plateau Sandstones facilitated greatly the ground and aerial reconnaissance of the region. The dark foliage and general density of the forest cover, made it easy to recognize the timber at great distances and enabled the writer to map many areas of these sediments. It was possible to confirm by actual inspection so many of these occurrences, that no doubt remains of its general applicability. Tse Great AUSTRALIAN ARTESIAN BASIN Lower Cretaceous sediments of marine origin underlie the extreme south-eastern corner of the Territory, Outcrops have been examined and described from the vicinity of Charlotte Waters and aa far north as Mount Daniel. Owing to the prevalence of recent aeolian sands, little is known of the greater part of the boundaries of the basin in this region. The sediments consist predominantly of dense, blue shales with some thin calcareous bands, and are fossiliferous in some localities. They have been studied, largely from bore samples, in the adjacent areas of South Australia and Queensland, and have been assigned to the Tambo Series, They are believed to underlic the region known as the Simpson Desert. Tt is possible that Paddy’s Hole Plain, south of Arltunga, may be under- lain, in part at least, by Cretaceous sediments, forming a northern outlier of the Great Basin. Lying above the Lower Cretaceous sediments of the basin, there are dissected remnants of sediments correlated with the Winton Series, of Upper Cretaceous age. These form mesas and buttes and consist of horizontal beds, capped by duricrust, and indicate the stage to which dissection has reduced the level of the former peneplain. Tue Burt Trouce The continuity of the surface outcrops of the Archaeozoic rocks of the Arunta Complex is interrupted by a number of plains, covered by recent soils and sands, The largest of these is the Burt Plain (Birt Plain of Jensen, 1944). (Pls. IIT, 2 and TV, 1), The severe topography exhibited by the Archae- ozoic rocks north of Alice Springs terminates. abruptly at about 12 miles at the southern margin of the Burt Plain, which in this sector has a north-south width of about 50 miles. It terminates a few miles tu the east, but extends westwards for at least 200 miles. Its furthest western limits have not beetr efined, Ground teconnaissance, and observations from the air by the writer. for a distance of about 100 miles along the northern and southern margins of the plain, as well as the study of aerial photographs, indicate that the Sh akees part and perhaps the whole of the Burt Plain is bordered by faults, (PI. ITT, 2.) The examination of samples from the 16 mile bore (Hossfeld, 1933}, showed that in this locality, which is close to the southern margin of the plain there exists a considerable thickness of sediments, which are immensely younger than the Archaeozojc rocks which form the northern, eastern and southern boundaries of the plain, E53 s0[q eAEIASNH IW saag Buy Najduioy eWunsy jo suonEWLOY pio (sae japlo) | SassiaUy, jee Sa}UeIC) Japjo) Sassiaug, aiitescy si Sa el aan aie a note = TR SI rc adioar xajduioy eyuNIy jO SuoNeuLoy JoMaN wom mee a = = Snag Ipuoosy Salag Ipuollsy so" " saduey uueusajeq > por SS TTT gauiag oduaarg dUEIN) psielaag stiles ELINIDEI | $31499 BYeIEIg Sa}lag e}1008}19q lenquiey S WEALD NG Saplag ouuideiey URDIAOPIO £ Sofleg eielnjiog =F. | tWeldinyi | na: | Pjoojoa10g (i) im d ura ‘useg a3ury jing ‘dios By PA Omula (e) —— eS Sr fal as tal liad Sali ar JaMO7] ,S849G auojspueg near, UISEG UeIsayIy 3eo1ry snoasezaiy ‘spag, Ssajizy julog pue dnoig uewriny cc) wT a pms ae ee HO] eBunsy yorgq eyunsy jo sziwy yO wos ‘eypessny jesuasy powag pue esa } WAIYIINOS OF BYeIYSNY [CAIWID ‘eyesjsHy YON ‘ | f10WAIIT, UTeyjJoNY ayy Jo Adojouosyy [eosojoay I] 31av 154 The total thickness of the sediments penctrated by the bore is 639 feet with a small possible extension, The sediments consist predominantly of shale with some beds of grit, The shales vary from gritty types to very fine material, They include black carbonaceous shales al several horizons but especially between 515 and 569 feet. Below GI7 feet the sediments contain large amounts of mica and below 639 the samples consists of fragments of mica schist indicating either thal Archaeozoic bedrock had been reached, or that this was not far below. No fossils were obtained from the bore samples, but the materials from 322 to 639 feet indicate a lacustrine origin and suggest affinities with the Winton Series. The thickness penetrated and the nature of the sediments suggest the strong probability of considerable fateral extent of this formation. The probability that there exists here a sub-artesian basin of considerable area, is increased by the amount of water under pressure which has been shown to exist in the more porous beds. The existence of carbonaceous shales indicates the possibility of the discovery of economically important coal deposits. Little is known of the attitude of the beds, which on general evidence appear to be sub-horizontal and inclined ta the westwards. Indications are that some at least of the sediments will prove to be lentictilar in shape. The discovery of, or failure to discover coal in any one locality must not be regarded, therefore, as typical of the whole of the Burt Plain. Water supplies also may be found to occur at various. depths in different bores, and at more than one horizon in one bore. It is an area which in its water contents and potential coal deposits, deserves systematic sub-surface exploration. , The potability of the water from the 16-mile Bore may be ascribed possibly to the existence of a western outlet. Ata distance of about 70 miles to the west of the eastern margin of the Burt Plain, there commences a series of salt lakes and swamps which continue in a narrow belt for more than q hundred miles further west. (Plate TV, 1.) Aerial examitation of these shallow depressions indicates that many are fed by springs issuing from their higher marginal areas. The writer believes that this zone of salt lakes and swamps which occupy an area of considerably lower altitude than that further east, is supplied to a large extent by water discharged from the basin underlying the Burt Plain and that it is this discharge which has permitted the existence of potable water in the basin, The gradual but con- sistent decrease in altitude of the surface of the Burt Plain from east to west, estimated at an ayerage fall of 35 inches per mile, is believed to represent fairly closely the inclination of the underlying sediments, That being so, it follows that there would be a slow, but constant movement of subterrancan water in that direction. It is true that the run off from the ridges of older rocks, which form the northern and seuthern margins of the plain will supply some water to the belt of lakes and swamps, but this is considered to be a minor contribution, The most suitable name for the structural feature, the filling of which has produced the Burt Plain, is the Burt Trough. The existence, on the border of Western Australia, in the extreme north-west of North Australia, of the Burt Range, resulted in the structural name of Burt Range Basin given to the sediments of that area (Mattheson and Teichert, 1945). How- ever, in view-of the occurrence of the Burt Trough in Central Australia, the tame proposed should not be confusing. Should it be so regarded, the 135 alternative name “Stuart Trough” is being suggested for obvious historical and geographical reasons. Two similar basins, the Plenty atid the Hale Plains, appear to be connected structurally with the Burt Plain. Both exhibit faulted boundaries, in part at least, and appear to be continuations of the fracture system responsible for the Burt Trough. No evidence is available to the writer of the material underlying the Vlenty Plain, which is believed, however, to be merely an extension of the Burt Plain and to have had a similar histery. (Fig. 2). The occurrence on the Hale and Plenty Plains, and elsewhere in Central Australia, of lacustrine sediments of Tertiary age, the Arltunga Series (Madi- gan, 1933), indicates that the underlying sediments were at least of older Tertiary and probably of Mesozotc age. . The penetration by a bore of a seam of lignite 12 fect thick in the Hale Trough, suggests that the sediments of that basin are of Tertiary age and depésits of Cretaceous age may occur. The osmundaceous plant remains fram the nearby Paddy's Hale Plain recorded by Madigan (1932b) suggest such a possibility. Other basins probably exist in Central Australia, and the Bundey, Sandover and Hanson Rivers are suggested as possibilities. No evidence is available and the writer does not contend, that the Burt, Plenty and Hale Troughs referred to and others which may be discovered were completely co-épochal in their formation. It is believed, however, that the basins ate not older than Upper Mesozoic. The subsidiary basins of the Plenty and Hale Plains are being drained, though imperfectly, by the rivers of the same names. The Burt Plain itself, however, despite its relatively high altitude, stated to approximate 2400 feet near its eastern limits, is still a basin of internal drainage which has been protected from dissection by the higher ridges of ancient rocks forming its borders, The reference by Jensen (1944), to this plain as the “Birt Plain pene- plain” is cpposed to the geological and topographical evidence. King (1950) has linked, the Burt Plain and the Missionary Plain with the “Australian” pediplam. The Missionary Plain may be such a continuation, as may the extensive peneplaned areas north and north-west of the Arunta Block, The Burt Plain, however, represents the filling by sediments of a high-level lake and its formation was considerably above the pediplain and had no con- nection with its formation. M. CAINOZOIC Detailed studies of the Cainozoic deposits uf the Northern Territory have been published for a few small areas only. The deposits are pre- dominantly of terrestrial origin and age determinations will be difficult to establish. Division into Tertiary and Quaternary Periods is impossible at present in many instances. No marine deposits of ‘Tertiary age +have been recorded from the Territory, Such deposits, however, may underlie some of the extensive coastal plains of the north and west, but if such exist, they would belong, probably, to Upper Tertiary Times. Pleistocene to Recent marine deposits have beer observed on the north and west coast (Noakes, 1949). They appear to he connected chiefly with world-wide eustatic strandline movements due to glaciations and de- gilaciations. Deposits of lacustrine and fluviatile origin exist in mary areas and indicate extensive lake development during one or more pluvial periods, 156 Deeply eroded stream channels now filled with alluvitim and aeolian deposits are another indication of former greater rainfall. Other climatic changes are indicated by the extensive development af evenly spaced sand dunes, enormous areas of sand plain and large tracts covered with loessia] material. The present fixation by vegetation of these aeolian deposits indicates subsequent changes as do the occurrences of various plant communities, separated from each other by long distances, The description, discussion, development of the terrestrial deposits of the Northern Territory and the information which they supply of diastro- phism and climatic changes are being reserved for a subsequent paper. Ill, REFERENCES AND BIBLIOGRAPHY Published by arrangement with the Author —Ep. The following list is not exhaustiye and is restricted to those publications to which ireet refererice is made in the text and to those which were used for general reference. .S.N.A, 1936a Aer. Geol, and Geophys. Sury. N. 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Busses, [E 1927 Geology af Portions of the Kimberley District. Geol. Surv. W. Aust. ull. 93 Brown, H, ¥_L. 1889 Government Geologist’s Report on a Journey from Adelaide to Hale River. S. Aust. Par}. Pap., No. 24 Brown, H, ¥. L. 1890a Report on Journey from Warrina to Musgrave Ranges. S. Aust: Parl, Pap. No. 45 Brown, H. ¥. L. 1890b Report of Geological Examimation of Country in the Neighbour- hood of Alice Springs. S. Aust, Parl, Pap,, No. 18 Brown, H, ¥. L. 1895 Government Geologist's Report on Explorations in the Nerthern Territory. S, Aust. Parl, Pap., No. & Brown, H. Y, L, 1896 Reports on Arliunga Goldfield, ete, S, Aust: Parl. Pap. No. 127 Brown, H. Y. L. 1902 Report on the White Range Goldmines, Arltunga Goldfield. S. Aust, Parl, Pap., No. 76 Brown, H, Y. L. 1903a Northern Territory of South Australia; Report on Cotintry fe- cently examined im the Davenport and Murchison Ranges, etc. S, Aust. Parl, Pan., ‘ uw Brown, H. Y. L. 1903b Northern Territory of South Australia: Report on the Gold Dis- coveties near Winnecke’s Depot, etc. S. Aust. Parl. Pap., No, 59 Brown, H. ¥. L. 1905 Report on Geological Explorations in the West atid North-west of South Australia, ete. S. Aust. Parl. Pap., No. 71 Baown, H. Y. L. Basenow, H., and Gee, L. C. E. 1906 Northern Territory of South Australia, North-western District, etc. S. Aust, Parl, Pap., No. 55 Brown, H, Y. EL. 1907 Record of Boring Operations in the Northern Territory, ete. S. Aust. Parl, Pap. No. 54 Brown, H. Y. L. 1908a Northern Territory of South Australia: North and Eastern Coasts. S. Aust. Parl. Pap, No, 25 157 Brown, H, Y. L. 1908p Norther Territory o£ South Australia; Government Geologist's Report on Recent Mineral Discoveries, etc. S. Aust. Parl, Pap., No, 85 Buown, H. ¥. L, 1909 Government Geologist's Report om the Tamatni Gold Country. & Aust. Parl. Pap, No. 105 Bryan, W. H. and Jonus, 0. A. 1945 The Geological History of Queensland, Unty, Qld, Dept. Geol. Papers, 2, (12) Camegzon, W, E, 1900a Post-Tertiary Limestones of the Barkly Tableland, Ain, Prog. Rept. Geol, Survy,, Qld, for 1900 ; Cameron, W. E, 1900b Geological Observations in North-western Queensland. Jhtd Uaewines, Goa The Sources of the Finke River. Reprinted from the Adel Observer, elaide Crewincs, C 1891 Geological Notes on the Upper Finke Basin, Trans, Roy. Soc, S. Aust, 14 Cuewines, C, 1894 Notes ot the Sedimentary Rocks in the Macdonnell and Jame: Ranges. Trans, Roy, Soc, S, Aust. 18 air C, 1914 Notes on the Stratigraphy of Central Australia. Trans. Roy. Soc. Anst, 38 Cuewrnes, C. 1928 Further Notes on the Stratigraphy of Central Australia. Trans. Roy. Soc S. Aust, 52 Cuewinos, C.. 1931 A Delineation of the Precambrian Plateau in Central and North Aus- tralia, ete. Trans, Roy. Soc. S. Aust., 55 Caewinos, C. 1935 The Pertatataka Series in Central Australia, with Notes on the Amadeus Sunkland. Trans. Roy Soc. S Aust, 59 CoMMONWEALTH OF AUSTRALIA: Bulletins of the Northern Territory 19124 Report of Pre- liminary Scientific Expedition Dept. Ext, Affairs, Bull. No. 1 COMMONWEALTH OF AUSTRAIIA: Bulletins of the Northern Territory 1912b Report of the raed Bay Prospecting Party (May-September 1911). Dept. Ext. Affairs, Bull, 0 3 CoMMONWEALTH OF AusIRALIA: Bulletins of the Northern Territory 1912c Report on the Geology of the Northern Territory by W. G. Woolnough, Dept. Ext. Aff. Bull, No. 4 CoMMONWEALTH OF AUSTRALIA; Bulletins of the Northern Territory 19144 Geolowical Re- port on the Darwin Mining District, McArthur River District and the Barkly Table- land, by H. I. Jensen, Dept. Ext, Aff, Bull. No. 10 COMMONWEALTH OF AUSTRALIA: Bulletins of the Northern Territory 1914h Progress Re- Report on the Geological Survey of the Pine Creek District, hy H. I. Jensen and T. G. Oliver, Dept, of Ext. Aff. Bull, No. 104 COMMONWEALTH OF AUSTRALIA: Bulletins of the Northern Territory 1915a Report om the Maranbpy Tinfield by G. J, Gray and H. I. Jensen, Dept. Ext. Aff. Bull. No. 11 ComMMONWEALTH OF AUSTRALIA: Bulletins of the Northern Territary 1915b Report on Dia- mond Drilling in the Northern Territory, by H. T. Jensen, Dept. Ext, AM Bull No. 12 COMMONWEALTH OF AUsrrALIA; Bulletins of the Northern Territory 1915¢ Report on Country between Pine Creelc and Tanami. Reconnitissance of Arnhem Land, etc, by H, 1. Jensen, G. J. Gray and R. J. Winters, Dept. Ext. Aff. Bull, No, 14 ComMONWEALTH OF AUSTRALIA! Bulletins of the Northern Territory 19162 Report on Yen- berric Wolfram avd Molybdenite Field, by G. J. Gray and R. J. Winters, Dent. Ext Aff, Bull. No. 154 Commonweattm or Austrarta: Bulletins of the Northern Territory 1916b "The Geology of the Woggaman Province by II, 1. Jensen, G. J. Gray and R. J. Winters, Dept. Ext. Aff. Bull. No. 16 ComMonweaLty or Austratta: Bulletins of the Northern Territory 1916c¢ Report and Plans of Explorations in Central Australia, by T. E. Day, Dept. Home and Terr. Bull. No. 20 COMMONWEALTH OF AUSTRALIA: Bulletins of the Northern Territory 1916d Report of In- spertion on Hatches Creek Wolfram Mines, by T, G, Oliver, Dept. Home and Terr, Bull. No. 21 Cow MONWEALTR OF AUSTRALIA: Bulletins of the Northern Territory 1919 Report on the Agicondi Province by H. I. Tensen, Dept. Horne and Terr. Bull, No. 19 CoMMONWEALTH OF AustRaLIA-: Rulletins of the Northern) Tettitory 1936 Report on Tetr- nant Creek Goldfield, by W. G. Woolnough, Dept. of Interior, Bull No. 22 Crarke, FE, or C, 1930 The Precambrian Succession in some parts of Western Australia. Rept. Aust. Ass. Adv. Sc. 26 : Corie, V. M. 1936 Geological Notes on the Britasinia and Zapopan Areas, A.G,G.S.N.A4, Rept. N, Terr No. 15 Corre, V. M, 1937a Geological Report on the Yam Creek Area. A.G.G-S.N.A. Report N. Terr No. 10 i158 Cortia, V, M, 1937b The Maude Creek Mining Centre, Pine Creek District AGGS.N.A, Rept. N. ‘Terr, No. 27 Cortre, V. i. 193%e (seological Report on the Fountain Head Area AG,GS,N.A, Rept. N. Tetr, No. COrTLeE, Me M. 1937d The Mount Todd Auriferous Area. A.G.G.S,N.A. Rept. N. Terr, 5 o. Danes, J. V. (911 Physiography of some Limestone Areas in Queensland. Proc, Roy, Soc. Qld, 23, pt. i Dai, T. W, E, 1932 Explanatory Notes to accompany a new Geological Map of the Commonwealth of Australia, (Arnold: London) Davin, T. W. E., and Browne, W. R. 1950 The Geology of the Comtnonwealth of Aus- tralia, 3 vols, (Arnold; London) Dav, Sia E., and Howcnim, W. 1923 Reports of Glacial Research Committee: AAAS. Wellington, 16 Davinsow, A. A. 1905 Journal of Explorations in Central Australia, etc., 1898-1900. 5, Aust. Parl. Pap. No. 27 Duxstax. B, 1920 North-western Queensland. Qld. Geol. Surv, Publication No. 265 Enwanps, AG. 1938 Tertiary Tholeiite Magma in West Australia. Journ. Roy, Sor. . Aust, 24 Enwaros, A. B. 1942 Some Basults from the North Kimberley, West Australia, Journ. Roy. See. W, Aust., 27 Ens, H. A. 1927 Report on the Tanami Goldmine, Tanami Golilfield, N.T. Euuis, H. A. 1936 Report on some Observations made on a Journey from Alice Springs, N-T., to the Country North of the Rawlinson Ranges in West Australia, : ete. Ann. Prog. Rept. Geol. Surv. W. Aust. Ezzerwor, R., June. Numerous Papers on Palaeontology forming the whole or parts of the following S. Aust. Parl. Papers: 1895, No. 82; 1896, No, 127; 1905, No. 71; 1906, No. 55; 1907, Supplement to No. 55 of 1906 BROCAT Bi J. se The Nullagine Conglomerates, Pilbara Goldfield. A.G.G.S.N.A, Rept . st. OL Fiuease, K, J. 19382 The Braeside T.ead Field, Pilbara District, Idem. No. 24 Finucane, K, J. 1938b The Hall’s Creek-—Ruby Creek Arca, Mast Kimberley District. Idem, No. 27 Frxucane, K. J. 1939 The Grant's Creck Gold Mining Centre, East Kimberley District. Tdem. No, 40 Gee, L. c E. 1911 General Report on Tanami Goldfield and District. S. Aust. Parl, Pap. o. 31 Grorcr, F, R.; and Murray, W. R.. 1907 Journal of the Government Prospecting Expedition to the South-western Portions of the Northern Territory by F. R, George, and to the Buxton and Davenport Ranges, by W, R. Murray. S Aust. Parl, Pap, No, 50 Gres, Ervesr 1876 E. Giles’s Explorations, 1875-6 S. Aust. Parl, Pap, No. 18 RSCARSEN M. FB. ef of 1948 Stratigraphical Nomenclature in Australia, Aust. Journ. c. xi, 1 Gossz, W. C. 1874 Reports and Diary of Mr. W. C. Gosse’s Facpedition in 1873. 5, Aust, Parl. Pap, No. 48 Harpman, E, T. 1885 Second Report on the Geology of the Kimberley District, W, Aust. Parl. Pap. No, 34 Hints, E. S. 1946 Some Aspects of the Tectonics of Australia, Clarke Mem. Lect. Journ and Prac, Roy. Soc. N.S.W., 79 Hnas, FE. S. 147 The Metalliferous Geochemical Zones of Australia. Econ, Geol, 42 Honce-Smiru, T. 1932 Geological and Mineralogical Observations in Central Australi: Rec. Aust, Mus, 18 Hoxman, C. S. 1936a The Mt, Freda-Canteen Area, Soldiets Cap, Cloncurry District. AG.G.S.N.A. Rept, Qld, No. 1 Honan, C. S. 1936b The Gilded Rose Area, Cloncurry District. Idem. No. 2 Hewmax, C. S. 1937 The Soldiers Cap Area, Cloncurry District. Idem, No, 18 Tionman, C. S$, 1938 The Mount Elliott-Harepden Area, Cloncurry District. Idem. No. 22 Hossrern, P. S. 1931 Report on the Jervois Range Mineral Field, Home Affairs Dept. On official files, not published. Hossrecp, P. S, 1933a Report on Samples fram 16 Mile Creek Bore, Northern Territory. Home Affairs Dept.. On official files, not published Tinssreco, P. S. 1933b Sutnmary Report of the Geology of the Northern Territory. Hame Affairs Dept. On official files, not published j Hossrexn, P, 5, 1934 Report on Samples from No. 1 Bore, Alexandria, Northern Terri- tory. Home Affairs Dept, On official files, not published Hossrecn, F, S$, 1935a The Geology of part of the Northern Mount Lofty Ranges, Trans, Roy. Soc. S$. Aust., 59 159 Hossretp, P. 5. 1935b Report on Mica in Central Australia. Prime Minister's Dept, On official files, not published Hossrexp, P. S. 1937a Report of the Lake Mackay Relief Expedition. Prime Minister's Dept. On official files, not published. Hossrextp, P. §. 1942 Interim Report on the Cosmopolitin Hawley Gold Mine, Bracks Creek Hossein, P. S. 1936a The Golden Dyke Mine and adjacent Areas. A-G/G,S.NLA, Rept. N. Terr. No. 3 Hossrevp, P. §. 1936b The Pine Creek Goldfield. Idem, No. I HossFety, P. S. 1936¢ The Union Reefs Goldtield, Idem, No, 2 Hossrezo, P. me 1936d The Ciccone Mine, Winnecke Goldfield, Eastem Maedonnell Ranges, lem, No, 22 Hossreip, P. §. 1937b The Fletcher’s Gully Area, Daly River District, Idem, No. 17 Hossretp, P. §, 1937¢ The Daly River Copper and Silyer-Lead Area, Daly River District, S. S. Idem. No. 19 HossFexp, P. 1937d The Evelyn Silver-Lead Mine, Pine Creek District. Idem, No. 26 Hoss¢ep, P. 1937e Quartz Body at Simpson's Gap, Alice Springs. Idem. No. 21 Hoss¥exp, P. S, 1937 The Iron-Blow Area, Pine Creek District. Idem. No. 14 Hosssep, P. S. 19372 The Tin Deposits of the Bukdiva-Collia Area, Daly River District. Idem. No. 18 Hossreto, P. S, 1937h The Glankroil Mine, Winnecke Goldfield, Eastern Macdonnell Ranges District. Idem. No. 39 Hossrenp, P. §. 19371 The Home of Bullion Mine, Central Australia. dem. No. 29 yogis > P. ee 1937} The White Range Goldfield, Eastern Macdormell Ranges District. Idem. No. 28 Hossreip, P. §. 1937k The he Portion of the Arltunga Arca, Eastern Macdonnell Ranges District. Idem, No. 20 Hossretp, P, S. 19382 The Wallaby Silver-Lead Lode, Daly River District, Idem, No. 32 Hpsorniat F Bi ae Preliminary Report on The Granites Goldfield, Central Australia, Idem. No Hossretp, P, §. 1939 ‘The Mineral Deposits of the Yeuralla Area, near Katherine, Idem, No. 44 (not published). Hossrezp, P. S. ae Gold Deposits of the Granites-Tanami District, Central Australia. demi Hoare, P. S. 1940b The Winnecke Goldfield, Eastern Macdornell Ranges District. Idem. o. 40 Hossrexvp, P. S. 1940c ‘The McKinley Gold Mine, Pine Creek District. Idem. No. 46 Hossrecp, P. S, 19414 The Drifheld Area, Pine Creek District. Idem, No. 38 Hoss¥ern, sat S, 1941b Limestone Deposits near Alice Springs, Central Australia. Idem. Jacx, RB. Lickwaity 1915 The Geology and Prospects. of the Region to the South of the Musgrave Ranges, etc. Geol, Surv. S. Aust. Bull, No, 5 jJacs, R. Lockuart 1923 The Composition of the Waters of the Great Australian Artesian Basin in South Australia. and its Sigtificance. Trans: Roy. ‘Soc. S, Aust, 47, Jensen, H. [. 1940 The Redhank (or Wollogorang) Copper Field, Northern Territory, A.GGS.N.A. Rept. N. Terr. No. 50 Jensen, H. I 1941 The Lawn Hill Silver-Lead-Zine-Field, Lawn Hill- Wollogorang Dis- trict. A.G.G.S.N.A, Rept Old. No. 46 Jensen, H. I. 1944 The Geology of Central Australia. Proc. Roy. Soc. Qld, $6 Jensen, H. I, 1945 The Origin, Distribution and Mode of Occurrence of Mica in Central Australia. Proc. Roy. Sac. Qld, 57 Jones, O, A, 1947 Pres. Address: Ore Genesis in Queensland. Proc. Roy. Soe, Old, $9 pti Jutson, J. T. 1934 The Physiography (Geomorphology} of Western Australia. Geol. Surv. W. Aust., Bull. 95 Krex, 5. N. 1941 The Mount Hardy Copper Field, Central Australia. A.A.G.S.N.A. Regt. N. Terr,, No, 55 Kine, a Pe Nil The Cyclic Land-Surfaees. of Australia, Proc, Roy. Soc. Vict, 62, pt Kreeman, A. W. 1934 An jpieelte from “The Granites,” Northern Territory. Trans, Roy. Soc. S. Aust., Kirrman, A, W, 1937 The ‘Soathern Extension of the Pine Creek Goldfield. A.G.G.S.NLA, Rept. N, Terr., No, 24 KLEeEeM ne AN 1938a The Wolfram Hill-Hidden Valley Area, Pine Creek District. [dem. No, Kicemayn, A, W, 1938) The Horseshoe Creek Tinfield, Pine Creek District. Idem. No. 37 Lewis, T. V. 1938 The Maranhoy Tinfeld, A.G,G.S.N.A, Rept. N. Fers., No, 35 160 Linvsay, D. 1883-84 Explorations through Ambemt Land. §. Aust, Parl Pap. No, 239 Lixngay, D. 1893 Journal of the Elder Scientific Exploring Expedition, Adelaide Lixnsay, D., and Wiysecke, C. 1898-99 Reports on Northern Territory Tablelands. 5. Aust, Parl Pap., No. 66 Hapmars De 1934 The Mackay Aetial Survey Expedition, Central Australia. Geogr. Journ, o 4 Manican, © T. 1930 An Aerial Recopaissance into the South-eastern Portion of Central Australia. Proc. Roy. Geogr. Soc. Aust. S, Aust Branch, 30 Manan, C. T, 1931 The Physiograpliy of the Western Macdonnell Ranges, Central Aus- tralia. Geogr. Journ., 78, No. 5 Manican, C, T. 1932a The Geology of the Western Mactlonnell Ranges, Central Australia J1.G.S. 88 Manica, 4 T. ay The Geology of the Eastern Macdonnell Ranges. Trans, Roy, Soc. >. Aust, Manan, C, T. \ 1933 The Geology of the Macdonnell Ranges, ete. Rept. A.N.ZA,A.S., 21 Manscaw, C. T. 1936 The Australian Sandridge Deserts, The Geogr. Review, 26, No. 2 Manioan, C. T. 1937 Addition to the Geology of Central Australia, Rept. ANZAAS. MAAR oe 1938 “fhe Simpson Desert and its Borders.. Jotirn and Proc, Roy. Soc. S.W,, 71 Martretson, R. S., and Trrcuert, C. 1945 Geological Reconnaissance in the Eastern Portion of the Kimberley Division, Western Australia. Ann. Rept. Geol, Surv, W, Aust. MarTEEryy, We H., 1905a Report on the Macdonnell Ranges Mining District. S. Aust. Part, ap. No, 50 Matraews, W. H. 19056 Report on the Arltunga and Winsiecke's Goldfields, and Harts Range Mica Fields. 5, Aust. Parl. Pap., No. 75 Mavrice, R. T. 1904 Extracts fromm Journal of Explorations. S, Aust, Parl, Pap. No 43 Mawson, D., and Manican, C. T. 1930 Pre-Ordovician Rocks of the Macdonnell Ranges, Central Australia Q.).G.S,, 86, pt. 3 Mawson, D., and Spreicc, R. C. 1950 Aust, Journ. Sci., 13, 3 Mawson, D. 1930 The Occurrence of Potassium Nitrate near Goyder's Pass, Mae- donnell Ranges, Central Australia, Min. Mag., 22 Mawson, D. 1925 Evidence and Indications of Algal Contributions in the Cambrian and Precambrian Limestones of South Australia. Trans. Roy, Soc. S. Aust, 49 Mawson, D, 1939 The Late Proterozoic Sediments of South Australia. Rept. A.N.Z.AA.S, 24 Mawson, D: 1947 The Adelaide Series as developed along the western margin of the Flinders Ranges. Trans. Roy. Soc. 5, Aust, 71 Miter, W, J. 1923 Precambrian Folding in North America, Bull. Geol. Soc, Amer., # Mounow-Campaett, J. 1917 Laterite—Its Origin, Structure and Minerals. Min Mag., 17 Noaxes, L. C. 1949 A Geological Reconnaissance of the Katherine-Darwin Region, North- ern Territory. Cwlth. of Aust. Bur. Min. Res, Bull., No. 16 Oxrver, T. G. 1917) Report on Tananm Goldfield by the Direetor of Mines, Northern Terri- tory Parkes, J. V. 1892 Report on Northern ‘Tetritory Mines and Mineral Resources. S, Alst. Parl. Pap, No. 32 Penoieton, R, L. 1941 Laterite or Sila Laeng, a peculiar Soil Formation. Thar Sc. Bull, 3 Patoer, R. T. 1945 IRyneous Activity, Metamorphism and Ore-Formation in Western AUis- tralia. Journ Roy. Soc. W. Aust, 31 Rennie, E. H. 1889 On some so-called South Australian Rubies. Trans, Roy. Soc. 5. Aust, 49 Simpson, E. S. 1912 Notes on Laterite in Western Australia. Geol. Mag., 9 Srmtweu., F. L., and Enwarvs, A, B. 1942 The Mineral Association of Tennant Creek Gold. Proc, Aust. Inst, Min. Met, N.S. No, 126 Stretcn, V. 1893 Scientific Results Elder Exploring Expedition; Geology. Trans, Roy, Soc S. Aust. 16, pt. ii PURER Cc 5. 1540 The Hercules Gold Mine, Pine Creek District, A.G.G.S,N.A. Rept. . Terr., No. Sutaran, C. J. 194Sa Mineral Resotitees of Australia. Summary Report No. 18. Beryllien Sunrwan, C, J. 1945b Ider No, 19. ‘Tantalum and Columbium, Suttvay, C. J. 1946 Idem, No, 24, Pigment Minerals District, Northern Territory, Aust, Inst. Min. and Met Taunor, H. W. B. 1910 Geological Observations in the Country between Wiluna, Hall's Traus. Roy. Soc, S, Aust, 1954 Vol, 77, Plate I Fig. 1 Looking south from Alice Springs. Archaeozoic Granite Gneisses in foreground, Unconformable junction of base of Heavitree (Pertaknurra) Quartzite marked in black, Fig. 2 Native Gap, north of Alice Springs, showing faulted northerly dipping sand- stones, probably part of an overfolded syneline of Pertaknurra age. Looking east-north-east. Trans. Roy. Soc. S. Aust., 1954 ‘ Vol. 77, Plate If ete Fig. 1 Horizontal Ordovician sandstones lying uuconformably on the Arunta Complex at Barrow Creek. Looking east. Fig. 2 Faulted margin of the southern edge of the Burt Plain, showing massive outcrops of the Arunta Complex in the background. Looking south, Trans. Roy. Soe. S. Aust., 1954 Fig, 1 View of part of Burt Plain about 100 miles w showing some of the numerous salinas of Vol, 77, Plate est of the Overland Telegraph Line, that district. Looking easterly. ~~ F eet goo The Granites, showing the occurrence of an adamellite monadnock in the sandplain, Vertical. All photographs are reproduced by permission of Adastra Airways. GEOLOGICAL MAP OF THE NORTHERN TERR ITORY OF AUSTRALIA ri ut 9 Ve ° Marine , Estuarine, Fluviatile, Lacustrine, Aeolian and Duricrust (MAPPED IN A FEW AREAS DISREGARDED WHERE SHALLOW! BATHURST Id MESOZOIC F<. => UPPER CRETACEOUS } TO JURASSIC of the Great Artesian Basin Darwin PT CHARLES = TERTIARY TO CRETACEOUS ? of Burt Trough, etc LOWER CRETACEOUS Mullaman Grcup, Plateau Sandstones TRIASSIC ? PALAEOZOIC PERMIAN q : : . Port Keats Group, - 4 c ees ae. Borroloola Area, ? r ‘ s . 4 4 ae Finke River Series? Port Keats 2 14° DEVONIAN Burt Range Basin Collia Series? ORDOVICIAN North of Amadeus Geosyncline. 0 0 GULF OF CARPENTARIA CAMBRIAN | Aa = j a4 ee? q ies Z r = pers ? ‘ Z 4 a Pa) Buldivan Series H ay . i : SILURIAN ?-CAMBRIAN Amadeus Geosyncline. PROTEROZOIC UPPER PROTEROZOIC Pertatataka and Pertaknurra Series. Borroloola Wollogorang Area? MIDDLE PROTEROZOIC Davenport Series Hatches Creek Group Carpentaria Group Victoria River Beds ? etc. LOWER PROTEROZOIC Agicondi Series ARCHAEOZOIC UPPER ARCHAEOZOIC Hart's Ranges etc? Riddock Series LOWER ARCHAEOZOIC Arunta and Musgrave | Blocks. Aruntan Series Acid Igneous Intrusions Strike Trends “a Generalized ARUNTA Xs ? AUSTRALIA. win Alice Springs Ms i SS hal P ™ “ss ib ; avs ‘ =" *y GREAT \, ARTESIAN es = oo 9° “> = oo. aw . f BASIN MUSGRAVE we f 40 60 ‘ foul £ Kosafeld. = . ——=———$ —__—_-——— ns Ss (5p Gi ae 161 Tarnor, H. W. B. 1918 The Geological Results of an Expedition to South Australian Border, ete. Journ. and Proc, Roy. Soc. W. Aust., 3 Tatnor, H. W. B. 1920 The Geology and Mineral Resources of the North-west, Central and Eastern Divisions. Geol. Surv. W. Aust. Bull. 83 Taunor, H. W. B,, and Cuarke, E. pe C, 1917 A Geological Reconnaissance of the Country between Laverton and the South Australian Border. Geol. Surv. W. Aust. Bull, 75 Tare, 1, and Watt, J. 1896 Report of the Horn Expedition to Central Australia. Pili Geology and Botany Tricuert, C. 1939 The Mesozoic Transgressions in Western Australia, Aust, Journ, Sci. 2. No. 3 Tercuert, C, 1947 Stratigraphy of Western Australia. Journ, and Proc, Roy. Soc. N.S.W,, 85 . Tercuert, C. 1949 Observations on Stratigraphy and Palaeontology of Deyonian, Western Portion of Kimberley Division, Western Australia. Cwlil, Aust, Bur. Min, Res. Report, No. 2 Terry, M, 1934 Explorations near the Border of Western Australia. Geog. Journ, 84, No. 6 TIETKENS, phe 1889. Jourtal of Central Australian Exploring Expedition. 5. Aust, Parl Pap. No. 115 ’ Trnpate, N. B. 1931 Geological Notes on the Illiaura Country north-east of the Mac- donnell Range, Central Australia. Trams. Roy Soc. S. Aust, 55 Tinnare, N. B, 1933 Geological Notes on the Cockatoo Creek and Mount Liebig Country, Central Australia. Trans. Roy, Soc. 5. Aust, 57 Vorsey, A. H. 1937 Geological Report on the Woolwonga Area, Pine Creek District. A.G.G.5.N.A. Rept. N. Terr. No, 12 Vorsey, A. H. 19391 Notes on the Stratigraphy of the Northern Territory of Australia, etc. Journ. and Proc. Roy. Soc. N.S.W,, 72 Vorsey, A. H, 1939b A Contribution to the Geology of the Eastern Macdonnell Ranges, Central Australia). Ibid Wane, A. 1924 Petroteum Prospects. Kimberley District of Western Australia and North- ern Territory. Cwlth. Parl. Pap,, No, 142 Warp, L. K. 1925 Notes on the Geological Structure of Central Australia, Trans. Roy. Soc. S. Aust.,. 49 Warn, L. K. 1926 Report on Water Supply Facilities on Stock Routes and elsewhere in the Northern Territory of Australia, Govt. Printer, Melbourne Weis, L. A. 1907 The Victoria River and the adjacent country. Govt, Printer, Adelaide Wetts, L, A., and Grorcz, F. R. 1904 Reports on Prospecting Operations in the Musgrave, Mann and Tomkinson Ranges. S. Aust. Parl. Pap., No, 54 Warrenouse, F. W.. 1928 The Correlation of the Marine Cretaceous Deposits of Aus- tralia, A.A.A.S., 18 ; Warrenousr, F. W. 1940 Studies in the Late Geological History of Queensland. Univ. Qld. Papers, Geol. Dept., 2 (N-S.), 1 ; Warrenouse, F. W. 1941 The Surface of Western Queensland, Proc. Roy. Soc. Qld, 53 Witson, A. F. 1947 The Musgrave Ranges—an Introductory Account. Trans. Roy. Sac, S. Aust, 71, (2) Winwecee, C. 1884 Mr, Wintecke’s Explorations during 1883, 5, Aust, Parl. Pap., No. 39 Woornoucs, W. G. 1927 Presidential Address. Jotirn. and Proc, Roy. Soc. N.S.W, 61 Woounouce, W. G. 1933 Report on Aerial Survey Operations in Australia during 1932. Govt. Printer, Canberra ICHTHYOSTRONGYLUS CLELANDI n.g., n.sp., FROM AN AUSTRALIAN SHARK BY PATRICIA M. MAWSON Summary Ichthyostrongylus clelandi n.g., n.sp., a Trichostrongyle worm, is described from the spiral valve of Emissola antarctica from South Australia. This genus is distinguished from others by the shape of the head. 162 ICHTHYOSTRONGYLUS CLELANDI ng. nap, FROM AN AUSTRALIAN SHARK By Patricia M. Mawson * [Read 10 September 1953] SUMMARY Tehthyosirongylus clelandt wg, msp., a Trichostrongyle worm, is described from the spiral valve of Emissola axtorctica from South Australia. The genus is distinguished from others by the shape of the head. A numberof Trichostrongyle worms were found in a tube labelled: “(1) Flukes from liver of salmon, (2) Cestodes from spiral valve of Sweet William Shark, Encounter Bay, 1/1922." There is an clement of doubt as to whether the nematodes, which were very much smaller than the flukes or the cestodes, came from the salmon, Arripis trutta, or the shark, mtssola antarctica. Because of the way in which the nematodes were lying intertwined with the cestodes in thick masses of intestinal material, while the flukes were separate from these, it has been assumed that they were from the elasmobranch, The males are up to 4-2 mm. in length, the females to 6-0 mm.; the maximum body diameter is 0°l mm. in the male and 0-13 mm. in the female. The cuticle is very markedly striated throughout the body, even on the bursa. The head end is slightly enlarged, forming a distinctive bulb, not by cuticular inflation but by thickening of hypodermal tissues and of the anterior oesophageal muscles, The mouth is surrounded by three strongly cuticularised shallow lips, which give the appearance of a cap at the anterior end. Each lip bears two rather elongate papillae. A buccal capsule is absent. The oesophagus is straight and cylindrical and measures about a tenth of the body length. The nerve ring is very small anc hard to discern; in those specimens in which it is seen it lies at the midlength of the oesophagus. The excretory pore, lying shortly behind the nerve ring, is very distinct, as its duct is strongly cuticularised. The ovaries are opposed, The vulva lies one-fifth to one-seventh of the body from the posterior end, The ripest eggs, containing morulae, are 70 by 40 p. The cuticle aroutid the vulva is slightly inflated, forming a folded belt in this region. The male bursa is tightly folded in all specimens; to examine the rays, shown in fig. 2, it was necessary to tear part of the bursa. The exact form of the dorsal ray varies slightly, the third bifurcation in some cases taking place nearer to the second than shown in fig. 2. The spicules are relatively simple for a Tricho- strongyle worm; the head is provided with a ventral knob; there is a slight swell- ing at the midlength, and from this projects a dorsal spite. The main body of the spicule ends in two small points. The overall length of the spicule is 0-13 - 0-14 mm., and that of the simple plate-like gubernaculum 40-48, There is a pair of rather elongate subventral prebursal papillae. This, as far as can be ascertained, is only the second record of a Tricho- strongyle worm from a fish. The first is Agamonema scorpaenae cirrhosae Mac- Callum 1921, renamed by Travassos (1937, 410) Trichostrongylus (s.1.) ses. Of this species, Travassos (loc. cit.) states that it was possibly an accidental occurrence. In the present case, this seems a most unlikely hypothesis. The worms are present in considerable numbers, and in a perfect state of preservation, and as they were taken from the spiral yalve of the host, it is not conceivable that they were ingested with bait. The life history of this Trichostrongyle is, pre- * University of Adelaide, Traua. Roy Soc. 5. Alist., 77, July, 1954 163 sumably, similar to that of related genera in ruminants. The infective larvae might be expected to inhabit the top layer of mud or sand on the sea floor, or to be on sea weeds growing there. Emissola antarctica is largely a browsing shark. _ I. clelandi differs from T. maci (s.1.) in the shape of the head, the position of the vulva, and in the disposition of the lateral and ventral bursal rays; it is not possible to compare the dorsal ray as this was not figured by MacCallum, The shape of the head is different from that of any Trichostrongyle of which the description is available to the author. In the form of the bursa and spicule it is perhaps closest to Oswaldocruzia Trav., differing from this genus in the shape of the head. A new genus is proposed, with the following diagnosis : Ichthyostrongylus n-g. Trichostrongylidae: head bulbous with three distinct and strongly cuticular- ised lips; buccal capsule absent. Ovaries opposite; vulva posterior but not close to anus. Spicule simple, with dorsal spine; gubernaculum present. Bursa symmetri- cal, dorsal lobe developed; externodorsal rays arising separately from dorsal, and lying in lateral lobes; dorsal ray dividing three times, forming six branches, Type species. I. clelandi n.sp. from Emtissola antarctica, Encounter Bay, South Australia. The specific name is for the collector of the worms, Dr. J. B. Cleland, in gratitude for his help. OQ.) mm. Fig. 1, head; Fig. 2, spicules and part of bursa; Fig. 3, ventral view of spicules;; Fig. 4, tail of female; Fig. 5, region of vulva. Fig. 2 and 3 to same scale. LITERATURE MAGNE m4 A, 1921 Studies in Helminthology. Zoopathologica, 1, (6), Travassos, L. 1937 Rivisao da familia Trichostrongylidae Leiper 1912, Monogr. Inst. Oswaldo Cruz., No, 1, 1-512 —_ PARORCHIS ACANTHUS VAR. AUSTRALITS, N. VAR., WITH AN ACCOUNT OF THE LIFE CYCLE IN SOUTH AUSTRALIA BY L. MADELINE ANGEL Summary . A review of the history of Parorchis acanthus Nicoll and its synonymy is given. Stage in the life cycle of P. acanthus var. australis n. var. are described. . The variety differs from the type species mainly in the absence of an excretory tube in the tail of the cercaria. Other relatively minor differences are noted. . The cercaria has been found as a natural infection in South Australia in Bembicium auratum (Quoy and Gaimard), B. melanostoma (Gmelin), B. nanum (Lamarck), and Emozamia flindersi (Adams and Angas). It encysts on the surface of hard objects, including a number of invertebrate animals, which are probably only accidental hosts. . Cysts were fed to seagulls, Larus novae-hollandiae Stephens, and adult trematodes were recovered. The adult was found as a natural infection in 1 of 25 seagulls examined by the late Professor Harvey Johnston. . The incidence of infection in the different snail hosts is given. This was highest in Bembicium auratum (up to 66%). The percentage of infection as determined from those snails which gave off cercariae when isolated, is much less than the true percentage, determined by crushing the snails. 164 PARORCHIS ACANTHUS VAR, AUSTRALIS, N, VAR., WITH AN ACCOUNT OF THE LIFE CYCLE IN SOUTH AUSTRALIA By L. Mavetine Ancet. * [Read 10 September 1953] SUMMARY A review of the history of Parorchis acanthus Nicoll and its synonymy is given, Stages in the life cycle of P. acanthus var, australis 1. var. are described, The variety differs from the type species mainly in the absence of an excrétory tube in the tail of the cercaria, Other relatively minor differences are noted, The cercaria has been found as a natural infection in South Australia in Bembiciuim auraitum (Quoy and Gaimard), B. melaonostoma (Gmelin), B. nanum (Lamarck), and Emasomia findersi (Adams and Angas). It encysts on the surface of hard objects, incluid- ing a number of invertebrate animals, which are probably only accidental hosts. Cysts. were fed to seagulls, Larus novae-hollandiae Stephens, and adult trematodes were recovered. The adult was found as a natural infection in 1 of 25 seagulls examined by the fate Professor Harvey Johnston. , 6, The incidence of infection in the different snail hosts is given, ‘This was highest in Bembicium auratum (up to 669%). The percentage of infection as determined from those snails which gaye off cercariae when isolated, is much less than the true percentage, determined by crushing the snails. : = NS te The type as well as other representatives of the adult and larval stages have been deposited in the South Australian Museum, This work was commenced with the late Professor Harvey Johnston, to whom I am greatly indebted for his unfailing help. I wish to acknowledge with gratitude the help given by Mrs. H. Anderson, who supplied the figures of the infection of snails trom the Patawalonga Creek determined by crushing, as well as other details. Acknowledgment is also made of help given by the staff of the South Australian Musetim in identifying intermediate hosts, and by members of this department in collecting material, as well as in other ways, INTRODUCTION In 1907 and 1912. Lebour described Cercaria purpura sp. ing. from Purpura lopiius in Great Britain, Later (1914) she identified it, on the grounds of mor- phological similarity, as FParorchis acanthus Nicoll 1907. P. acanthus was originally described as Zeugorchts acanthus (Nicoll 1906) and later rehamned and redescribed (Nicoll 1907 a, 1907 b), Zeugorchis heing pre-occupied. Stunkard and Shaw (1931) described Cercaria sensifera from Urosalpinx cinereus from Waood’s Hole, Massachusetts, stating that it might be identical with Cercaria purpurae, They also suggested that C. sensifera might be the larval stage of Parorchis avitus Linton 1914. (Linton’s type material, from the herring gull, Larus argentatus, was from the same region.) Linton (1928) had discussed the possibility of synonymy of Parorchis avitus with P. acanthus, but did not change his classification. In 1932 Stunkard and Cable recorded Thais (Purpura) lapillus as another host of Cercaria sensifera. They had fed cysts of this form to guinea pigs, white rats, mice and two species of tern, and obtained immature flukes, which they identified as Parorchis avitus, only from the terns, Sterna hiryndo and S. dougalli, The diagnosis was confirmed by Linton- Cable and Martin (1935), who obtained mature adults after feeding meta- * Department of Zoology, University of Adelaide, South Australia. Trans. Roy Soc. S. Aust. 77, July, 1954 165 cercariae of Cércaria sensifera to herring gulls, concluded that Parorchis avitus was invalid, and was a synonym of P. acanthus. Cercaria sensifera was thus synonymous with C, purpurae. Rees (1937) from other evidence, independently suggested that C. sensifera and C. purpurae were identical and that the names of the adults were synonymous. This suggestion was supported by a later examination of the adult parasites (Rees 1939). Dawes (1946) listed Parorchis avitus as a synonym of P. acanthus. j UB o-1mm Fig. 1 Parorchis acanthus var. ausjralis. The cercaria. Fig. 1, stained and mounted; excretory bladder and pore from living specimen. Position of dorsal collar spies indicated. 2, anterior end of body to show narrow- ing of cuticle. 3, 4, tail; 3, living, contracted; 4, fixed, elongated. Fig, 1, 4 to same scale; 2, sketch; 3, sketch. ep, excretory pore, Maxon and Pequegnat (1949) described a cercaria (Echinostome IT) from Upper Newport Bay, California, which was probably identical with that described by Hunter (1943) as the cercaria of P, avitus (Cercaria sensifera Stunkard and Shaw 1931). Reish (1950) recorded Parorchis acanthus from Larus occidentalis from Newport, Oregon. Rediae and cercariae which agreed with the descriptions given by Stunkard and Cable (1932) for those of Parorchis avitus (= P, acanthus) were found in Thais emarginata from this vicinity. Encysted cercariae were fed to one golden hamster and one mallard duck, but did not develop in either animal. 166 The present investigation was’ initiated when megalurous cercariae were found in a marine tank containing Bembicium auratum (Quoy and Gaimard)} (Anderson, personal communication). These cercariae, which were similar to Cercoria pur- furne Lebour as described by Rees (1937), were later found to be a common parasite of the snails, The cercariae encysted on any hard surface. Cysts, collected from glass dishes in which the host snails were isolated, were fed to seagulls, from which adults of a species of Parorchis were recovered later, In al] stages of the life cycle the only significant difference between the Australian form and P, aganthus Nicoll was in the absence of an excretory tube in the cercarial tail, but it is thought that this difference is sufficient to warrant placing the Australian specimens in a distinct sub-species, for which the name Parorchis acanthus var. australis is proposed. A description of the life history of this form follows. THE EGG AND MIRACIDIUM Eggs were dissected from the adult, fixed in formalin and cleared in glycer- ine; the range of the larger ones was from 94 by 56y to 98 hy 64, (Rees (1940) found that ripe eggs were considerably larger than those in which the tnitacidium was freely formed; her measurements were made in sea-water, the ripe eggs being 130 by 68, and the young ones 90 by 35). The eggs did not appear to hatch freely, but those examined had been obtained from a specimen kept in the refrigerator for two or three days in normal saline, and ynder these samewhat unnatural conditions the eggs may have been extruded before they were fully mature. One miracidium hatched quickly when it was placed in sea- water under a coverslip, and this was the only one which remained alive under a coverslip for any length of time; it died immediately when neutral red was added. In this one specimen all the main features described by Rees (1940) could be seen, te, the rostrum, penetration glands and gland pores, the united kidney-shaped eyes, the brain region, the apical gland, the lateral processes (which help the miracidiumi in its escape from the shell}, and the contained redia lying at the posterior end of the résting miracidium. The artangement of the epithelial cells was not exantined, but the subepithelial layer of cells was apparent, and the arrangement of the cilia also corresponded to Rees’ description, No flame cells were seen, but parts of the excretory tubes were visible in the same positions as figured by Rees. THE REDIAE The rediae were white and opaque. The small (first generation) rediae varied from 0-34 by 0°052 mm, to 0-63 by 0-060 mm, in ten formalinised specimens, the average being 0465 by 0-060 mm. They agreed with the description givert by Stunkard and Shaw (1931) in having a muscular, lip-like snout in front of the “oral sucker”; also the posterior tip of the body was protruded in a tail-like or foot-like protuberance, used, like the foot processes, in locomotion. The birth- pore, as in Rees’ material (1937, p, 66) was thick-lipped, conspicuous and pro- trusible, Rees (1937, 1940) recorded that first generation rediae did not produce cercariae, but gave rise to twenty or more daughter rediae. Stunkard and Shaw (1931) stated that small rediae may contain one or more fully formed cereariae. No cercariae were observed in the small rediae of the South Australian material. The large (second generation) tediae varied from 1:39 by 0'255 mm. to 1:92 by 0:345 mm, in ten formaiinised specimens; the average size was 1°67 by 0295 mm. Stunkard and Shaw (1931) stated that rediae increased toa length of 2-1 mm. and a width of 0°4 mm. (presumably in living material), Rees (1937), for living material, gave the measurement of a fully grown redia as 3°5 mm. by 147 0:46 mm. and of a young redia a§ 0-58 by 0-08 mm. It will be noticed that the size Is great than that of the Australian form. (Fixation of the rediae in forma- lin probably does not produce a very great change in size.) THE CERCARIA The cercaria was vety similar (anatomically, in habit, and in reaction to intra-vitam stains) to that described by Stuttkard and Shaw (1931) and Rees (1937), with the exception that an excretory system could not be demonstrated in the tail. Lebour (1912) recorded that the excretory system was not continued into the tail of Cercaria purpurae, but Stunkard and Shaw (1931) found this feature in Cercaria sensifera, and this supposed difference was one of the characters by which Stunkard and Cable (1932) separated Parorchis acanthus and P. azitus. However, in 1937 Rees noted the excretory tube in the tail of Cercaria purpurae. In 1953 (personal communication) Dr. Rees stated that the excretory tube in the tail was difficult to find in Parerchis aconthus; that other workers at Aberystwyth had experienced the same difficulty, but that its presence had been confirmed on several occasions. No sign of an excretory tube in the tail was seen in several hundred cer- cariae examined over a period of eighteen months, Basic fuchsin did not make the details uf the excretory system any clearer, as it does with most fresh-water ecercariae; and horse serum, which is also very useful with most forms, caused the cercariae to encyst immediately, even in very dilute solution, However, the excretory system, with an excretory pore opening from the bladder to the ventral body surface, was clearly seen, This latter feature has not been mentioned by other authors, It would tot be surprising, perhaps, if an excretory pore in the body should be present at the same time as the two pores in the tail, but failure to demonstrate the latter over such a long period cannot be ignored. The number of collar spines was difficult to deterntine. It was at least 60, and in one specimen possibly 66; there were 10-11 on each side ventrally. Stunkard and Shaw (1931) recorded 44-48 spines on the dorsal surface and 10 on each side ventrally. Rees (1937) gave the total number as 64. The ratio of oral sucker to acetabulum varied from 2:3 to 3:4 in living specimens. Immediately anterior to the first row of body spines the cuticle was thinner for a short distance, after which it widened again in the region of the anterior papillae (fig: 1, 2). This thinning of the cuticle has not been described for Pararchis acanthus, 1 was noticeable in greatly compressed specimens, as well as in specimens stained with neutral red which were still elongating and contract- ing. The region of thinner cuticle was very much paler than the rest of the cuticle. The cuticular layer, which probably consists of cuticle plus cystogenous material, is 8-9 wide in living, flattened specimens; it stains a uniform, carmine colour with neutral red. The primordia of the reproductive system are obvious in stained specimens, The only feature in which the tail differed from the descriptions given by Stunkard and Shaw (1931, p. 265) and Rees (1937, p, 67), apart from the absence of an excretory tube, was that it was marked with very fine annuli on which were arranged minute spots, which might have been granules or tiny spines (fig. 3). These were variable in size, but even the largest were extremely small. The annuli were seen well after treatment with orange G; there were about six across the diameter of one of the large vacuolated cells of which the proximal part of the tail is composed. Stunkard and Shaw ( 1931) and Rees (1937) described the cuticle of the tail as being thin and smooth, The following measurements were made on twenty specimens fixed by add- 168 ing an equal volume of boiling 10% formalin to the water containing the cer- cariae ‘body length 370-670 2 (average 450 4); greatest width 130-225» (average 170 «); width at “waist” (constriction of body immediately postefior to acetabu- Jum) 105-180 p (average 130») ; tail length 265-595 » (average 450 ») ; tail width 45-60 (average 52»). Rees (1937) found the body length to be 1:00 mm, expanded and 0-36 mm. cantracted ; breadth 0-09 mm, expanded, 0°35 mm. contracted, The number of specimens measured was not mentioned, nor was the method of fixation, but elsewhere in the paper it was stated that rediae and cercariae were examined in the living state. Presumably the measurements represent the upper and lower range for living cercariac examined under a coverslip, and are thus not to be compared with measurements of specimens fixed in formalin. Stunkard and Shaw (1931) stated that fixed and stained specimens measured 0°21-0°47 mm. in length and 0°14-0:26 mm. in width; the jails varied from 0:12 to 0°26 mm. in length. The average body size of seven stained and mounted careabige of Perorciis acanthus yar, australis was 520 by 160», and for the tail, 615 by 504. Too much importance should not be attached to differences in measurements of cercariae, especially when the state of preservation of the matertal is variable- THE CYST Stunkard and Cable (1932) concluded that the cercariae would encyst on almost anything with which they came in contact. P. acanthus var. australis encysts readily on glassware, Animals which were placed in contact with cercariae and on which cysts were formed were :—the cirripede Alminius modestus (mainly on the appendages); the isopods H.xosphacroma gigas and Trichoniscus sp. (mostly on the joints of the legs); insect larvae of the Acalyptrate group (the body surface of these became so thickly encrusted with cysts that the insects, though still alive, could barely move); the crab Helice haswellianus (the shell of the body and legs was heavily encrusted); and the lamellibranch Amphidesma angusta (on the shell, more concentrated on the free edges, and scattered on the free edge of the mantle). The lamellibranch Anapella pinguis did not become infected ; this was buried in the sand, but the siphons were, of course, protruding. Rees (1948, p. 234) noted that cercariae of P. acanthus normally encyst round the aperture of the shell and on exposed parts of the body of the host, Nucella (Purpura) lapiilus. Cysts of the Australian form were sometimes found on the operculum of Bembiciwn axratum (im one case thirty cysts were present on the outer surface and the same number near the edge of the inner surface of the operculum); and occasionally om the inner surface of the shell, but they were never observed round the aperture, and rarely on the outer sarface of the shell, Cyst formation follows the same course as that reported by Rees (1937). Stunkard and Cable (1932) found that most of the cercariae encysted within 48 hours of leaving the snail. The Australian cercatiae encyst within a few hours. The cercariae encyst immediately when exposed to unfavowtrable conditions (such as too strong solutions of intra-vital stains), as was observed by Stunkard and Shaw (1931). The average measurement of 20 cysts from which the rough outer coat had been removed was 200 by 1804. Rees gave the cyst diameter as 0-295 mm., of which the outer layer was 0-045 mm. thick; the cyst enclosed only by the inner coat would thus be 0-205 mm. in diameter. Lebour and Elmhirst ( 1922), how- ever, described the cyst as “roundish oval,” which is consistent with the shape oi the Australian forni. 169 THE METACERCARIA , Metacereariae were recovered by breaking the cyst wall with needles. This often resulted in damage to the metacercaria, but some were recovered intact. The following measurements apply to specimens mounted in canada balsam. The length of four specimens averaged 405 (range 300-470). The average diameter of oral sucker was 65 p, and of ventral sucker 82% (in three specimens), The metacercaria most favourably mounted for measuring was 400 by 255», with the oral sucker 68 w (long axis) by 75», and the ventral sucker 87 » in diameter- Lebour and Elmhirst (1922) gave the measurements (apparently in living speci- mens) of the oral sucker as 0-08 mm. and of the ventral sucker 0°10-0'14 mm, The primordia of the genital system were slightly more obvious than in the cercaria; they consisted of two, small, darkly-staining masses of tissue. One, circular, or oval in the transverse plane, and situated immediately anterior to the acetabulum and posterior to the intestinal bifurcation, marked the position of the genital atrium and its associated structures. The other, slightly larger, circular or elongated in the longitudinal axis, and situated midway between the acetabulum and the posterior border of the body, was no doubt the primordium af the gonads and thete docts. The excretory formula was the same as for the cercaria, that is 2[(3-+3+3) + (3+3+ 3) I]. THE ADULT An accurate assessment of the number of collar spines was not possible in living specimens, and many of them disappeared in the preparation of permanent mounts. Nicol! (1907 b, p. 346) recorded the number as “about 60.” He men- tioned that immersion in a weak acid solution for even a short time caused the spines to disappear wholly or in great part, and suggested this as the reason for their absence in Distomuy pittactum Brawn, which he transferred to the genus Parorchis, Stunkard and Cable (1932, p. 333) gave the number of collar spines a “sbout 68."" Other authors have not recorded the number of spines for the adult. Table I gives measurements of adult and juvenile forms, with the measure- ments given by Nicoli (1907 b) and Linton (1914) for comparison. Ovaries and testes were measured in three specimens mounted in balsam, in which all measurements were slightly less than when the flukes were meashred in cedarwood oil. The ovary was rotinded or oval in outline; measurements were:—(1) 2404, (2) 290, in diameter, (3) 240 (long axis) by 255. (Rees (1939) described the ovary as transversely oval, measuring 0-29 by 0°33 mm.) The margin of the testes was lobed; they were sometimes elongated in the longitudinal axis, and sometimes one was situated slightly in advance of the other. In a specimen 5-2 mm. long the right testis was 525 by 450 and the left 560 hy 490 In the other specimens the testes were larger, but had the appearance of being more compressed. EXPERIMENTAL INFECTIONS Four seagulls (Larus notae-hollandiac) and a white mouse were fed with cysts. The mouse did not become infected, but adult Parorchis were obtained from two of the seagulls. Two seaguils caught at Tailem Bend“) on the River Murray were kept in re WO SESE NSO ee ee ee ee ee ee ES eee @ Altiough na work has been done in South Australia on the habits of the seagull, it seems likely that the birds retutn each day to the same feeding grounds. This view ts sup- ported by the fact that certain birds which can be identified by some deformity have been seen im the same place for several weeks at a time. Thus birds caught at Tailem Bend, although they probably return to a roosting ground near Lake Alexandrina (an inlet of the sea) each hight, are, in all probability, frequenters of the river and its shores, and are eoisidered unhikely to feed in places where Pembicitin spp, occur. 170 ‘JIYINS yeIO Se IIIT se 91M} ULY} s1OUr JOYIEI,, UM[NGeIIV » ‘sUaUTIDedS PajUNOU INO} JO sjUsUIaINSeayT “A 'qy3ua] “Wu pf ynoge JO [ENPtAipur we 0} pastsajar YZuay, uEY} Jayjo syusuTainsvaur {Buray Ayqissod jnq ‘payeys jou suammdeds jo uolIpuoy ‘AT ‘Bulrespd aojaq peinseour pue wulpeursoy ut paxy (s[[na 0} sjshd Surpsay jo ynsaz se paurejqo) sapuaanl gy “[]T ‘]10 poom Jepad Ul paimseattl (SUONDaJUT [eIN}eU se PUNO} OM} SHG ‘T Wory asoyj) si[Npe g “T] ‘BULIva]O JIOjaq Poinsvant puv ‘ainssaid JNoy}LM UlpeMIO; UI pexy ‘SJusTUIIadxe Surpeay Jo ynsar se paureyqo ‘s}y[npe g T “UIAIS. «- SPUQUIBINSEDT BY} WOIF PsUlUa}ap IIOM SOI IDYOING ‘sjayoeIq UIyyM USAID DIB SoNJeA ULI ‘SOIPIUIT[[IW Us S}uaWaInsvat JO asuel ay} oAls soinsy ayy - - - Tunpnqe}soe 2zitl +Z:1 . ZZ2it t1ayONs [BIO JO O1VERY (Z6-0) S€+1-12-0 * (r0-1) ¥+T- 6:0 7 s =. tiningepoy (Tr+0) 6F-0-9E-0 S+0- (£b-0) S-0- #0 - > 7 qayINS [2IQ (61-0) #2-0-41-0 £1-0 (61-0) 22-0-ST+0 - > Yypeasq (02:0) Z-0-8T:0 bZ-0 (zZ-0) $Z-0-61-0 - - y}Sua,—xudreyg 28+0-Z8-0 (990) Z:0-9-0 (6-0) £+I- 8-0 (ZIT) £+1-O-1 + —- aBYOO Ssoise yIpesig - (JeAd] TE[NGe}29"-prut) (9-1) 89-I-Te-T (h2-1) #-1-0'1 (9-1) O+Z- ZT (€6-1) 1-Z-8-T SIEM, JE WLIpeag (2-2) 99-2-01-Z “UnUE ¢— (9h-1) Z-I-2:T (S-Z) 0-€- 0-2 (S0-£) PE-2-2 - Julod ysopia ze yyprorg (€9-%) 88-S-96-£ c-¢ (eS) S+p-€-Z (€-S) Z-9- BE (0:9) 6:2-€°4 he q3ue7] (PI6I) uowurT A (42061) HOWIN AT sajtuaanf{ TIT simpy IT. synpy | es ne 2h ee ee —— ee St aw t= = on te i. SHYIUDID SIYIL0AD I StDAISND “TWA SHYIMPID *T ] Tavy WI captivity for several weeks before the experiment was commenced_ The first was given two insect (Aecalyptrate) larvae which were heavily encrusted with cysts; it was killed 32 days later. No Parorchis were found, though four heterophyids and a blood fluke were recovered from the intestine. The second gull was fed with a large number of cysts scraped from the sides of the tank in which the snails were kept; they were given 46, 38, 31 and 17 days before the bird was killed, when five mature and nineteen immature specimens of Parerchis were recovered. Of these, four adults and twelve juveniles were in the cloaca, and the remainder in the rectum. When the bird was killed, a period of 10-11 weeks had elapsed since it could have acquired infection under natural conditions; it therefore seems almost certain thar the juvenile, if mot the adult, trematodes had developed from the cysts fed to the birds. Faeces from the birds obtained 1, 7, 22 and 29 days after commencement of the experiment were free of eggs. Of four seagulls captured at St. Kilda beach (a few miles north of Adelaide), two were killed immediately; no Parorchis were recovered, The other two were given meat in which cysts had been packed; neither of the birds was interested in food, and it is doubtful how many of the cysts were ingested, The first gull died’ in two days; it was negative for Parorchis, The second died eight days after exposure to infection, and one medium-sized, egg~bearing specimen of Pororchis was found in the duodenum (length 4°7 mm.). If this specimen had developed as a result of the experimental feeding (its Iocation in the duodenum and the fact that the three other birds from the same locality had not harboured the infection suggesting this) the trematode must have become egg-bearing in eight days, whereas nineteen specimens from the other experimental host (from Tailem Bend) were still immature at least seventeen days after they had been ingested as cysts. Stunkard and Cable (1932) found that specimens recovered fifteen days after infestation were not sexually mature. Two attempts to infect Bembicium spp. with miracidia failed. Ta the first about 25 Parerchis eggs were put in a small tank with three Bembictum nanwm ; and in the second, seagull faeces collected from the Patawalonga mud- flats were used, with eight B, auratum. The experiments were not repeated, because of the shortage of adult trema- todes from which to obtain eggs, | INCIDENCE OF INFECTION IN SNAILS The cercaria of Parorchis acanthus var. australis was first identified from Bembicium auratim (Quoy and Gainmvard) collected from a tidal mud-flat at the mouth of the Patawalonga Creek, Glenelg, South Australia; a high percentage of the snails was found to be infected,‘?)? The number of infections detected by isolat- ing each snail in a 3” x 1” tube over a twenty-four hour period was considerably less than the true number as determined by crushing the snails, For instance, from April to September 1951 (inclusive}, of 582 B. auratwm isolated, 64 (11%) gave off cercariae, while in the same period, of 1,072 snails crushed, 633 (59% ) were infected. The true percentage of infections must have beer even higher, since at least some of the snails crushed were from groups which had been isolated, and from which those snails actually giving off cercariae had been removed. In collections made in October-November 1951, and in May-September 1952, infections identified by crushing snails which had not been isolated pre- viously were 1,159 of 1,758 (66%). @) Several other types of cercarial infection were found in Rembicium spp. but Parorchis infections were readily distinguished by the large, characteristic rediac. 172 The high percentage of infection of the snail host seems somewhat surprising, in view of the fact that in 1939, only one of eight seagulls from this region was infected with Parorchis acanthus. However, silting up of the stream, which has occurred rapidly since 1937, has no daubt had a strong influence on the ecology of the region, and it may well be that in 1939 Bembicium auratum was not a common member of the fauna as it is today. These cercariae have also been found in B, nanum (Lamarck) and B. selanostoma (Gmelin), but the percentage of infection is much less in both species than in B. awratum. It is, however, impossible to draw any conclusions as to any host. preference shown by the parasite, because of the different habitats favoured by the three species of host, In the Patawalonga mud flats B, anratun is to be found at low tide in small pools where the chances of infection are high; at low tide B. melunostoma occupies more exposed positions on small rocks, mangroves, etc.; B. nanum lives on rocks which are exposed at low tide and subjected to strong wave action at high tide. Parorchis cercariae wete found by isolation in 1 of 360, and by crushing in 10 of 431 Bembicivm nonum collected along the coast from Marino Rocks to Encounter Bay, South Australia, and im two of three B. nemum from the Patawalonga Creck (where infections were so common in B. auratum). The infection was not found by isolating over a hundred 8. nonum collected in February 1952 along the coast of Yorke Peninsula; nor by crushing 50 of the snails collected south of Corny Point (Yorke Peninsula) and 15 from Salt Creek (Yorke Peninsula) in February 1953. In October 1952, 11 of 434 B, melonestoma from Port River and Outer Harbour were found to be infected by crushing, In February 1953, of 450 B. melanostoma collected on Yorke Peninsula, five were infected. These five infected snails were from a collection of 50 taken at Port Wakefield, where con- ditions for infection must have been favourable; the remaining 400 were collected from Pine Point, Stansbury, Salt Creek, Edithburgh and Corny Point. Infected snails will remain alive and continue to give off cetcariae for some time under laboratory conditions. Eighteen B. auretum kept under observation survived 14, 30, 39, 49 (seven snails), 55 (three snails), 61, 88, 91 and 95.days respectively, Anderson (1953) kept 20 snails out of water for three months; of the six which survived, five contained rediae. Other gastropods which were examined during this investigation were: 98 Melaraphe unifasciata and 42 Austrocochlea concamerata from Hallett’s Cove; 22 A. torrt trom Marino Rocks, and a ntimber of Salinatar fragtlis and S. solida from the Patawalonga. None of these gave off cercariae when isolated. Snails from Yorke Peninsula were examined after crushing: 50 Neothats texttliose Thaididae) from an ocean beach south of Corny Point were uninfected, but two of 13 Emazamte flindersi (Murtcidae) from Port Vincent, and two of 7l of a same host irom Pine Point were infected with Perorckis acanthus var. australis, DISTRIBUTION AND HOSTS OF PARORCHIS ACANTHUS ADULT P. acanthus has been recorded from the herring gull (Larus argentatus) from Great Britain and from the east coast of North America; the common gull (L. canus) from Scotland; the western guli (ZL, occtdentelis) from the west coast of North America: the flamingo (Phoeniropterus ruber) from Cuba (Vigueras, 1941}; and, as a restilt of experimental feeding, from terns (Sterna hirundo and S, dowgalit) from Massachusetts. Parorchis acanthus var, australis is now recorded from Soyth Australia. The adult was found by the late Professor Harvey Johnston in only one of 25 173 seagulls (Larus novae-hollandiae) examined between 1937 and 1951. This positive host was one of eight gulls caught at Glenelg in 1939; it contained two adults and one immature specimen of the Auke. The remaining negative birds were from other parts of St. Vincent’s Gulf (5), American River, Kangaroo Island (1), and River Murray (11). CERCARIA ; The cetcaria has been recorded from Nucella lapillus and Urosalpinx cinereus irom Great Britain and Massachusetts, U,S.A., and from Thais emarginata from Oregon. Cerithidea californica trom California also harbours tediae and cer- cariae which are very probably the larval stages of Pororchis acanthus. The known South Australian molluscan hosts of P. acanthus var. australis are Bembicium curatum, B. melanostoma, B. narum and Emozamia flindersi. LITERATURE Anperson, H. 1953 Studies on the biology of three species of Bembicium and their trematode parasites. (M.Sc. thesis; not yet published ). Cante, R, M., and Martin, W. E. 1935 Parorchis avitus (Linton, 1914), a synonym of P. acanthus (Nicoll, 1906), Jour. Parasit., 21, (6), 436-437 Dawes, B. 1946 The Trematoda. University Press, Cambridge. 644 pp. Hunter, W. S. 1943 Studies on cercariae of the common mud-flat snail, Cerithidea californica, Unptiblished doctor's dissertation. U.C.L.A.. 129 pp. (not seen) Lesour, M. V. 1907 On three mollusk-infesting trematodes. Ann. and Mag. Nat. Hist., 19, (7), 102-106 Lenour, M. V. 1912 A review of the British marine cercariae, Parasitol, 4, (4), 416-456 Lenour, M. V. 1914 Some larval trematodes from Millport. Parasitol., 7, (1), 1-11 Lepour, M. V., and Ermurrest, R. 1922 A contribution towards the life his- tory of Parorchis acanthus Nicoll, a trematode in the herring gull, Jour. Mar. Biol. Ass. U-K., N.S., 12, 829-832 Linton, E. i Notes ona viviparous distome, Proc. U.S, Nat, Mus., 46, 551- Lixtox, E. 1928 Notes on trematode parasites of birds, Proc. U.S, Nat. Mus., 73, 1-36 Maxon, M. G., and Peourcnat, W. E. 1949 Cercariae from Upper Newport Bay. Jour, Ent. and Zool., 41, (1), 30-55 Nicoun, W. 1906 Zeugorchis ecanthus, gen. and sp, n. Ann. and Mag. Nat. Hist., 17, (7), 519-522 Nreont., W. 1907a Parerchis, n, nom. for Zeugorchis, Nicoll, 1906. Ann. and Mag. Nat. Hist., 19, (7), 128 Nicout, W. 1907b Parorchis acanthus, the type of a new genus of trematodes. Quart, Jour. Mier. Sci., N.S., 51, 345-355 Rees, G. 1937 The anatomy and encysttnent of Cercaria purpurae Lebour, 1911. Proce, Zool., Lond. 107, Series B, Pt. 1, 65-73 Rees, G, 1939 Studies on the germ cell cycle of the digenetic trematade, Parorchis acanthus Nicoll, Pt. 1, Parasito!., 31, (4), 417-433 Rees, G. 1940 Studies on the germ cell cycle of the digenetic trematode, Parorchis acanthus Nicoll, Pt. 1, Parasitol., 32, (4), 372-391 Rees, G. 1948 “ ~ A 2 2 213 SUMMARY This paper gives an account of the metamorphic and igneous history of the Rosetta Head area. Regional metamorphism of folded greywdcke and subgreywacke. types of ? Early Palaeozoic age produced quartz, biotite schists which were later intruded by granite. The conditions required for metamorphic differentiation were provided by the presence of the granite magma and andalusite, cordierite, albite and chlorite schists were formed at the expense of some quartz biotite schists, The material not wanted in these transfortnations formed andalusite chlorite and andalusite cordierite chlorite “sweats” and numerotis qttartz and quartz felspar veins, The final intrusion of the granite recrystallized and partially mobilized some of the albite chlorite schists. A mush con- sisting of coarse albites and chlorites in a mobile base, which was capable of inttttsion, was produced. This mush was pushed up along the granite-country rock contact by the intruding magma atid on cooling gave rise to coarse albite chlorite rocks of igneous aspect. The formation of the porphyritic granite of Rosetta Head and its unusual features are explained by the assimilation of albite- and chlorite-rich rocks in a potash-rich granite magma, 1, INTRODUCTION (a) Location ann PHyYSIoGRAPHY Rosetta Head is a promontory at the western extremity of Encounter Bay, on the south coast of South Australia, about 50 miles south of Adelaide. This headland—better known as “The Bluff”—juts abruptly out of the sea to a height of approximately 325 feet. The seaward end is a large granite mass intrusive into a folded sedimentary series which is now represented by quartz biotite schists. Together with West Island to the west and Wright Island, Granite Island, Seal Island, Pullen Island and Port Elliot Head to the east, Rosetta Head is part of a chain of granite masses outcropping in the Encounter Bay area. (Fig. 1 and Plate V., Fig. 1.) Glacial action during late Palaeozoic times determined much of the present topography. Rosetta Head itself is a roche moutonnée (Fig. 3.) and large areas of the rolling hills behind the headland are covered by glacial till, The glacial topography and deposits have been described and illustrated by Howchin (1926 and earlier reports listed therein). * Department of Geology, University College of Swansea Trans, Roy Soc. S. Aust., 77, July, 1954 183 The coastline features depend on geological factors. The granite mass rises as sheer cliffs from the sea, but a wave-cut platform with smaller cliffs behind has been formed where the schists form the coastline (Fig. 10). This platform has irregular and jagged features owing tu many criss-crossing veins and the cropping out of irregular bands and lenses of knotted schist. Where glacial till forms the coastline there is usually a sandy beach. [+ ]oranrtic Rocks [v ]coarse aLaire CHLORITE. ROCKS ny >} E-FROSETTA HEAD &® WEST |, 48 SEAL |. 483 PULLEN SOUTHERN Fig. 1 Locality plan showing the outcrops of igneous rocks in the Encounter Bay area. (b) Previous INVESTIGATIONS In an account of the igneous rocks-of Encounter Bay, Browne (1920) discussed the geology of Rosetta Head. The granite mass which forms the seaward face of the headland was considered an intrusive mass and part of a large batholith. The associated coarse-grained albite chlorite rock was termed an “albite mica syenite” and its origin ascribed to the flotation of carly-formed crystals during the fractional crystallization of the granite magma, . The occurrence at Rosetta Head of certain fine-grained, richly albitic and richly chloritic rocks was recorded by Browne (1920) and their forma- tion attributed to impregnation of the surrounding quartz biotite schists by magmatic material. Mawson (1926) suggested that “assimilation of the intruded schist” had taken place. The presence of “andalusite mica schist” and “cordierite mica schist” in Petrel Cove was also reported by Browne and the origin of these rocks attributed to the contact metamorphism of the quartz biotite schists. No other contributions to the geology of Rosetta Head have been published, (c} PRESENT INVESTIGATIONS The desirability of a further detailed petrological investigation firstly of the albite, chlorite, andalusite and cordierite schists and secondly of the coarse-grained albite chlorite rock was suggested by Professor Mawson who made available material previously collected from the area. The investi- gations were carried out during 1946 during the tenure of the James Barrans Scholarship of the University uf Adelaide and continued during 1947. Further field and laboratory investigations were performed during 1950-52. 184 A detailed geological map at the seafe of 20 in, =i mile was made (Fig, 2) and fifteen rack analyses and one mineral analysis were completed. The specimens referred to in the text are those of the Rock Catalogue. Department of Geology, University of Adelaide where the specimens. and corresponding thin sections are housed. The present investigations have provided evidence to suggest that the alhite, chlorite, cordietrite schists and most of the andalusite schist were formed in the aureole of the intrusive granite by contact metasomatism of the country rock (quartz biotite schist). The metasomatism was not due to offshoots of the granite penetrating the country rocks but due to the presence of the requisite conditions to cause metamorphic differentiation. There is no evidence to suggest the flotation of crystals to giye rise to the coarse-grained albite chlorite rocks but the evidence indicates thit these unusual rock types were formed by the partial or complete mobilization of albite chlorite schists by the intrusion of the granite. The granite over- rides the country rock and the coarse albite chlorite rocks are mainly found along the main granite-country rock contact. The unusual features of the granite are explained by the assimilation of albite- and chlorite-rich maternal, This paper gives an account of the metamorphic and igneous history af the area with particular reference to the genesis of the fine-grained albite chlorite schists and the coarse-grained albite chlorite rocks of igneous aspect. If. REGIONAL SETTING AND STRUCTURE (a) Recionar, SETTING Investigations in south and south-eastern South Australia have revealed Numerous occurrences of coarse-grained granite. Outcrops at Cape Wil- loughby, Kangaroo Island (Tilley 1919), in the Encounter Bay area (Browne 1920) and in various parts of south-eastern South Australia (Mawson and Parkin 1943, Mawson and Dallwitz 1944, and others) have heen described, but most of these outcrops are either granite islands or completely surrounded by Tertiary or Recent deposits. At Rosetin Head, however, the intrusive nature of the granite can be established, the intruded country rock being a quartz biotite schist, very similar to the unaltered xenoliths in the granite at Granite Island and Port Elliot. Howchin (1926) showed that this country rock is portion of the upper part of a sedimentary series which rests uncomformably on the schists and gneisses of the Barossian Complex (Older Precambrian). This country rock, which is largely composed of recrystallized greywackes and subgreywackes together with some argillaceous and same arenaceous horizons, is well developed and exposed on the south-eastern und eastern flanks of the Mount Lofty Ranges. In general it has been metamorphosed to the biotite grade although in some areas metamorphism has been more intense. Its age and stratigraphic position have not been definitely determined. Howchin (1926, 1929) heid that this series corresponded to the Adelaide System found on the western flank of Mount Lofty Ranges but Mawson (1947) suggested that it was of Mosquito Creek Age, Recent investigations by the South Australian Geological Survey have suggested that these rocks are part of the Kanmantoo Series and are of ? Early Palaezuic age.) A general account of the regional distribution of this series together with the nature and composition of some of the rock types has been given by Robinson (1946), Owing to the presence of overlying irregular patches of Permian gtacia! till, it is mot posstble to trace a continuous sedimentary succession from Rosetta Head inland, but Howchin (1926) has published a geological map ©) This statement is published by kind permission of the Director of the Geological Survey of South Australia, 185 NYSHLNOS 4S1HO5 aliLom Zuoyno WoAasNni PA Px Fs uaiNnoons ANDRA ALISOASIHIS oniaaag M320" OSTSAIYNY 0856 SNWLesAVEL BYANTY v= alinvad DiLitAHdHOd | pDOW Fu1eCTHO ah wens, ] ALi 384vOo ex SUStH3S BLOW ¥ SLlal SHIGA IL) — hia EJ "sargadeco’ 3LiSN1¥ONY Law a4wa108 aA igtHos JAuoI@ ZLEvNO [4] VIWYLSNY HLNOS GQ¥V3H ViLasou 30 dAVW 1V9I5O01039 ASIHDS ZLu01e Eon HSLNNGOING , 44 —5 a 2 ‘Old 186 of a large area north of Encounter Bay and has described glacial deposits. Apart from recent superficial deposits, these represent the last episode of sedimentation in the area, {b) Structure The regional structure of the metamorphosed sedimentary series making up the country rock is simple, From the base of the series some ten miles inland, the beds dip regularly towards the south-east at moderate angles, and can be traced in ascending stratigraphic order towards the sea. Close to the granite intrusion at Rosetta Head the strike varies from N.50°E. to N.60°E and the dips vary due to folding (Fig. 2). Fig. 3 Rosetta Head from: the Encounter Bay shore illustrating the distribution and relationships of the yarious rock formations. Outside the contact metamorphic aureole but close to the headland, bedding is a conspicuous feature. Slumped structures, one inch high, are sometimes seen along the bedding planes as in the cliff at the side of the road two hundred yards from the wharf, Regional: cleavage, which cuts across the bedding and which is post-folding is a prominent structural feature especially on the wave-cut platforms (Fig. 10 and Plate V,, Fig. 2). Behind the headland the plane of this schistosity strikes N.25°E and dips 70° southerly. It swings gradually to N.35°E near Half Way Rock but the dip remains constant, The general direction of the granite-country rock contact and also of the line joining the contact at Rosetta Head to the contact on Wright Island is approximately that of the strike of the plane of schistosity. Withia the area affected by contact metamorphism the bedding is difficult to detect but the schistosity is a prominent structure. Bands, masses and lenses of knotted andalusite and cordierite schist and light-coloured albite chlorite schist are also conspicuous. Although showing no apparent structural control the bands generally bear about N.50°E. They cut across and destroy both the schistosity and the bedding. Their presence, together with numerous associated veins and stringers has resulted in a very confused structural pattern on parts of the wave-cut platforms. The dip of the country rock near the granite contaet is approximately 3S°S.E, (i.e. out to sea) and this is the dip of the main granite-country rack contact, the granite having overridden and intruded over part of the country rock (Fig, 3). It appears as if the magma stoped its way up the dip during its intrusion, the bedding exercising a structural control. The frontal advance of the magma appears to have been structurally controlled by the schistosity as the direction of the main contact corresponds with the strike of the achistosity. A vague lineation in the granite parallel to this direction is shown on the aerial photograph. Roof pendants have not been moved as the orientation of the schistosity and bedding remains the same, but xenoliths of country rock, which are common, are disoriented. 137 The granite is cut by several major joint systems which show close rela- tionship to thuse of West Island (vide Jack 1923). Of the major joint systems one system strikes N-S and dips 20°W. but the others are verttcal or nearly so and strike N.10°E, N.40°E., S.70°E, and S. 40°E. respectively. Ti. THE COUNTRY ROCKS The country rocks are part of an extensive series now represented by recrystallized greywackes, quartz biotite schists and impure sandy quartaites found on the south-eastern and eastern flanks of the Mount Lofty Ranges. Most of the rock types are dense, fine-grained, dark-grey and composed essentially of quartz together with biotite. They are generally massive except for some areas where the parallel orientation of some of the biotite has produced a schistosity, The age and stratigraphic position of this series has heen discussed in the previous section and Robinson (1946) has recorded descriptions of the main rock types. The composition of the upper part of the series shows little variation 4s is indicated by Kleeman (1937) who, in discussing the origin of the xeno- liths in the granite of Granite Island states that the “granite was intruded into a large area of hornfels of fairly uniform composition. The rocks are well exposed in hills just north of Rosetta Head and to the north of Victor Harbour itself,” Two miles inland from Rosetta [lead the country rock is massive, muicaceous-looking and almost black in colour with no traces of schistosity (Browne, 1920). Owing to overlying patches of Permian glacial till, it is not possible to trace a continuous series towards Rosetta Head, but within the area mapped the country rock is a dark-grey, fine-grained quartz biotite schist. It consists essentially of quartz and biotite, in varying proportions together with minor amounts of felspar and muscovite and accessory mag- netite, apatite and zircon. Some of the biotite flakes show parallel orientation and, in general, the degree of schisiusily tends lo increase as the headland is approached. (a) PeTrocrapuy The country rock outcropping by the coast at the side of the road in the most northern part of the area mapped (Fig. 2) is a dark-grey, fine- grained quartz biotite schist (9590). It consists essentially of uncracked grains of recrystallized quartz, varying considerably in grain size (from 0:25 mm. to 0:05 mm.}, which form a mosaic in which the less abundant minerals are dispersed, together with brown biotite flakes (Fig. 4a). Some of this biotite is present as short stumpy flakes but most of the individuals are long (up to 1-2 mm. with ratio of elongation 4:1), show parallel orienta- tion and are pleochroic with x=light yellow. y—=2z—=dark brown. Some orthoclase, towards which the quartz is idioblastic, is present together with a few crystallized grains of albite (Ab,,). There are a few stumpy muscovite flakes, magnetite is fairly abundant, zircon, apatite and tourmaline less so, This rock ts a greywacke type which has been metamorphosed and is repre- sentative of much of the surrounding area. Its chemical composition is set out in Table 1, Approaching the headland the schistosity tends ta become more pro- nounced and the size of some of the biotite flakes increases. Two hundred yards from the granite contact the rock (9591) in the cliffs by the road leading to the wharf has a pronounced schistosity and consists of vague, discontinuous bands about i mm. across which are alternately biotite-rich aud biotite-poor, the biotite fakes generally being 0°35 mm, in length (Fig. 4b). Recrystallized quartz grains together with minor amounts of orthoclase, 188 albite, muscovite, magnetite, apatite, zircon and tourmaline make up a mosaic which is practically even-grained with an average grain size of 007 mm. This rock represents a belter-sorted, more argillaceous sediment than the rock previously described but the more pronounced schistosity suggests that stress was a more important factor in its metamorphism than int the case of the rock further inland. The chemical composition of this rock is set aut in Table Ll, (a) Quartz biotite schist (9599) x 27, with accessory zireda and magnetite. (b) Quartz biotite schist (9591) x 27, (c) Quartz biotite andalusite schist (9593) x 6, showing relics of schistosity in the andalusite porphyroblasts and a large chlorite flake which cuts across the schistosity. Claser to the pranite mass the rocks show a weaker schistosity and the texture becomes decussate. A few yards from the granite, in the roof pend- ant just south of the wharf, the country rock (9592) is a quartz biotite hornfels although a few biotite Hakes showing preferred orientation are still present. Most of the biotite shows randotm orientation and together with an equigranular mosaic of recrystallized quartz grains (average prain size 0°15 mm.) makes up the decussate texture, The chemical composition of this rack is given in Table 1 and this, together with microscopic observations indicate that it is stmuilar to rock 9590 in mineralogical and chemical com- position although it represents a better-sorted sediment and has undergone contact metamorphism following regional metamorphism, Close ta the margin of parts of the granite mass, 2 natrow zone, up to fen feet wide, of banded quartz biotite schist has been produced. This is well shown on the north-western side of the headland where tts schistosity is paralle), in detail, to the pranite-schist contact, The regional schistosity has been obliterated in these areas and the directional features of this con- tact schist often cut across it. In various parts of the area there ts local develapment of sericite, mus- cavite, andalusite and chlorite. Knots of very fine sericite, irregularly developed over a limited area some 480 yards from the contact arta were reported by Browne (1920 p, 53). Some muscovite is also present. The schistosity, which curves around-the knots, is very marked, A spotted anda- lusite schist (9593) crops out next to the granite mass, just west of the albite chlorite schist near the wharf (Fig. 11). It is distinctly schistos¢ and is made up of alternate bands respectively rich in parallel oriented biotite and granu- lar quartz. The schistosity curves around clear eye-shaped crystals of anda- 189 lusite which are practically free from inclusions (Fig. 4c). Browne (1920) also reported the sporadic occurrence of rocks containing a few large flakes of green chlorite that cut across the schistosity although small quartz inclusions carry the schistosity through the chlorite flakes. (b) SEDIMENTARY VARIATIONS AND CHEMICAL COMPOSITION The country rocks in the immediate vicinity of Rosetta Head are now composed essentially of quartz and biotite in varying proportions with compositions ranging from subgreywacke to argillaceous greywacke. This is borne out by the chemical compositions of the analysed rocks and a comparison with the average composition of greywacke (Table 1). The variation diagram (Fig. 5) shows that Al,O,, total Fe, MgO, CaO and K,O increase as Si O, decreases. This. reflects the inverse relations of quartz and biotite. Felspar is never present in large amounts. Often it is mainly potash feldspar although albite is usually present as indicated by the Na,O content of the analysed rocks. The norms of the analysed rocks are given in Table 2. Taste 1 Analyses of the country rocks and comparisons with greywacke A B Cc D E F G 510s wre, eee ens “O8B2 63-55 68°76 68-92 72-90 64-2 68-1 TiO ee ee O96 0-86 0-74 0-88 0-56 0°5 0-7 AbOs oo... a. 18°34 16-55 13-79 © 12-65 13-74 14-1 15-4 FesOe on ves vee 096 0-97 0:66 1-60 0-04 1-0 3450 FeQ vac) atin en 5895 4-67 4-60 5:07 3-29 4-2 34 MnO oa ae ee 0°05 0-09 0-07 0-02 n.d. O-1 0-2 MeO 2. ue ee 400 3*12 2°65 2-52 1-85 2-9 1-8 C20 taee pose dat SSS 311 2-81 2:06 2:12 35 2-3 NasO wn a. a = 339 3-33 2-54 2-80 3-02 3-4 2-6 K:0 ieiap wore ees, SON 2S 3-24 2°29 2:10 199 2:0 2-2 HaO+ a ae ae 027 0-50 053 0-96 0-46 2-2 2.1 H,O-(110°C.) 1... 0-10 0-10 0:04 0+04 0-11 POs ee ee = OD 0-19 0-21 0-17 0-15 0-1 02 ZrOy ns ee ee 005 tr. 0-19 = p.n.d. n.d. — — BaQ ne se 0050058 A OO nd. = 3 SB ae cuee el! bee AP 0+19 0-13 0-18 tid, _ _— C Os eee aes tare —, ay _— = — 1°6 = 99-95 100+52 100-15 99-98 100-23 100-0 102°4x LessO .. ws © 0-01 0-08 0-05 0-07 — = _— for S ee eee eee eee CC 99-94 100-44 100-10 99-91 100-23 100-0 102-4 x Probably in error; FesQ. probably should be 1-00 and the total 100-0. Quartz biotite schist (9591) in cliff by road, 200 yards from wharf, Rosetta Head. Analyst: D. R. Bowes, Inclusion on Breakwater, Granite Tsland, Victor Harbour, Analyst: A. W. Kleeman, (Kleeman 1937). Quartz biotite schist (9590) by coast at side of road, half mile north of Rosetta Head. Analyst: D. R. Bowes. Quartz biotite hornfels (9592) in toof pendant south of wharf, Rosetta Head. Analyst: D. R. Bowes. Sedimentary inclusion, Breakwater Quarry, Granite Island, Victor Harbour. Analyst: A. W. Kleeman (Kleeman 1937), Average of greywacke analyses given by Pettijohn (1949, p, 250), Average of 30 preywackes. Compiled by Tyrrell (1933, p. 26). > Ons tM Do & 190 TABLE 2 Norms of the country rocks A B Cc D E Quartz sue sets wre nee O15 18+36 32-52 34°14 38°76 ‘Orthoclase ce ee ones | 19°46 18:90 13-34 12-23 11-68 Albite (ee eevee pees 2B4B2 28°30 21°48 23°58 25°15 Anorthite 0 a ae oe 16°96 14-18 13-34 9-45 9-73 Corundum wn. ase es ene 2486 2°35 2-24 2°45 3-06 Zircon ay ed ete ane MTB — 0°37 — _— Hypersthene—En 10-00 7°80 6°60 6°30 4-60 i Fs ou. a = 8°51 6:07 6-60 6:20 §-15 Magnetite ws. wn ae ee 159 1-39 0-93 2°32 — Iimenite suse! Gare tyerh oe | DBZ 1-67 1+37 1-67 1-06 Pyrite oo. a a eee O12 0°38 0-24 0-30 _ Apatite bdo power pom. “ans O94 0-44 0-34 0-34 0-34 A study of the thin sections and chemical compositions of the rocks, together with the variation diagram, confirms that no minerals except quartz and biotite are present in large amounts. The rocks described and analysed are representative of the country rocks and show the extent of the minera- logical and chemical variations in the immediate vicinity. Variations in the conditions during deposition are reflected by changes in grain-size, Some of the rocks are even-grained and well-sorted although many are uneven-grained and ill-sorted with the quartz individuals varying considerably in size, FIG.5 VARIATION DIAGRAM OF ANALYSES OF o x 1 o E ae R f T ae CST (c) METAMORPHISM Two separate episodes of metamorphism are recorded by the courtry rocks in the area. The first episode was one of regional metamorphism which took place after the folding but before the intrusion of granite and which changed the sediments to quartz biotite schists. Shearing stress appears to have played only a minor role in the metamorphism of the rocks inland, as evidenced by their lack of recognizable schistosity, but as Rosetta Head is approached shearing stress became a more important factor and the biotite shows parallel alignment. All the rocks have been completely recrystallized and metamorphism reached the biotite grade. 191 The second episode was one of contact metamorphism resultant upan a magmatic invasion of the area. Close to the granite contact the schistosity becomes less prominent and, in parts, a hornfels was produced indicating that heat was the dominant factor. The final emplacement of the granite mass at Rosetta Head must have been atcompanied by some shearing stress as andalusite quartz schist and banded qnhartz biotite schist are found in parts immediately adjacent to the granite. Andalusite, cordiecrite, albite and chlorite schists were also produced during the phase of contact meta- morphism but as their formation involved a considerable addition and re- moval of material, their genesis is discussed separately in the next section. It is possible that the local development of knots of sericite, muscovite and chlorite previously described may represent an early stage in these metaso- matic alterations, IV. THE ANDALUSITE, CORDIERITE, ALBITE, CHLORITE SCHISTS Rocks characterized by knots of andalusite or cordierite, wthers by masses of white albite grains and yet others by the abundance of interwoven chlorite flakes crop out extensively in parts of the area and their presence was recorded by Browne (1920). Rocks containing knots of both andalustte and cordierite are not common, although these two minerals, together with quartz, are associated in smal! irregular veins and lenses. Albite and chlorite are commonly associated with each other and together with andalusite or cordierite. Irregular stringers of fine-grained quartz and felspar and veins of coarse andalusite transect some of the schists and associated country rocks. (a) Distrinution anb FIELD RELATIONS These schists occur as bands, lenses and irregular masses and are dis- tributed sporadically on the wave-cut platforms and close to the main granite contact. There is no regular distribution of any of these types. Generally they cross-cut and obliterate hath hedding and schistosity (Fig. 2) and are observed to have replaced the country rock to give a rock having little or ne directional features. They are best studied in two main localities. (1) Wave-cut platform west of Rosetta Head Knotted andalusite and cordierite schists, as well as light-coloured, granular albite-rich schists crop out in Petrel Cove and to the west (Figs. 2 and 10). They mainly occur as long, narrow bands which generally bear about N.50°E, and thus cross-cut both hedding and schistosity, although a few do run parallel to the schistosity, The bands are not very regular and do not follow one direction continuously although many are approximately parallel toa prominent joint plane of the country rock, Small lens-shaped masses of schist also outcrop and relic lenses of country rock are sometimes found in the schist outcrops. _ The knotted schists and albite schists are readily distinguished from the prey schistose country rock by the jagged nature of the weathered surface (Plate V.. Fig. 3), andalusite and cordierite forming the knots, and by the light colour respectively, but because of their intimate relations and grada- tions it has not been possible to separate these types in mapping. Some of the bands and’ lenses show sharp boundaries which generally cut across both bedding and schistnsity, but many grade out into the country rock as indi- cated by the gradual disappearance of the knots or by the gradual change from the white of the albite schists ta the grey af the country rock, West of Half Way Rock veins and lenses of pink andalusite occur. They are short and have sharp baundaries, There are also irregular veins and masses of coarse-grained rock consisting of knots of blue cordierite (up to 192 half inch across), masses of pink andalusite, colourless anhedral masses of quartz and greenish flakes of chlorite which wrap around the other minerals, These tocks are not regularly distributed and are only of limited occurrence. (2) Chi near wharf Irregular and interlocking masses of white albite schist and green chlorite schist make up a large part of the cliff face just south of the wharf (Fig. 11). “Veins” of chlorite which have no simple, regular shape and no constant direction cut across the albite schist. Their presence, together with the presence of irregular veins and masses of coarse albite chlorite rock (Fig. 12) and veins of granite give the cliff face a very heterogeneous appearance. No knotted schisig are present in this area Normally the boundary between the albite-rich and chlorite-tich rovks is sharp, but in some cases the contact appears a3 a series of distinct steps. The ratio of albite to chlorite in these rocks varies, and all types from albite-rich to chlorite-rich schists are found. The boundary between these schists and the grey schistose country rack appears sharp and cuts across the bedding and the schistosity, both of which generally have been obliterated. Some fine parallel banding is, how- ever, sometimes shown in the albite schists, due to the oriented growth of smail green chlorite flakes along original bedding planes. The disposition of these relic bedding planes corresponds with the bedding in the country rock near the main grantte contact and also that seen in the roof pendant south of the wharf. (3) Other localities Knotted schists crop out on the wave-cut platform on the eastern side of the headland but they are neither as abundant nor as prominent as in Petrel Cove and to the west. The rocks are cut by numerous thin, criss- crossing quartz felspar veins together with some barren quartz veins. Small outcrops of albite chlorite schist are found along the main granite- country rock contact (Figs. 2, 10 and 11). In almost every instance they are separated from the granite by masses of coarse albite chlorite rock elongated parallel to the contact, The small patch of albite chlorite schist between the country tock and the coarse albite chlorite rock on the landward side of the S.W. Tip (Fig. 9) shows the gradual transformation of the country rack to albite chlorite schist (Plate VI., Fig. 1). This transformation is best seen near the southern boundary of the roof pendant south of the wharf and is described in the following section. Small patches of albite chlorite schists also crop out amongst the country rock. A mass of chlorite schist is found on the S.W. Tip of the headland (Fig. 9), It resembles the chlorite sthist near the wharf, but t5 coarser grained. {b) Country Rock — Auxerre Cauorttr Scuisr TRANSFORMATION The transformation of the grey country rock into a white albite chlorite schist is shown about eighty yards south of the wharf near the southern boundary of the large roof pendant. Over a distance of twenty-four feet the tock grades, across the strike, from a grey hornfels, through light-grey schists in which albite and chlorite have developed, into a light-coloured albite chlorite schist. The country rock, a quartz biotite hornfels (9592), has been described (p. ). With the gradual growth and increase in amount of small individuals oY albite and flakes of light-green chlorite the character of the rock changes, Initially the chlorite developed as. thin wisps aligned along. the original bedding planes, The biotite, which decreased in amount remained randomly 193 oriented together with some larger chlorite flakes. Small grains of albite became abundant but quartz decreased in amount (9594). With the continued trans- formation there was a further decrease in the amount of quartz and biotite and a corresponding increase in albite and chlorite, flakes of the latter being larger and generally showing no alignment (9595), Flakes of muscovite are more common than in the country rocks and so are zircon, apatite and tour- maline. Finally the rock was transformed to an albite chlorite schist (9596) similar to those described in the following section. This transformation involved a considerable increase in albite, chlorite and rutile together with a decrease in quartz and the almost complete dis- appearance of biotite. Chemical analyses of these rocks set out in Table 3 reflect the mineralogical variations and show the progressive decrease in SiO, and K,O together with the increase in Na,O, MgO, H,O and A1,Q,. These chemical changes are graphically set out in the variation diagram, Fig. 6, TasLe 3 Analyses showing the country rock—albite chlorite schist transformation A R Cc D E SiOe ae ee cee um tee = 68492 60-07 58-45 56-39 58-63 TID: ae tee ee BB 0:96 1-03 0-92 0-73 Al sue eee cee eee eee TBS 17-65. 18*40 18-00 20-10 Fe:Os iad fied tetris «E60 1:29 0-94 2-04 1-01 FeO sade “¥en elgep wide) deed POE 5-50 5°65 4-00 2-08 MnO ye eee cee ee ee = O02 6-05 0-03 0-04 0-04 MeO a eee oe ee ee 25 3+95 4-09 8-14 6-15 CaQ oa aa am ee ue | 206 2°22 2-63 1+29 1-09 NaQO et ee eee | 2 BO 3°88 4-44 5:36 6°95 K,0 Joss -teset vtpen itpee asap “BAG 1/89 1-78 0r15 0-16 HiOF eee ee 096 2+20 2-20 2+96 2°34 HsO-(110°C.) ee O04 0+07 0-12 0-11 0-06 PaOe sass vet tte sete cae O17 0-16 0-15 0-22 0-20 ZrOe wee eee tee nee cae DEL, 0-30 020 0-11 0:22 BaQ ae ey te ee ee O01 0-08 0+08 0+20 0-04 SY dues hie ner pet ane ver Alto 0-16 0-08 0+13 0-11 99-98 100+43 100-27 100-06 99-91 Less O fot S 4. ae ne = 0°07 0-06 0-03 0-05 0-04 99-91 100 +37 100-24 100-01 99-87 A. Quartz biotite hornfels (9592) in roof petidant south of wharf, Rosetta Head—24 ft. north of schist—coarse albite chlorite rock contact. ; Analyst: D. R. Bowes. B. Quartz albite chlorite schist (9594), 18 ft. north of contact. Analyst: D. R. Bowes. C. Quartz albite chlorite schist (9595), 12 ft. north of contact. Analyst: D. R. Rowes. D. Albite chlorite schist (9596), 6 ft. north of contact, Analyst: D. R. Bowes. E, Coarse albite chlorite rock (9614), 24 ft. souith of contact. Analyst: D. R. Bowes. rs An amalysis of the coarse albite chlorite rock (9614) found between the albite chlorite schist and the granite is also given in Table 3. This shows the similarity in composition of the albite chlorite schist and the coarse albite chlorite rock. FIG.6 VARIATION DIAGRAM OF ANALYSES OF o x t i p | e R ¢ f t (c) PETROGRAPHY ANB CILEMICAL COMPOSITION For the pttrpose of description it 1s convenient to divide these schists into two main groups: (I): those characterized by the presence of andalusite and/or cordierite and (2) those characterized by an abundance of albite and/or chlorite. This grouping to a large extent separates those types found in Petrel Cove and to the west from those that crop out near the granite- country rock contact, éspeciully at the cliff near the wharf. Detailed rock descriptions are omitted where they haye been recorded by Browne (1920). (1) Andalusite and cordierite schists The knotted andalustte schists consist of irregular andalusite individuals, which show sieve texture and are crowded with minute inclusions of quartz and Hmenite, together with abundant smaller grains of quartz and flakes of biotite, chlorite and muscovite. Some of the micaceous minerals show a preferred orientation. In parts they curve around the andalusite knots, which are up to 3 mm. across, but in other parts the andalusite has grown at the expense of these minerals. Small knots of sericite, showing features similar to the andalusite, are found in same of the rocks. Much of the chlorite, with which. rutile is invariably associated, is intergrown with biotite, some of which has a bleached appearance. Veins and lenses consisting essentially of andalusite and chlorite are found west of Hali Way Rock (9597). The large andalusite crystals are irregularly cracked and contain abundant inclusions while the chlorite occurs as fakes and rosettes (Fig. 7a). Large and smal! clear colourless masses of quartz are also present together with biotite Hakes, zircon and ilmenite. The texture is variable; it is usually coarse but sometimes fine-grained with an andalusite, biotite, quartz mosaic. Roundish patches of blue cordierite, up to 1 cm. across are sometimes found in these masses and veins (9598), some of which now consists of a mosaic of quartz and biotite together with small crystals of andalusite and cordierite, The knotted cordierite schists consist of irregular roundish patches. of inter- locking cordierite crystals, sometimes up to 1 cm. across and either bluc or 195 brownish-yellow in colour, in a fine-grained somewhat schistose base, The knots show some traces of a preferred orientation parallel to the schistosity of the base. In thin section (9599-9600), they are seen to be composed of interlocking crystals, alk im optical continuity, fell of inclusions of quartz, zircom, chlorite, biotite, muscovite and rutile giving a micro-sieve structure, and with ragged boundaries which are frayed out into the fine-grained groundmass (Plate V., Fig. 4). This groundmass is usually made up of irregular laminae of fine granular quartz and albite alternating with laminae of parallel oriented biotite flakes. Larger biotite chlorite and muscovite flakes are present; some of these cut across the schistosity while others sweep around the cordierite patches. There is a concentration of zircons (all surrounded by pleochroic haloes) in these biotile flakes and a concentration of red-brown prisms of rutile in the chlorite. The groundmass in some of the rocks shows neither laminae nor schistosity and is a mosaic of quartz, biotite and albite together with some larger biotite, chlorite and muscovite flakes and some larger quarta individuals. The size and relative concentration of the cordierite patches varies considerably. Half of some of the rocks are made of cordierite knots, but in others they are not as common or as Jarge. The grain-size of the groundmass also varies appreciably amongst the rocks of this group. There is no microscopic evidence in either the andalusite or cordierite schists on which to base the order of formation of the constituent minerals. It appears that all these minerals were formed during the same period and in no particular order, A chemical analysis of a knotted cordierite schist (9599) is given in ‘Fable 4 and this indicates the relatively high proportions of Al,O, and MgO and, the dominance of Na,O over K,O in these rocks and the differences in their composition compared with that of the country rocks. (Table 1). "FABLE 4 Analyses of the cordierite, albite, chlorite schists A B Cc Dp E F SiOs 58-75 58-91 56-39 46-39 44-33 43°81 TiOy .... 0-70 0°85 0-92 1-28 1-10 1+33 AlLOs wee 20048 21-37 18-00 21-94 16-94 24-60 FesOs . 063 0-82 204 0-65 402 1-20 FeO ..., ‘rt 3-97 1-90 4-00 $-95 4+35 5:14 MnO rt 0-03 0-03 0-04 0-09 0-08 0-08 MgO we = «793 4-50 814 11-61 16-17 12-74 CaQ aw «1578 0-78 1+29 1+28 0-70 0°53 Nav sey ates eee 3+35 8-72 5°36 4-53 1-17 1-80 K,0 1:97 0°16 0-15 O52 4-62 2-62 H,O+ site aat 1-43 1-47 2:96 5+39 4-24 5-74 HyO- (110°C.} 0-15 0-06 O-13 0-05 0-88 O17 PaO. ete mee ee = G60 Q-21 +22 0+23 0-31 0-32 ZrO— os 0-21 0-04 0-11 0-04 0-12 0:08 Bam ee tm 0-13, O13 0-20 0-05 012 0-17 5 «OS 0-06 G13 0-02 0-t5 0-06 F er oom — — _ 0701 . —_ _ LisO ot _ = _ — abs —_ 100-24 100-01 100-06 100-03 99-90 100°39 Less O for S&F... 0°06 Or 6-05 0-01 0-06 0-02 100-18 99-99 100-01 106-02 99-84 100-37 196 A. Cordjerite schist (9599) on wave-cut platform at west side of Petre) Cove. Analyst: D. R. Bowes. . Albite schist (9601) in cliff by wharf, Rosetta Head. Analyst: D. R. Bowes. . Albite chlorite schist (9596) in roof pendant south of wharf, Rosetta Head —6 ft. north of schist-coarse albite chlorite rock contact, Analyst: D, R. Bowes. D. Chlorite albite schist (9605) adjoining coatse albite chlorite rock vein (9606) in cliff by wharf, Rosetta Head. Analyst: D, R. Bowes. E, Chlorite schist (9609) in cliff by wharf, Rosetta Head. Analyst: D. R. Rowes, F. Chlorite schist (9607) in cliff by wharf, Rosetta Head. Analyst: D, R, Bowes, (2) Albite and chlorite schists White albite grains and green chlorite flakes occur together in all pro- portions in these rocks, which show all gradations between an albite schist and a chlorite schist. The albite in all these rocks has a composition of Ab,, and has the same composition and optical properties as the larger albite individuals of the coarse albite chlorite rocks, the mineralogy and chemistry of which ate discussed later (p, 203 and Table 6). The chlorite is the same as that found in the knotted schists and in the coarse albite chlorite rocks. An analysis of this mineral given in Table 5 indicates its richness in MgO. The mineral is biaxial positive with a small optic axial angle (2E —10°) and weak birefringence. It is characterized by the presence of many minute crystals of rutile up to 0-1 mm, in length and the TiO, of the analysis should be allotted to the rutile and not the chlorite. The derivation of much of the chlorite from biotite is suggested by the apparent gradations from brown biotite to a bleached biotite and finally to chlorite with abundant rutile inclusions. Tape 5 Analysis of chlorite SiOs oc. ee tee eee GOST Na.Q wee cer gee 46 + i a BE 7 FeO 2k ee OS AlOs wee tee ane 22! BZ H:0+ Au am ane BSS Fe,Q. Te, ce eanmis 0-21 H.O- Week he wee DNril FeO a. anu wee oe 11-39 PuOs oe 6 ae TTR MgO fin ter eee 2G CaO vn. ne aye | O55 Total ... 98'65xx « The TiOs of the analysis should be allotted to rutile crystals included in the chlorite flakes. xx Low total probably due to low H:O determination. Analysis of chlorite from chlorite schist in cliff by wharf, Rosetta Head- Analyst: A. W. Kleeman.@) The albite schists are dull white in colour and consist essentially of a fine- grained mosaic of both twinned and untwinned albite (Ab,,) and quartz together with small chlorite flakes and accessory rutile, zircon, apatite and biotite (Fig. 7b.). The average grain size is 0-1 mm. although the grain size varies as does the composition. Chlorite is sometimes more abundant in certain bands and in parts there are lenses and irregular segregations of larger quartz crystals and chlorite flakes, Thin stringers of chlorite, biotite and muscovite cut these rocks and small pockets of chlorite and muscovite are sometimes present. No rocks consisting wholly of albite haye been dis- covered; some chlurite is always present. An analysis of an albite schist (9601) is set ott in Table 4. ©) Published by permission of the analyst. 197 With an increase in the proportion of chlorite and a decrease in albite, the rocks become albite chlorile schists which are fine-grained and usually banded (9596, 9602), They consist of irregular wavy bands of chlorite flakes (up to 2 mm. long) and anhedral quartz individuals with ragged edges alternating with finer grained bands of albite (Ab,,) and quartz together with smail chlorite and biotite flakes, Rutile is an abundant accessory; zircon, apatite and brown tourmaline are also present. Au analysis of an albite chlorite schist (9596) is given in Table 4. With a further jnercase in the amount of chlorite and a decrease in albite, the rock becomes a chlorite albite schist, many of which are patchy (9603-4), Long chlorite and muscovite flakes make up part of the rock, These wrap around fine-grained masses consisting of alternating bands of parallel-oriented chlorite flakes and granular albite and quartz. The relative abtindance of the larger chlorite and muscovite flakes as compared with the fine-grained banded part varies considerably amongst rocks of this group, as does the proportion of each mineraJ. Biotite is sometimes present with the chlorite and muscovite and often with chlorite alone, but lhe predominant mineral is abways chlorite. Yeins of randomly oriented chlorite fiakes, up to 1-5 mm, in length, together with anhedra! quartz containing small chlorite inclusions sometimes transect these rocks, (a) (b) (c) Fig. 7 {a} Andalusite chlorite vem (9597) x LI. ; ; P (b) Albite schist (9601) x 27, with fakes of chlorite, which include rutile prisms, and grains of magnetite. (c) Chlorite bwwtite schist (9608) x 11, with large muscovite flakes, In the cliff near the wharf a chlorite alhite schist (9605), the chemical composition of which is set out in Table 4, is cut by a vein of coarse albite chlorite ruck (9606) (Plate V1., Fig. 2). This schist consists of smal! chlorete flakes oriented parallel to the edge of the vein in association with a fine- grained mosaic of pellucid untwinned albite (Ab,,) and some quartz. The chlorite schists (9607 -9) are green foliated, crenulated rocks consisting of parallel oriented Makes of green chlorite and brown biotite, the average length of the flakes being 0-5 mm. and the ratio of elongation 6:1, Chlorite is generally the predominant mineral although in some of the rocks it is subordinate to hietite, Some muscoyite is usually present. Between bundles of flakes of the micaceous minerals are areas of a fine-grained mosaic of quartz together with a small but variable amount of alblte (average grain 188 size 0°08 mm.} and accessory rutile, apatite and zircon (Fig. 7c), Analyses of two chlorite schists are set out in Table 4, A comparison of the analyses of these albite and chlorite schists (Table 4) with the analyses of the country rocks (Table 1) reveals marked differences in chemical composition. The high proportion of Na,O associated with the low proportion of K,O in the albite schists and the high proportion of MgO in the chlorite schists are distinctive features of these rocks and are far from the corresponding values for the country rocks. Fi6.8 VARIATION DIAGRAM OF ANALYSES OF The mineralogical dominance of albite, the scarcity of biotite and the presence of some chlorite in the albite schists is reflected in the relatively high amount of Na,O, the small amount of KO and the presence of MgO in considerable amounts. As the rocks becotme more chloritic the amounts of Na,O and SiO, decrease while K,O increases as do H,O and MgO, the latter constituent to a very marked degree, This reflects the gradually diminishing amount of albite, the increased Proportion of biotite and the mineralogical dominance of chlorite. The proportion of TiO, present shows the greater amount of rutile present in the chloritic rocks as compared with the albitic types. These chemical changes are graphically represented in the variation diagram, Fig. 8. (d) Genesis Field evidence shows that the parent rock of these andalusite, cordierite, albite and chlorite schists was the quartz biotite schist of the country rock, Gradations from quartz biotite schist to albite chlorite schist south of the wharf have been described (p. 192) and similar gradations, both along and across the strike, can be seen at the boundaries of many of the albite chiorite schist masses on the wave-cut platform west of the headland and at the main country rock-albite schist boundary at the §.W, Tip as illustrated in Plate VL, Fig. 1. Relics of quartz biotite schist remain within some of the albite chlorite schist masses although these relics usually consist of an tinaltered core, with schistosity corresponding with the general schistosity of the country rocks, and a periphery which grades aut into the albite chlorite schist. Gradations: from quartz biotite schist to knotted andalusite and cordierite schist are also shown at the boundaries of many of the knotted schist masses on the wave-cut platforms and also at the boundaries of relics of quartz biotite schist within them. As the gradation takes place, sa the proportion of knots of andalusite or cordierite increases. 199 These bands and masses of andalusite, cordierite, albite and chlorite schist generally cut across and destroy the bedding, so that their unusual com- positions cannot be due to original sedimentary bands of tinusual composition. "They also generally cut across and destroy the regional schistosity indicating that their formation was after the regional metamorphism which was respon- sible for the formation of the quartz biotite schists and the regional schistos- ity. Their distribution is related to the granitic rocks of the area. To the north and north-west of the contact zone of the granite at Rosetta Head the country rocks contain no masses of andalusite, cordierite, albite and chlorite schists, but to the west of the granite outcrop there is a concentration af these rocks which becomes Jess intense west of Half Way Rock. Half a mile further west none of these rocks is seen. This asymmetric arrangement around the outcropping granite mass suggests that these rocks were prodaced in the aureole of an underlying granite mass which fed the over-riding in- trusion at Rosetta Head at a late stage in the general process of its emplace- ment. The small mass of granite now exposed produced a small zone of contact schists but, in general, it modified rather than was responsible for the main contact metamorphic changes. The production of andalusite, cordierite, albite and chlorite schists in the aureole of this granite mass at the expense of the quartz biotite schists involved a considerable transfer of material as shown by a comparison of the analyses of Table I with those of Table 4. There is no evidence to suggest that the granitic magma provided the necessary material and such a postulate would involve the simultaneous production of offshoots of the granite re- spectively rich in Na,O, MgO and Al,O, to produce the albite, chlorite, cordierite and andalusite schists as well as offshoots rich in K,O and 5i0, tn produce the veinlets of orthoclase and quartz which transect the wave-cut platforms. The evidence availahle suggests that there has been no intro- duction of material into the area of the aureole, but that the presence of the mass of intrusive granite produced the requisite conditions for meta- morphic differentiation. There has been a cedistribution of some material resulting in the production of the andalusite, cordierite, albite and chlorite schists but there has been no bulk introduction of material. The chemical changes which took place during the formation af these schists were considerable. In each case there was a decrease in SiO, and, except in the case of the muscovite- and biotite-rich chlorite schists, of KO. The excess of these constituents above that remaining in the schists is now found as yuartz veins and thin quartz orthoclase veins and stringers which are most abundant in the areas where the schists are most prominent. The role of AL,Oy varied; it was added to some of the rocks while from others it was taken away. Any excess Al,O, is found as “sweats” of andalusite which take the form of veins, Iubes and lenses. Surplus SiO, and MgO was also concentrated, in parts, in some of these “sweats’ in the furm of quartz, chlorite and cordierite. Both FeO and MgO were concentrated in the chlorite schists, the Mg@ especially, while their amounts in the more albitic types are less than those present in the country rocks. To a lesser extent MgO is concentrated in the cordierite schists. The albite schists, sotne of which contain as much as 80% albite, were enriched in Na,O, but the more chloritic iypes contain a low proportion of this constituent showing that it has been leached out during the transformations. The ammount of H,O in all the schists is considerably greater that the amaunt present in the country rocks and this, together with the presence of numerous “sweats” and veins in the area suggests that H,O was introduced into the area, possibly from the magma below, so that the rocks were relatively rich in this consti(uent during the rock transformations. 200 Varying proportions of andalusite, cordierite, albite, chlorite, biotite. muscoyite and quartz are found and the various mineral assemblages repre- sent Stages in the process of metamorphic differentiation. There is no regular distribution of any of the various types of schist and there is no definite order of formation of the constituent minerals: Most of the textures and structures of the country rock’ were destroyed by the transformations but telics of bedding and schistosity do remain in parts suggesting that the pracess was one of “soaking” with molecular or ionic exchange. Apart from the amount of H,O, the bulk composition of the area appears to be the same as it was before metamorphic differentiation, The process ceased when the granite mass cooled and the requisite conditions were no longer present. V. THE COARSE ALBITE CHLORITE ROCKS OF IGNEOUS ASPECT Rocks of this group—the “albite mica syenite” group of Browne (1920)— are generally coarse-grained, light-coloured and composed essentially of white albite crystals, up to 4x 3x3 cm, and green chlorite. In many respects these rocks resemble plutonic igneous rocks. They are distinguished fram ALAITE COMORES sDINST WI PATCH e@ OF Coan ALDINE CHCORITE MOCA +++ 4+iHe44 ++tettate GRanite 4+ + 4 = © 4 + Pio a ap + + + + +4 + + + + oa + + + + + + + 4 + + + + + + + + 4 +. 4 + + q- oo + + + + a + + + + + 4 + + + + Fig. 9 Geological Map of S.W. Tip of Rosetta Head. the porphyritic granite by the absence of blue opalescent quartz, the lighter colour and the abundance of white, twinned albite crystals. The proportions of albite and chtorite vary considerably from place to place, the rock varying from an albite-rich rock to a chlorite-rich rock although albite is generally present in the greater amount. Because of these variations in compositior the term “coarse albite chlorite rock of igneous aspect” is considered to lie more appropriate than “albite mica syenite,” as the rock is, in many instances far from syenitic in composition, 201 (a) Disrrrpution AND FIELp RELATIONS ‘These coarse albite chlorite rocks are mainly found at the main granite- country rock contact and they crop out almost continuously between the granite and the country rock (or albite chlorite schist in parts) on the landward slope of the headland (Fig, 2). Outcrops completely surrounded by granite and others completely surrounded by country rock are also seetl. The steep nature of the terrain at the S.W. Tip of the headland and near the wharf provides good exposures and enables (he field relations of these rocks to be studied in three dimensions. (1) South-west Tip of Rosetta Head The relationships of the cnarse albite chlorite rock with both the albite chlorite schist and the granite can be seem in this area. In the cliffs close to the sea, by the main contact with the country rock, veins, stringers and patches of coarse albite chlorite rock are present in the albite chlorite schist (Plate VL, Fig. 1). They are not present in the adjoining country rock or in the relics of country rock in the albite chlorite schist. The veins and stringers show no ordered arrangement or distribution and in many cases they do not connect with one another; many of thet are in the form of isolated lenticular masses. Further from the contact there are “xenoliths” of albite chlorite schist in the coarse albite chlorite rock. The boundaries of some of these xenoliths’ are not sharp; a gradation from fine albite chlorite schist to Aa eat Ole hSe ALONE Coyonire=e ry : Ss = _ Stange GLACIAL a att AIGTITE SC4iST =I S4ACIAL GHAATICS Toes hes ee pact wWorres ScHis ine Chlorite albite types contain less albite and quartz and more chlorite, biotite and muscovite than the rocks described above. The amount of micaceous minerals is greater than the amount of albite which still occurs as large crystals (9615-6). ‘These albites tend to weather out and from a distance the rock has, at first sight, the appearance of a vesicular lava (Plate VI, Fig. 3), Litle granulation is evident in these types although many of the large albites are cracked and show displacement of the twin lamellae along the cracks. The texture of one of these rocks is illustrated in Fig. 13c. These rocks grade into chlorite-rich types. which appear to be identical with the chlorite schists and have been mapped as such. A comparison of the analyses of these coarse albite chlorite rocks (Tahle 8) with the analyses of the albite chlorite schists (Table 4) reveals very marked similarities in chemical composition and the variations shown. As in the case of the schists, there is a high proportion of Na,O associated with a low proportion of K,O, especially in the more albitic types, and a high proportion of MgO in the chloritic types. The mineralogical dominance of albite and the scarcity of biotite in the albitic types is again reflected in the high amount of Na,O and the low amount of K,O, The small amount of chlorite present is reflected in the MgO: percentage. As the rocks become 207 more chloritic, the amounts of Na,O and SiO, decrease while MgO, H.O and to a lesser extent K,O, increase. As in the case of the schists, this reflevts the gradually diminishing amount of albite, the importance of chlorite and the increased proportion of biotite. These chemical changes are graphically represented im the variation diagram Fig. 14. FIG.I4 VARIATION DIAGRAM OF ANALYSES OF TABLE 8 (d) Genesis The present investigations have shown that these coarse albite chlorite rocks are related in the field to both the albite chlorite schists and to the granite. The salient points concerning their relationship with the albite chlorite schists are as follows: (1) Much of the coarse albite chlorite rock is found in association with albite chlorite schists, This is the case when granite is associated with the albite chlorite schists but not when granite is not associated with the schists. (2) At the 5.W. Tip and in the cliff near the wharf, lenses and masses of coarse albite chlorite rock appear to have been developed in site at the expense of the albite chlorite schists and both rock types have the same mineralogical and chemical compositions. (3) In some places, veins of coarse albite chlorite rock cut the albite chlorite schist and jin these cases, the veins are usually more albitic than the schist. (4) Variations in both mineralogical and chemical compositions are parallel even in respect of many details. The salient features concerning the relationship of the coarse albite chlorite rock with the granite are as follows: (1) Coarse albite chlorite rocks crop out almost contunuously along the main granite- country rock boundary. Their form is .as a sheet or a series of isolated fiat bodies in the plane of the contact {1e. dipping 35°S.E.) with the granite above and the country rock—or albite chlorite schist—below. (2) There is always a sharp contact between the two rocks, regardless of the composition of the coarse albite chlorite rock. (3) In some cases the granite tongues in and out of the coarse albite chlorite rock but in other cases the coarse albite chlorite rock tongues in and out of the granite or is found as small plug-like masses in the granite. The salient features of the coarse albite chlorite rock itself are as follows: (1) Tt shows intrusive relations with the granite and the country rock and in some but not all cases, with the albite chlorite schists {as stated above). (2) Many of the albites are strained, cracked and broken and show con- siderable peripheral granulation. This is most pronounced in the albitic types and is not common in the chlorite types. (3) Some of the chlorite flakes 208 are bent, some wrap around the large albites, and yet others are found as rosettes of large crystals, (4) A few of the albite individuals in the veins of coarse albite chlorite rock are considerably larger than the narrowest parts of the veins, (5) The shapes of the walls on either side of the veins often do not match. This evidence suggests that the parent of the coarse albite chlorite rock Was the albite chlorite schists and that the rock was formed during, and because of the intrusion of the granite by recrystallization and partial mobilization, In the eatly stages of the process, large albites and chlorites grew in the albite chlorite schist in favourable areas, which were probably those containing most moisture and those most affected by the heat from the magma. Hence there developed irregular lenses, masses and stringers of coarse albite chlorite rock in albite chlorite schist of the same composition. As the processes proceeded there was loss of cohesion hetween some af the smaller grains and the rock hecame capable of movement and intrusion, The more albitic rocks were most susceptible and so a semt-mobile coarse albite chlorite rock containing large albites and some large chlorites in a mobile base veined the surrounding rocks. This provided the heat and Auid necessary for parts of the vein walls to become semi-mobile and so the veins widened and the size of the crystals increased, The more chloritic types were not sa readily mobilized, but large albite crystals developed in them and the grain-size of the chlorites increased. The chlorite-rich schists were not mobilized but were recrystallized to give coarse chlorite-rich rocks. A considerable amount of semi-mobile coarse albite chlorite rock was farmed at the expense of albite chlorite schist along the main gramite contact during the over-riding intrusion of the granite up the dip of the strata. This miush of albite and chlorite crystals in a Huid base was forced along beneath the intruding granite and incorporated into itself mare albite chlorite schist over which it pushed, Thus the coarse albite chlorite rocks are found as a sheet or a series of flat bodies in the plane of the main granite-country rock contact and show sharp, intrusive relations with the vranile, the country rocks and some of the albite chlorite schists. With this type of intrusion the large albites were cracked, broken, strained and granulated and the chlorites were bent and pushed arptind the albites. With the cooling of the granite mass, the fluid base crystallized forming some large rosettes of chlorite, but mainly the finer grained base of albite and chlorite with some quartz. VI. THE GRANITIC ROCKS (a) Distaiution ann Pirin RELATIONS The scaward part of Rosetta Head is a mass of grey porphyritic granite (Fig. 3) which is similar in mode of outcrop, appearance and composition to the granite found on West Island, Wright Island and in some Jocalilies at Port Elliot (Fig. 1). Sharp contacts are shown at Lhe junction of the granite with the country rock, the albite chlorite schist and the coarse albite chlarite rock of igneous aspect. Small tongues of pranite are injected into the country tock at the contact, much of the nearby rock is a hornfels and a narrow zone of contact schist follows the contact, The granite overlies the country rock as the main contact dips 35° S.E. Angular disoriented xenoliths of metamorphosed and metasomatised country rock are present in the granite anc these are concentrated near its margins, The metasomatic alteration of the xenoliths of country rock in the granile of Granite Island has been studied by Kleeman (1937) and 209 similar stages of alteration to those described in that area aré shown in the xenoliths at Rosetta Head. Two small masses of even-grained granite (9617) with sharp intrusive contacts, outcrop on the landward side of the main granite-country tock boundary, Directional features due to the parallel orientation of biotite flakes are shown in some of these rocks. Small, angular disoriented xenoliths of country rock are enclosed in the granite and some of these have dark rims enriched in biotite (9618) due to teaction between xenolith and magma (Plate VL. Fig. 4), There ts a small outcrop of graphic quartz felspar granite just east of the old mine shaft, The prophyritic granite is cut by dolerite dykes which are now uralitized. One dolerite on the south-eastern side of the headland intrudes into both the coarse albite chlorite rock and the granite and has a fine-grained margin which shows parallel flow banding through four or five inches within the contact, The associated granite shows directional features, with the orienta- tion of biotite flakes parallel to the edge of the dyke. The dolerite itself is cut by small quartz tourmaline veins. (b) MINERALOGICAL COMPOSITION Soda-microcline microperthite, The felspar phenocrysts from the granite of Granite Island were described by Gartrell (1903) who classed them as anorthoclase. Later Browne (1920) suggested they were microcline mucro- perthite. The mineral shows microcline crass-hatching, has two cleavages at right angles and measurements on the Universal Stage have shown that it has an optic axial angle of 74° (+1°), a negative optical sign and an extinction angle YA(010) of 54°. This suggests a composition intermediate hetween microcline and anorthoclase. A section parallel to (010) shows intergrown streaks of plagioclase which are roughly parallel to (100), This plagioclase has an optic axial angle of &2° (+1°), is optically negative, has a maximum extinction angle on a section normal to (010) of +14° and has a composition of acid andesine (Ab,.). The mitieral is thus. a soda-microcline microperthite, the chemical com- position of which was recorded by Gartrell (1903) and the above determina- tions show why the CaO percentage is high for a perthite and why the Na,O pereentage is high for microcline and low for anorthoclase. The proportions 4 the various felspar molecules calculated from the analysis are Org,, ADag, Nij- Plagioclase. Albice and pericline twinning is offen shown and many of the crystals are strongly zoned, The centre of some of the zoned. ctystals is andesine (Ab,,} but the composition becomes progressively more albitic towards the outer zones which are usually Ab,, although some are Ab,,. A few small crystals in the ground muss also huve a composition pf Aby,,. (c) Tetrocrapuy, CHEMICAL COMPOSITION AND CLASSIFICATION The porphyritic granite (9619) consists of large, tabular, subhedral phenocrysts of soda-mirocline microperthite up to 4x3 cm,, together with some large plagioclase and quartz individuals set in a coarse-grained ground- mass, with hypidiomorphic texture, of quartz, microcline, acid plagioclase and biotite, Muscovite, apatite, zircon, ilmenite and pyrite are accessory, The potash felspar phenacrysls are studded with inclusions of irregularly distributed biotites, up to 3. mm. in length, small laths of andesine and ragged or rounded grains of quartz together with smaller biotite flakes and small apatite prisms. All these inclusions are primary and of earlier crystallization than the felspar, but some later quartz and muscovite fills cracks. As a 210 described by Browne (1920, p. 13) a “fairly constant characteristic of these felspar phenocrysts is the presence of a rim of variable width composed of quartz granules graphically intergrown with felspar . . . ‘The inter edge of the rim is usually straight. There are outgrowths of felspar beyond the rim, the phenocrysts having as a result irregular boundaries against the other minerals of the rock. These outgrowths are usvially notably free from perthitic intergrowths . . .” This rim often shows up megascopically as an outer, whiter zone, giving the appearance of a zoned felspar. TABLE 9 P Analyses of granites A 8 Cc D E F SIGq eg ee tee eee nee PS 71°44 68°20 75 +8 70-18 65-01 TiOn ae ce ee ee ee OSA OSB DH 0-39 0-57 AlsO,s vue te eee eee 1G7B 15-09 18509 12-90 14g? 15.04 FesOn 0. ce cae ee ee O80 0-86 0-39 0-25 1°57 1-74 REO i cas tai ake ats ER 2-58 0-85 1-78 2-65 MnO wee ee O01 0-02 0-04 = 0-12 0-07 MgO wn ue ke ae ee NY 8) 0-80 0-13 0-88 1-9) CaO... n., oer ys Os F: | 0+74 1-99 4-42 NasO oo. ee ee ene cee 2h 2-09 285 231 3-48 3-70 Katd= oe co. ein pine 4035 4-46 4-60 6°06 4-11 2:75 H,O+ tin ate one cet DSS 0-24 0-64 0:60 > HiO-(#10°C) a OE 04 et eee O84 1-04 PrOw ee cee ee OT 0-22 O14 _ 49 ‘0-20 Zr Qe ve cece cess cee aeee EB — pad. _ = — BaO cee ay ree ee OD mil 0:04 — —_ — Ss wets tins aork atte en "OOS —_— — _ _— — HeSy fen can, od xine) Ane — 0-04 O11 = ~ Sn, Cl sagh | Hite wane Yqi'e _ 0-05 — —_ ~ ~ 100, +52 GO-41 =100+28 99-70 «106-00 =: 180-00 Less O for S ou. an a. =©002 _ — um ee — 100°50 99-41 10028 99-70 100-00 100-00 A. Porphyritic granite (9619), Rosetta Head (bulk analysis), Analyst: D, R. Bowes, B, Porphyritic granite, West Island. Analyst: W. S. Chapman (Jack, 1923). C. Porphyritic granite, Granite Island, Victor Harbour. Analyst: W. R. D E Browne (Browne, 1920). Even-grained granite, Port Elliot. Analyst: W. R. Browne (Browne, 1920). . Granite of all periods: average of 546 analyses (Daly, 1933). F. Granodiorite: average of 40 analyses (Daly, 1933). The analysis of the porphyritic granite shows that its composition is comparable with those of the corresponding rocks from West Island and Granite Island (Table 9). A comparison with averages of compositions of granite and grandiorite (Daly 1933) shows that the SiO,, MgO, CaO and K,O percentages of the porphyritic granite from Rosetta Head are similar to those of the average of granite, while the TiO, and FeO percentages are similar to those of the average of granodiorite. The rock contains considerably less Na,O than the average of either granite or granodiorite and much more K,O than the latter, whereas the even-grained granite from Port Elliot is even poorer in Na,O but very rich in KO. Apart from an abnormally high 241 amount of corundum in the norm of the West Island granite, the norms of the granites (Table 10) reflect the variations shown in the different granites in the variations of the percentages of the standard minerals. Potash ‘felspar and acid plagioclase are present in approximately equal proportions with quartz and biotite being abundant and the only other ‘essential minerals. Hence, petrographically, the rock should be classified as-an adatnellite, whereas its chemical composition is similar to granite in some respects and granodiorite in others. Field and internal evidence reveals that the rock is a contaminated one, hence it is best termed a contaminated granite. Taste 10 Norms of granites A B Cc D Quartz ever) EYL | 37-2 26°28 36-48 Orthoclase cue wee 26713 26°69 27-24 36.14 Albite sae un pee 2308 17-82 24-30 19.39 Anorthite 2... sa. wo 8°34 4-45 11-95 361 Corundum oe ve 1+43 5-10 1-94 1-22 Zircon car wee we = O37 _ — —_ Hypersthene—En ... 2°80 2-00 2-00 0-30 ” Fe .. 3:43 2:64 3-04 1-19 Magnetite 0 1. sn. 1716 1-16 1°39 0-46 Timeniteé 0 =. a 1°08 1-06 1-06 0-23 Pyrite oa eee nee 0-12 _— = — Apatite Hiss eons ony WDA 0-50 0-4 — ee a ee ne ee sees ee (d) GENESIS ‘The intrusive, magmatic origin of this granite is clearly demonstrated on field evidence. It contains hornfelsed and metasomatized disoriented xenoliths of country rock, the granite-country rock boundary is sharp with small veins and stringers of the granite penetrating the country rock, and the granite mass has an associated contact metamorphic aureole. Hence it is considered that in this area, a granite magma stoped its way upwards and blocks of displaced country rock are strewn ahout as xenoliths. The gtanite is in close association with the albite chlorite schists which it veins and cuts near the wharf. It would thus appear that the granite now occupies space formerly taken by these schists, but no remains of the albite chlorite schists are found as xenoliths and no grains of albite or flakes of chlorite are strewn about in the granite, As albite and chlorite are lower in the ‘reaction series (Bowen 1928) than the plagioclase and biotite of the granite, these minerals are thought to have been reactively dissolved by the magma. It is considered that the assimilation of such albite- and chlorite-rich rocks into potash-rich granite magma, possibly similar to that represented by the even-grained granite of Port Elliot (vide Table 9), would explain the formation of the porphyritic granite and its unusual mineralogical and textural features. The following is an elaboration of this hypothesis, With the incorporation of blocks of albite- and chlorite-rich rock into the granite magma, the albite was dissolved and its heat equivalent of ande- sine (Abg,)—the plagioclase with which the magma was saturated—was precipitated. The chlorite, together with the associated muscovite, was alsa dissolved with the concomitant precipitation of its heat equivalent of biotite. Any quartz individuals present in the incorporated rock were reacted upon by the magma giving them ragged outlines. These processes enriched the 212 magma in soda, magnesia and titania and from this melt the snda-microcline microperthites were precipitated, The phenocrysts probably grew quickly inclnding within themselyes crystals of the previously precipitated andesine and biotite and the ragged-edged quartzes. The plagioclase intergrowth is more albitic (Ab,,) than the previously precipitated crystals. Following the formation of the phenocrysts, crystallization proceeded normally with falling temperature, The composition of the plagioclase became more albitic and a coarse-grained groundmass of quartz, bictite, microcline and acid-plagioclase, together with accessory minerals, crystallized. The rim of graphically intergrown quartz and felspar which forms a zone around the phenocrysts grew during this period; the inner edge is straight against the erystal face. but the outer edge dovetails inta the grotindmuss. The occurrence of coarse albite chlorite rock on both Wright Island and Granite Island suggests that the granite in these areas may have assimi- lated albite- and chlorite-rich rocks during intrusion and that the genesis suggested above is applicable to the porphyritic granite of these islands and in othet areas of the Encounter Bay region. The small masses of even-grained and graphic granite cropping out on the landward slope of Rosetta Head are taken to represent two of the final stages of crystallization of the contaminated granite magma. VII. THE PETROLOGY OF THE SERIES The earliest effects of metamorphism in this area were of a regional nature with the isochemical metamorphism of greywacke and subgreywacke types to quartz biotite schists, This was post-folding but during the period in which stress was an active agent, The other metamorphic and igneous events were post-tectonic and alse after all regional stresses had ceased to operate. They were connected with the upward intrusion of magmatic gtanite into rocks which had previously only reached the biotite grade of regional metamorphism. A mass of intrusive granite just below the present level of the wave-cut platforms produced an aureole of contact metamorphism and metasotnatism. Metamorphic differentiation took place with the exchange of material and the production of andalusite, cordierite, albite and chlorite schists at the expense of the quartz biotite schists, The bulk composition of the area Temained essentially the same and “sweats” of andalusite, chlorite, cordierite and quartz, veins of quartz and stringers of quartz and felspar represent the material thrown out during the formation of the contact schists. The granite intrusion reached its highest level in the crust at Rosetta Head and this cupola-mass weakly hornfelsed the surrounding area but partially mobilized the albite chlorite schists with which it came in contact. The granite made its way up the bedding planes, using bedding and schist- osity as structural controls, and over-rode both quartz biutite schists and contact schists, Any albite chlorite schists along this gtanite contact were made mobile and pushed as a mush along the dipping boundary of the intrusion by the intruding granite above. This mush was capable of intrusion and crystallized as a coarse albite chlorite rock of igneous aspect. The original granite magma is considered ta have assimilated considerable quantities of albite- and chlorite-rich rocks and its composition, porphyritic nature and other features are thought ta be due to this cause, ‘A final movement in the emplacement af the granite at Rosetta Head was either associated with, or caused some local stresses, as a zone of contact schists up to Len feet wide, follows the main contact in must parts. These rocks modify the hornfelsed quartz biotite schists and there was local devel- 213 opment of andalusite schists by isochemical contact metamorphism under some stress, Hence four periods of metamorphism and three phases of the granite intrusion have been separated by this study. The first period of meta- morphism was associated with regional factors, but the other three stages are connected with one another and with the main emplacement, the emplace- ment of the cupola-mass of Rosetta Head and the final movement of the intfusive granite, respectively. Dolerite dykes—now uralitized—were injected later, followed by a small amount of pegmatitic activity, VIII. EXTENT AND AGE OF THE INTRUSION There are many outcrops of granite in the Encounter Bay area (Browne 1920) all of which appear to be part of the same intrusion. The granite at Cape Willoughby, Kangaroo Island, is considered by Tilley (1919) to be part of the same batholith and a suite of similar rocks from south-eastern South Australia has been described by Mawson and Parkin (1943) who assume that the rocks are “an eastward extension of the Encounter Bay and Cape Willoughby intrusions.” As previously suggested (Bowes, 1953), it is considered that there was a period of granite formation and intrusion in South Australia during early Palaezoic times. At this fime the granitic rocks of southern and south-castern South Australia formed upon the collapse of the eugeosyncline which ex- tended to the east and south-east of the miogeosyncline in which the sedi- ments of the Adelaide System were deposited, This period is correlated with the migmatization and granite intrusions which took place in the North- eastern Flinders Ranges, the final stages of which have been dated as mid-Ordovician by an age determination of 400+ 50 million years on a samarskite from a granite pegmatite (Kleeman, 1946), The postulated (?) Early Palaeozoic age of the intruded and altered country rocks at Rosetta Head appears compatible with the correlations. ACKNOWLEDGMENTS I wish to record my thanks to Professor Sir Douglas Mawson for suggesting the area and for making available specimens and data previously collected; to Mr, A, W. Kleeman for his advice and he)pful criticism and to the University of Adelaide for the assistance made available by the award of the James Barrans Scholarship. BIBLIOGRAPHY Bowen, N.L. 1928 The Evolution of the Igneous Rocks. Princetown Bowes, D, R. 1953 The Genesis of Some Granitic and Associated Rocks in the North-eastern Flinders Ranges, South Australia, Trans. Roy. Soc, S. Aust. 76 Browne, W, R. 1920 The Igneous Rocks of Encounter Bay, South Australia. Trans. Roy. Soc. S. Aust., 44 Day, R. A. 1933 Igneous Rocks and the Depths of the Earth. New York Gartretr, H.W. 1903 The Port Victor Granite. Trans. Roy Soc. S, Aust., 27 Howenin, W. 1926 The Geology of the Victor Harbour, Inman Valley and Yankalilla Districts, with special reference to the Great Inman Valley Glacier of Permo-Carboniferous Age. Trans. Roy. Soc. S: Aust., 50 Howcutx, W. 1929 The Geology of South Australia, Adelaide Jacx, R. L, 1923 The Building Stones of South Australia. Geol, Surv., S. Aust., Bull. 10 214 Kireman, A. W. 1937 The Nature and Origin of the so-called Diorite Inclu- sions in the Granite of Granite Island. Trans, Roy. Soc. S. Aust., 61 Kreeman, A. W. 1946 An Age Determination on Samarskite fram Mount Painter, South Australia. Trans, Roy. Soc. S. Aust., 70, (2) Mawson, D. 1926 A Brief Resumé of Present Knowledge Relating to. the Igneous Rocks of South Australia. Aust. Assn. Adv. Sci., 18 Mawson, D. 1947 The Adelaide Series as Developed along the Western Mar- gin of the Flinders Ranges. Trans. Roy. Soc. S. Aust., 71, (2) Mawson, D. and Datiwitz, W. B. 1944 Palaeozoic Igneous Rocks of Lower South-eastern South Australia, Trans. Roy. Soc, S. Aust., 68, (2) Mawson, D., and Parxrn, L. W. 1943 Some Granitic Rocks of South-eastern South Australia. Trans. Roy. Soc. S. Aust., 67, (2) Pertiyoun, F. J. 1949 Sedimentary Rocks. New York Rozinson, E, J. 1946 The Hornfels Series of the Eastern Mt. Lofty Chain. Portion of Thesis, University of Adelaide, Tittey, C. E. 1919 The Petrology of the Granite Mass of Cape Willoughby Kangaroo Island, Part I. Trans. Roy. Soc. S, Aust., 43 TYRRELL, S W. 1933 Greenstones and greywackes. Bull. Comm. géol. Finlande, 102 ‘UL S— (0096) ; "AAOD [PV ‘ISUPPS aoIpsoo Ppayouy Jo ydeasoyoyd-Oss1yy FAL VPALN Ty UN0 | “yao ws SPUD BHULAIE AY PUR Jitlod *QA07) [oted OL SpAleMjsae pray. FeSO" ULOLL Z “8g = ss) . ye Me r . one MOL WiOd, PLHe[Ssy Ht “DAO PAI UL JST S}dorploa pyHoury Jo do1dqUg , e ‘Bly ‘PURS[ apiuBts AV pure I ‘ pues | ISIN TPoH PYPSOPY Bud Plate V1 77, Vol. + 5 Roy. Soe. S. Aist,, 19 Trans. TWAYO AJINOGD F pur aes u ‘peaH E}jesoy ‘OT X— (8196) UoX 9} JO ML Yu-ayorg ay Surmoys yWpouaxX yso1 JIMJaq JORPUOD Jo Yydes ayiq[e aT LO[ To UA JO ydeisoyoyd-O1atyy “‘pRaH Blasoyy ‘ULE CAS VE JoRyUOD ayUBIA—yoos APR ayo 2 nO} ¢ “Shy “pray Eyosoy LL “AVS a9 Wes ‘ Ol] F}ITe EB ASIBOI—]S1Yos aliqye—yoo1 Aapunas 215 ROYAL SOCIETY OF SOUTH AUSTRALIA (INCORPORATED) Receipts and Payments for the Year ended 30th September, 1953 RECEIPTS | eu ae? ree £s.d £ 8. d. By Tratsactions— lla i To Balance, 1/10/52... 678. 5 10 ’ Printing and Publishing » Subscriptions chee ah 138 14 0 Vol. 75 ow, 837 14 6 » Government Grant for Part Vol. 76. .. $61.15 81,399 10 2 PAS. 1400 0 0 =~ 19 a » Reprint: ve ius 1953/84 (Istinstlt) ‘350 0 041,750 0 0 ” Tibrarian 5 ear —<————— » Printing an St: » Sale of Publications and ” Postage, a ationery ic i i Reprints ike Seden i413 2 . Filing Cabinets du 6716 4 ” Interest Saop) ge -eegen Qeees 214 8 9 ” Insurance nese Bn 1210 O » Lighting bes stk 12 8 8 » Cleaning Rooms x: 38 7 0 4 Sundries 717 0 » Balance 30th Sept., 1953: A. and N.Z. Bank Ltd..... 672 11 5 Less Out- standing Chqus6 5 0 100 3 8 0 1013 0 661 18 5 Savings Bank of S.A.: General A/c. 536 0 0 Ex Endow- ment Fund 11 7 9 547 7 9 Cash on Hand ay 215 61,212 1 8 £2,996 1 9 £2,996 1 9 ENDOWMENT FUND Receipts and Payments for the Year ended 30th September 1953 £sda € a a £sd4a £ s. d. 1952—October 1 1952—Sept. 20 To Balance— By Revenue A/e. wo 214 8 9 Commonwealth Inscribed » Balance Stock 6,010 90 0 Commonwealth In- Savings Bank of S.A, 62 18 76,072 18 7 scribed Stock ....6,010 0 Q ————— Savings Bank of S. A. | 6218 7 6,072 18 7 1953—Sept. 30 Inscribed Stock aw =199 14 6 Savings Bank of S.A... 1414 3 214 8 9 £6,287 7 4 | £6,287 7 4 rewire oo I Audited and. found correct. The stock and Bank Balances have been verified by certificate from the respective institutions. M. ANGEL Ul _-Hona. N. ANGEL, A.U.A.Com. § Auditors T. R. N. LOTHIAN, Hoa Treasurer Adelaide, 6th October, 1953 216 AWARDS OF THE SIR JOSEPH VERCO MEDAL 1929 Pror. Warrer Howcuin, F.G.S. 1930 Jown McC. Brack, A.LS. 1931 Prov. Sin DoucLas Mawsos, O.B,E., D.Sc. B-E,, F.R.S. 1933 Pror. J. Burtow Crzranp, M.D. 1935 Pror. T. Harvey Jonnston, M.A., D.Sc, 1938 Por. J. A. Prescott, D.Sv., F.A.LC. 1943 Herpert Womenstey, A.L,S,, F.R.E.S. 1944 Paor, J. G. Woon, D.Sc. Ph.D, 1945 Crem T. Manicax, M.A., B.E., D.Sc. F.G.S. 1946. Hervent M, Hare LIST OF FELLOWS, MEMBERS, ETC. AS AT 30 MARCH 1953 Those marked with au asterisk (*) have contributed papers pyblished in the Society’s Transactions. Those marked with a dagger (t+) are Life Members, Any change in address or any other changes should be totified to the Secretary, Noie—Yhe publications of the Society are not sent to those members whose subscriplians are in arrear. Bates, Honorary Feccows 1945, *Fenner, C. A. E., D.Sc., 42 Alexandra Avenue, Rose Park, Adelaide—Fellow, 1917-45; Council, 1925-28; President, 1930-31; Vice-President, 1928-30; Secretary, 1924-25; Treasurer, §932-33; Editor, 1934-37. 1949. *Cretann, Pror. J, B, M.D., Dashwood Road, Beaumont, S,A.—Fellow, 1895-1949; Verco Medal, 1933; Council, 1921-26, 1932-37; President, 1927-28: 1940-41; Vice- President, 1926-27, 1941-42. Frttows. 194, Appre, Prov A. A., M.D., D.Sc, Ph,D., University. of Adelaide, 1953. Apcock, Miss A., 4 Gertrude Street, Norwood, $.A. 1951. Arrcaison, G, D., B.E,, Waite Research Institute (Private Mail Bac), G.P°0., Adelaide. 1927. *AcperMaAK, A. R., Ph.D., D.Sc, F.G.S. , Div. Indus, Chemistry, C.S.LR.O., Box 4331, G.P.0., Melbourne, Victoria—Couneil, 1937-42. 1951. Anpvrrson, Mrs, S. H., B.Sc., Zoology Dept., University of Adelaide, S.A. 1931. Anorew, Rev. J. R., c/o Methodist Manse, Maitland. 1951, Awprews, J., M.B., B.S., 40 Seafield Avenue, Kingswood, S.A, 1935. *Anprewarrma, H. G, M.Agr.Sc., D.Sc., Waite Institute (Private Mail Bag), Adelaide—Counctl, 1950; Vice-President, 1950-51; President, 1951-. 1935, *AnprewarrHa, Mrs. H. V., B.Agr.Sc., M.S. (nee H. V. Steele), 29 Claremont Avenue, Netherby, S.A. 1929. *Ancer, F. M,, 34 Fullarton Road, Parkside, S.A, 1939, *AncEL, Miss L, M,, M.Sc., c/o University of Adelaide. 1945. *Bartrert, H. K., L.Th., 15 Claremont Avenue, Netherby, S.A, 1950. Brastey, A. K,, Harris Street, Marden, S.A. 1950, Brcr, R. G, B.Ag.Se., R.D.A,, Linewood Park, Mittel, S.A. 1932. Brce, P, KR. D.D.Se., L.D.S., Shell House, 170 North Terrace, Adelaide. 1928. Best, R, J., D.Sc, F.A.C.1., Waite Institute (Private Mail Bag), Adelaide, 1953. Bro, A. F., B.Sc., Zoology Department, University, Adelaide, 1934, Bracx, E. C, M.B., B.S. Magill Road, Tranmere, Adelaide. 1950. Bonnin, N. J.. MB, B.S., FRCS. (Eng:), FR.A.CS,, 144 Hil Street, North Adelaide, S.A. 1945, *Bonyrsoy, C. W., B.Sc, A.A.C.I.; Romalo House, Romalo Avenue, Magill, S.A. 1940. BonytHon, Sir J. Lavincron, B.A, (Camb,), 263 East Terrace, Adelaide. 1945. *Boomsma, C, D,, M.Sc., B.Sc.For., 2 Celtic Avenue, South Road Park, S.A. 1947, Bowes, D. R,, Ph.D., M.Sc,, D.1.C, F.G.S., 51 Eton Street, Malvern. 1939. Brookman, Mrs. R. D. (nee A. Harvey), B.A., Meadows, S.A, 1945. Brovucuton, A. C, Farina, S.A, 1948. Brownine, T: O., B.Sc. (Syd.), Waite Institute (Private Mail Bag), Adelside. 1944. *Burpipcr, Miss N. T., M.Sc, C.S.LR.O., Div. Plant Industry, P.O.. Box 109, Cat:- berra, A.C.T. Bunvon, R, S., D.Sc., University of Adelaide—Coyncil, 1946, 2 Oate of Election, 1922. *Cameseir, T. D, D.DSe, D.Sc, Dental Dept, Adelaide Hospital, Adelaide— Council, 1928-32, 1935, 1942-45; Vice-President, 1932-34; President, 1934-35, ' 1953. Canten, A. N., B.Sc., 70. Madeline Street, Burwood F 13, Vict. 1951. areata, R. G, B.Sc, c/o CS.LR.O,, Div. of Fisheries, 1 Museum Street, Perth, W.A. 1929. Curistre, W., M.B., B.S., Education Department, Social Services, 51 Pirie Street Adelaide—Treasurer, 1933-38, 1950, Coatsran, 5. T, BSc, 6 Iampton Street, Hawthorn, S.A, 1949. Cortiver, FP, S., Geology Department, University of Queensland. 1930. *Corgunoun, T. Ty MSc., 10 French Street, Netherby, S.A. Secretary, 1942-43. 1907. *Cooxr, W. T., D.Sc, AA.C.L, 4 South Terrace, Kensington Gardens, S.A.—Counell, 1938-41; Mice-President, 1941-42, 1943-44: President, 1942-43, 1942, *Coorsr, H. M,, 51 Hastings Street, Glenelg, S_A, 1929. *Corrox, B, ©, SA, Museum, Adelaide—Connei, 1943-46, 1948-49; Fire-President, 1949-50, 1951; President, 1950-51. 1953, Dawe, D. M. S. MB. B.Chin, M.R.CS., L.RC.P., B.A,, Institute of Medical and Veterinary Science, Frome Road, Adelaide; 1951, Dayne, AGL, PLD, B.Sc, Waite Research Institute, Private Mail Bag, G.P.G, co 1950, Detanp, C. M, MB, BS, DPD, DJ, 29 Gilbert Street, Goodwood, S.A. 1941. Dicxtnson, S. B., M.Sc, 51 Moseley Street, Glenelg, S.A. Council, 1949-51; Vice- President, 1951-. 1930. Dix, E. V., Hospitals Department, Rundle Street, Adelaide, $.A. 1944. Duxstows, S. M. L, M.B., B.S., 124 Payneham Road, St. Peters, Adelaide. 1931, Dwyer, Ff, M,, M.B., B,S., 105 Port Road, Hindmarsh, 5.A. 1933. *Earpizy, Mrss C. M., M.Sc. University of Adelaide—Council, 1943-46. 1945. *Enmonns, S. J, B.A. M.Sc. Zoology Department, University, Adelaide, 1902. *Epouist, A. G, 19 Farrell Street, Glenelg, S.A—Couneil, 1949-, 1944. Freres, Mrss H. M., M.Sc., 8 Taylor's Road, Mitcham, S.A. 1927. *Fintayson, H. H,, 305 Ward Street, North Adelaide—Council, 1937-40. 1951. Fismer, R. H., 265 Goexdwood Road, Kings Park, SA. | 1923. *Fry, H. K., O.S.0., M.D, B.S., B.Sc, F.R.A,C.P,, Town Hall, Adelaide—Council, 1933-37: Wier-President, 1937-38, 1939-40; President, 1938-39, 1951. Futon, Cor, D, C.MG.,, CB.E., Aldgate, S.A. 1954. Greson, A. A., A.W.A.S.M., Geologist, Mines Department, Adelaide. 1932. *Greson, E. S, H., M.Se., 297 Cross Roads, Clarence Gardens, Adelice. 1927, Goorrev, F, K,, Box 951H, G,P.O,, Adelaide, 1935. }Go.nsacx, H., Coromandel Val'ey, S.A. 1925. Gosse, Sm James H., Gilbert House, Gilbert Place, Adelaide. 1910. *Gaant, Prov. Sin Kerr, M-Sc., F.LP., 56 Fourth Avenue, Se. Peters, S.A, 1930. Gray, J. T,, Orroroo, SA, 1933, Greaves, H., 12 Edward Street, G'ynde, S.A. | 1951, Green, J, W. 4 Holden Street, Kensington Park, S.A. 1904, Grirrivn, H. B,, Dunrobin Road, Rrighton, 5.4, 1948, Gross, G F,, B.Sc, South Australian Museum, Adelaile--Secretury, 1950-— 1944, Guevy, D, J., B.Sc. Mineral Resources Survey, Canberta, A,C,T. 1922. *Hacr, H- M., Director S.A. Museum, Adelaide—Ferro Medal, 194; Council, 1931-34, 1950-; Vice-President, 1934-36, 1937-38; Presides?, 1936-37; Treasurer, 1938-1950. 1949, Hatt, D, R,, Mern Merna, via Quorn, S.A. 1953. Hansen, I. V., B.A., 34 Herbert Road, West Croydon, §.A. 1946, *Harvy, Mrs, J. E. (nee A. C. Beckwith), M.Sc., Box 62, Smithton, Tas. 1944. Harars, J. R., B.Sc, 94 Archer Street, North Adelaide, S.A. 1947. Henperson, D. L. W., P-M.B., 20 Bourke, N.S.W. 1944. Herrror, R. 1, B.Agr.Sc,, Soil Conservator, Dept. of Agriculture, S.A. 1954. Hinroy, F. J., B.AgSe., Botanist, 298 Miugill Road, Benlaly Park 1951. Hoeexrne, L. J., 57 Marino Parade, Seacliff, S.A. 1949, Horioway. B. W., B.Sc., 33 Kyre Avenue, Kingswood, S.A, 1924. *Hossrernn, P_S, MSe, (322 Fisher Street, Fullarton, S.A. 1950. Howarp, P. F., USe., c/o Great Western Consolidated, Bullfitch, W.A, 1944, Humere, D. S, W~ 238 Payneham Road. Payneham, 5.A. 1947, Hurron, J. T.. B.Sc, 18 Emily Avenue, Clapham, 1928, Irounn, P. Kurralta, Burnside, SA, 1942, Jenxins, C F. H., Department of Agriculture, St. George’s Terrace, Perth, W.A, 1918 “Jenwison, Rev. J, C., 7 Frew Street, Fuilarton, S.A 1945, *Jessur, R, W,, M.Sc. 3 Alma Road, Fullartan, 5.4. 1910. *Jonnson, FE. A., M.D. MRCS, 1 Baker Street, Glenelg. 1950. Jouns, R. K., B.Sc, Department of Mines, Flintlers Street, Adelaide, S.A. 1951, Kavarovic, D., B.A‘Sc, (Mun), 22 Grandview Road, Toorak Gardens, S.A 21g Date of Eleeslon, 1954. Kaars, A. L., BE, prey C/o. North Broken Hill Led, srolaope Hi 1951. KxsTine, YN. fe Dept. Ar and Ed., P.A.C, Preparatary School, 3 Hartley R ‘esp Brightan, tKeaamy i Mi, Ph.D., MB, F.R.GS., Khakhar Buildings, C.P, Tank Read, Rom- *Kine, D,, M.Sc. 44 een Avenue, Blair Athol, S.A. . *KLEEMAN, A. W., M.Ses University of Adelaide—Secretary, 1945-49: [ice-Prest- deni, 1948-49, 1950-51; President, 1949-50. Lenpow, G. A., M. es B, Sc E.R.C. P., A.M.P, Building, King William Street, Adelaide, Loratan, T. R. N,, N.D. i, cN. 2). er Botanic Garderis, Adelaide. Lowek, H, F., 7 Averue Road, Highgate, S. *Luveroor, Mrs. N. H., M.A., Pn.D. D.LC., Fo. S., Department of Mines, 31 Flinders Street, Adelaide, McCurtocn, R, N., M.B.E., B.Sc. (Oxon.), B.Agr.Sci. (Syd.), Roseworthy Agricul- tural College, S.A. Maporen, C, B., B.D.S,, D.BiSe, Shell House, North aierrace, Adelaide, Maszeg, D. A, B.Sc. (Hons.), Waite Institute, Adelaide, Mann, E. A., C/o Bank of Adelaide, Adelaide, MARSHALL, T. J. M.Aer.Se, Ph,D., Waite Institute (Private Mail Bag}, Adelaide— Council, 1948 *Mawson, "Prov. ‘Sin Doors, 0.8.E, D.Sc, BE, PRS, University of Adelaide-~ Vereo Medal, 1931; President, 1924- 25, 1944-45: ¥ ice-President, 1923-24, 1925-26; Council, 1941-43. May, L. H., BSc, 691 Esplanade, Grange, S.A, Mayo, THe "Hon, Me: Justice, LL.B., K.C., Supreme Court, Adelaide, Mayo, G, M. E,, B,AgSc., Waite 2 Instimte (Private Mail Bag), Adelaide, S.A. McCauray, Misa D, BA. & B.Sc., 70 Halton Terrace, Kensington Park, McCautnezy, J. E,, MD. D Sc. (Edin), Institute of Medical and Veterinary Science, rome Road, Adelaide. F: , . . tMmes, K. R, D.Sc. FES. Mines. Department, Flinders Street, Adelaide, Mries, J. A. K, MA, y BChie. (Cant), 48 Gladys Strest, Edwardstown, S.A. Mincuam, V. H. ee ene tMrecuent, Peor. Sie W., CMC, M.A, D.Se., Fitzroy Ter, Prospect, SA. Mitcee1, Paor, M. L, a. M Se. University, A MitcHeiw, F. J., c/o The South Austrafian Museum, North Terrace, Adelaide, Moonnouse, F, W., M.Sc., Chief Inspector of Fisheries, Flinders Street, Adelaide. *MounTFoRD, Cc. P., 25 First Avenue, St. Peters, Adelaide. Mourrew., J. W., Engineering and Water Supply Dept, Port Road, Thebarton, S.A Neat-Suirtna, C. A., B.Agr.Sci., 16 Gooreen Street, Reid, Canberra, A,C,T. Niwnes, A. R,, B.A, 62 Shetheld Street, Malvern, 5.A. *Nortucore, K. H,, B.Agr.Sc., A.T.A.S., Waite Institute Cena Mail Bag), Adelaide. Ocxenoen, G. P., "B.A, Schoal House, Box 63, Kimba, S.A. *Orpner, I. L., 65 Fifth Avenue, St. Peters, S.A. *Oszonn, Pror. T. G. B., D. Se., Department of Botany, Oxford, England—Counedl, 1915-20, Ba President. $925-26-- Vice-President, 1924-25, 1926-27, *Paruin, L. Me Sc, ¢/o North Broken Hill Mining Co., Melbourne, Victoria. Parxinsox, K ‘a B. Sc, 8 Mooreland Avenue, Beverley, SIA. Patrrson, G., 68 Partridge Street, Glenelg, S.A- PAuLL, A. G, 10 Millon Avenue, Fulfarton Estate, S.A . *Prrra, C. S,, 'D.Sc.. Waite Institute (Private Mail Bag}, Adelaide—Council, 1941-435; Vice-President 1943-45, 1946-47 President. 1945-46. Powrtr, J. K. . BSc, CSIRO., Division of Biochemistry, University, Adelaide. Poynton, J. “O., MD. MA. ChE, MRCS, LRCP, Institute Medicine, Vet Science, Frome Road, Adelaide. Pratrr, R. G., 81 Park Terrace, North Unley, S ’ *Paescorr, “PROF. j. A, CBE, DSe., ALC, PES. Waite Instinite (Private Mail Bag), Adelaide—V’erco Medai, 1938; Council, 1927-30, 1935-39; Wice-President, 1930-32; Evendent 1932-33, Parcs, A. G., M.G., M.A., Litt.D., F.R.GS,, 46 Pennington Tersate, North Adelaide, Pryor, L. D., se Dip. For., 32 La Perouse Street, Griffith, N.S.W. *Rarmcay, J. H, B.Sc., Bureau of Mineral Resources, Melbourne Building. Canberra, Raysen, P., B. Se) Bos, 111, SA. Riceman, D. S., M.Sc., B.Agr. Sc, CSLRO, Division of Nutrition, Adelaide, Rienen, Ww. R, BSc, Oceanographic Institute, Gettenburg, Syeeden. *Rimes, ‘ D., B.Sc., 24 Winston Avenue, Clarence Gardens, S.A. Rex, C. E., 42 Waymouth Avenue, Glandore, S.A, *Restnson, E.G, M.Sc. 42 Riverside Drive, Sudbury, Ontario, Canada. 2 Date of Election 1953, Rocers, W. P., Ph,D., Zoo! ent University, Adelaide, ter Baath, LD cfg Huh Scawl, Port Pita, SA 195%, Rows, S.A, 22 Shelley Street, Firle, SA. 1951. E,, B.Sc, 22 Shelley Street, Firle, S.A. 1950. voo, Pror. E A. B.Sc, A.M,, University, Adelaide, S.A. 1945. Rv, J. R,, ne Penola Estate, Penola, S.A. 1944, *Sannars,,. Miss D B,, M.Se,, University of Queens; vie Brisbane, Queeosland. 1950, Saunneys, F. L., ‘99, Winchester Street, Malvern, 1933. Scuwmmex, M., MB, B.S, 175 North Ter, Adel 1951, Seorr, T. D,, Be c/o S.A. Museum, North. Terrace, Adelaide, S.A. 1946. *Sranrt, E. R, M.Sc., C.S.LR.O., Division. of Industrial Chamistry, Box 4331, G.P.0, 1924, *5 Metbbunie, Viet BSc, En and Water. Supply Vi ‘ EGNIT, G5 gwineer ater, Supp! trnent, ictoria Square, Adelaide—Se feretary, 1930- recone 1937-38; Vice Bes ident, 1938-39, 1940-41; President, 1939-40, 1925. *Sueaap, H., Port Elliot, $.4. 1936. *SHkaAgy, K., Fisheries Research Div, C_S.1.R.0., Universi a De of on Medians, W.A, 1945. SHEPHERD, ‘T. H,, M.Sc, B.A, ¢/o Anglo-Weatralian 1934. Suinxrievo, R. Cc. Salisbury, 5-A- 1924. Simpson, F. N., Pirie Street, Adelaide. 1949. Simpson, dD, A, M.B., B.S., 42 Lockwood Road, Burnside, S.A. 1941. *Suire, T. 1, B.Sc, Regional Planning Section, Department of National Develop- ment, Canberra, A, CT 1M]. *5ourecoir, R. V., M.B., B.S., D.T,M. & H., 13 Jasper Street, Hyde Park, S.A— Couneil, "1948-51; Treasurer, 1951-_ 1936. Sourn won, A.R, ‘M.D., M.S. (Adel), M.R.C.P., Wootestig Ter., Glen Osmond, §.A, 1947, ean K 1. Ly MSc., 15 Main Ro d, Richmo nd, S:A.—Council, 1951+. 1936. +*Spzicc, RC. "MSc. ” Mines Menarinent Flinders Street, Adelaide. 1951. STEADMAW, Rev. W. R, 8 Blairgowrie Road, St. Georges, S.A, 1947. Spurinc, ML. B., BA Sc, Agricultural College, Roseworthy, 5.A. 1949, *Spry, A. H., B.Sc., 63 LeFevre Terrace, North Adelaide, S.A. 1938. *STEPHENS, ¢ at D.Se,, Waite Institute (Private Mail Pag), Adetaid 1935. Srrickianp, A. G, M.Agr. Sc., 11 Wootoona Terrace, Glen Osmond, SA —Council, 1947, 1932. Swan, D. C, M.Sc, Waite Institute (Private Mail Bag). Adelaide—Secretary, 1940-42 ; Vie Eeeeleaet, 1946-47, 1948-49; President, 1947-48, 1M8, Swann, F. J. W., 38 Angas Road, Lower Mitcham, S.A. 1931. Swirsxt, P,, Mag. Sc, 22a Henry Street, Croydon, $.A- 1934. Symons, 1, G. 35 anreas Street, Lower Mitcham, S.A—Editor, 1947-, 1929. *Taveor, J. K., B.A, MSc., Waite Institute (Private Mail Bag), Adelaide—Counecsl, 1940-43, 1947-505 "Librarian, 1951. 1950. Tavuor, G. H., BSc, Department of Mines, Old Legislative Council Building, North Terrace, Ads S.A. 1948. eons, I. M, M.Sc. (Wales), University, Adelaide—Seerelary, 1948-50; Council, 1938, *THomas, Mrs, I, M. Mn e P, M. Mawson), M.Sc., 36 King Street, Brighton. 1940, THomson, Capt. J. M. 138 Military Road, Semaphore South, 1923. *Tinnare, N. B., BSc, South Australian Museum, Adelaide—Seeretary, 1935-36; Corned, 1946-47 : Vice-President, 1947-48, 1949-50; President, 1948-49 7945, . §, M.Sc, B.AgrSc., Waite Institute (Private Mail Bas), Adelaide. 1937. *TRUMILE, Prov. H. Cy D.Sc, M.Agr.Sc., Waite Institute (Private Mail Bag), Adelaide—Council, 1942-1945 ; Pice-President, 1945-46, 1947-48; President, 1946-47. 1925. Turner, D, C, Brookman ' Buildings, Grenfell Street, Adelaide, 1950. Vuerca, S, T, Port Lincola, 8 S.A. 1912. *Warp. L. K., 1.S.0., B.A., B.E. D.Se.. 22 Northumberland Avenue, Tusmore—Counciél, 1924-27, 1033, 353 Vice- President, 1927-28: President, 1922-3), 1941. *Warr, D. C., Agr. Se, Div, Plant Industry, C.S.LR.0,, Canberra, A.C.T, 1936, WATERHOUSE, Miss L. M, 35 King Street, Brighton, S.A 1953, Waterman, R, A, BA., M.A., PhD.. North-western University, Evanston, Thinois, As S.A, 1954. Wens, B. P., B.Sc., Geologist, Mines Departs, onaee 1954. Wetns, C. B., ae Sc, Research Officer, C.S.LR Soils ‘Division, Adelaide. 2939, *Wrenrnc, Rev. B J. 5 York Street, Henley Beac . 1949, *Weoener, C. F., B. Se, Department Mines, Flinders Street, Adelaide, S.A. 1954. Warrecaw, A. I, B.Sc., C/o. Adelaide Boys High School, Adelaide. 16, WHrTLe, A. W. 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Wooptanps, Harotp, Box 989 H, G.P.O., Adelaide. 1945. Worruuey, B. W., B.A. M.Sc., A. Inst. P., University, Adelaide, 1948. *Wymonp, A, P., B.Sc., 4 Woodley Road, Glen Osmond, S.A. 1949. Yeates, J. N., L.S. AM.LE, A.M.LM.E, Richards Buildings, 99 Currie Street, Adelaide, S.A. 1944, Zier, W. J., Dip.For., F.L.S. (Lon.), 7 Rupert Street, Footscray West, W.12, Vict. 221 GENERAL INDEX [Names in italics indicate that the forms classified are new to science] Centenary Addresses, i-xiy Angel, L. Madeline: Parorchis acanthits var. australis, n. var., with an Account of the Life Cycle in South Australia Australonereis ehlersi, 19 Babiangia bulbifera, 98 Bowes, D. R.: The Metamorphic and Igneous History of Rosetta Head, South Aus- tralia, 182-214. Boydaia derricki, 65 Ceratocephala edinondst, 23 Cleland, J. B., and N, B. Tindale: The Eco- Jogical Surroundings of the WNealia Natives in Central Australia, and Native Names and Uses of Plants, 81-86 Eight New Species of Trombiculidae (Aca- ra) from Queensland: H. Womersley, 67-80 Fuschongastia parva, 74; E. popet, 76; E. procang, 77; E. andromeda, 80 Hansen, Tan V.: An Account of the Negalia Initiation Ceremonies at Yuendumu, Cen- tral Australia, January 1953, 175-181 Hartman, Olga: Australian Nereidae, 1-41 Hossfeld, Paul §.: Stratigraphy and Struc- ture of the Northern Territory of Aus- tralia, 103-161 ichthyostrongylus clelandi n,g., n.sp., from an Australian Shark: Patricia M. Maw- son, 162 Ludbrook, N. H.: The Molluscan Fauna of the Pliocene Strata underlying the Ade- laide Plains, Part I, 42-64 Mawson, Patricia M.: Ichthyostrongylus cle- lendt nog, nosp, fromm an Australian Shark, 162 Metamorphic and Igneous History of Rosetta Head, South Austraha: D. R, Bowes, 182-214 Micromereis halei, 25 Molluscan Fauna of the Pliocene Strata underlying the Adelaide Plains, Part I: N, H. Ludbrook, 42-64 Mountford, Charles P.: A Carved Human Figure from the Durack Range, north- western Australia, 87 Nercidae, Australian; Olga Hartman, 1-41 Nealia Natives in Central Australia, Ecologi- cal Surrotindings of: J. B. Cleland and N. B. Tindale, 81-86 Negalia Initiation Ceremonies at Ytrendumu, Central Australia, January 1953; An Account of the: Ian V. Hansen, 175-181 Neotrombidium barringunense, 89-97 Northern Territory of Australia, Strati- graphy and Structure of: Paul S. Hoss- feld, 103-161 Parorchis acanthus var. australis, n. var., with an Account of the Life Cycle in South Australia; L. Madeline Angel, 164-174 Rosetta Head, South Australia: The Meta- morphic and Igneous History of: D. R. Bowes, 182-214 Stratigraphy and Structure of the Notthern Territory of Australia: Paul S. Hoss- feld, 103-161 Sauthcatt, R. V.: The Genus Neotrombidium (Acarina: Leeuwenhoekiidae), I, Descrip- tion of the Ovum and Larva of Neo- frombidium barringunense Hirst 1928, with an Account of the Biology of the Genus, 89-97 Southcott, R. V.; Description of a New Genus and Species of Larval Trombiculid Mite from New Guinea, 98-102 Trombicula derricki, 67; T. antechinus, 69; T. thylogale, 71; T. Mackayensis, 72 Tindale, N. B., J. B. Cleland and: The Eco- logical Surroundings of the Nealia Natives in Central Australia and Native Names and Uses of Plants, 81-86 Womersley, H.: Atother New Species of Boydaia (Speleognathidae, Acarina) from Australia, 65 Womertsley, TI: light New Species of Trombiculidae (Acarina) from Queens- land, 67-79 CONTENTS CENTENARY MEETING, 24 September 1953— Dickinson, 5. B.: Centenary of the Society Rocers, W. P.: The Biological Sciences .... Prescorr, J. A.:-Agricultural Sciences Mawson, D.; The Role of Geology in the Activities of the Society HartMan, Orca: Australian Nereidae Lupsroox, N. H.: Molluscan Fauna of the Pliocene Strata underlying the Adelaide ; Plains Womerstey, H.: Another New Species of Boydaia (Speleognathidae : Acariua) from Australia Womerstey, H.: Eight New Species of Trombiculidae (Acarina) from Queens- land CieLann, J. B., and Trxnare, N. B.: Ecological Surroundings of the Ngalia Natives in Central Australia and Native Names and Uses of Plants ... Mountrorp, C. P.: A Carved Human Figure from the Durack Ranges, North- western Australia i Pe: Sourncorr, R. V.: The Genus Neotrombidium (Acarina :_Leeuwenhoekiidae) I, Description of the Ovum and Larva of Neotrombidium Barringun- ense Hirst 1928, with an Account of the Biology of the Genus .... Soutucorr, R. V.: Description of a New Genus and Species of Larval Trom- biculid Mite from New Guinca Hossrerp, P. S.: Stratigraphy and Structure of the Northern Territory of Australia Mawson, Partricra M.: Ichthyostrongylus clelandi, n.g., n.sp., from an Aus- tralian Shark ANGEL, L, Mapettne: Parorchis acanthus var. australis, n.var., with an Account of the Life Cycle in South Australia Hansen, tan V.: An Account of the Ngalia Initiation Ceremonies at Yuendumu, Central Australia, January 1953 Bowes, D. R.: The Metamorphic and Igneous History of Rosetta Head, South Australia eee Page i—iii iv—vi Vii—xi xii—xiv 1—41 81—86 87—88 89—97 98—102 103—161 162—163 164—174 175—181 182—214 i ee i oe