Beyrichicopids and kirkbyocopes are represented in the Early Carboniferous benthic ostracod fauna of the Bonaparte Basin by at least 29 species referable to 18 genera (including two that are probably new, but unnamed). The described number of species are distributed among the ostracod families. Of the species described, eight are new (Libumella bonapartensis, Welleriella atypha, Malnina spinosa, Coryellina excaudata, C.robertsi, Selebratina serotina, Tetrarhabdus dictyon, and Scrobicula inaequalis), eight are closely related to, if not conspecific with, established taxa [Pseudoleperditia cf. venulosa, Coryellina cesarensis, Kirkbya aff. lessnikovae, K. aff. quadrata, Amphissites aff. centronotus, A. umbonatus, Kirkbyella (Berdanella) quadrata, and Scrobicula aff. inaequalis), and 13 are placed in open nomenclature, most of which are comparable with previously described taxa. The morphological similarities of the extinct Kirkbyacea and the extant Punciacea are discussed, and possible homoemorphic resemblances between them are considered. Detailed SEM examination of the reticulation pattern of the kirkbyacean species Amphissites sp.B revealed the results of epidermal cell-division during the ecdysis between the A-I stage and the presumed adult stage. Mitosis of the epidermal cells not only increases the valve surface area, but also initiates carinae by the fusion of adjacent muri of twin fossae. An interim biostratigraphic scheme for the Early Carboniferous sequence of the Bonaparte Basin consists of a succession of eight ostracod assemblages that are based on the first appearance (in ascending order) of the following species: Welleriella atypha, Coryellina robertsi, Shivaella cf. armstrongiana, Coryellina cesarensis,. Malnina spinosa sp. nov., Selebratina serotina, Scrobicula inaequalis and A mphissites sp.B. The scale of assemblages is controlled by conodont and foraminiferal zonations, and is calibrated against the Dinantian time-scale. So far, the atypha, robertsi and armstrongiana Assemblages have been recognised in the Early Carboniferous (Tournaisian) sequence of the Canning Basin. The major affinities of the Early Carboniferous beyrichicopids and kirkbyocopes from the Bonaparte Basin are with cognate species from Western Europe (Belgium, northern England), the Russian Platform, Kazakhstan, and Tibet. North American affinities are of minor significance. In general terms, the entire Early Carboniferous ostracod fauna from the carbonate shelf sediments of the Bonaparte Basin belongs to the Bairdiacea-Paraparchitacea ecozone, suggesting warm climatic conditions. The Tournaisian (Burt Range Formation; Septimus Limestone) faunas may include ecologically mixed assemblages, i.e., marine nearshore and shallow offshore, but the palaeoecological studies needed to test this model must await the description of the total Early Carboniferous ostracod fauna. The Visean (Utting Calcarenite) Kirkbyacea are as frequent (in species abundance) as the Paraparchitacea, both superfamilies ranking second to the Bairdiacea; a proportion indicative of open-marine shallow offshore conditions.

A collection of geological papers from 1970-71.

New Ireland is a narrow island 360 km from northwest to southeast and up to 48 km wide. The broader southern part of the island is steeply mountainous, with peaks to 2400 m above sea level in the Hans Meyer Range, and is diagonally bisected by the Kamdaru and Weitin valleys. The central and northwestern parts of the island are extensively capped by limestone plateaux which are tilted to the north-northeast. The plateau in the northwest is known as the Schleinitz Range, and the higher plateau in the central region is the Lelet Plateau. A low saddle separates the Lelet Plateau from the southern mountains. Outcrop is generally poor and extensively weathered beneath the dense primary rainforest that blankets the island, though entrenched river gorges provide some good, though relatively inaccessible, sections. The oldest rocks are the lower to middle (or lower upper) Oligocene Jaulu Volcanics. These consist of lapilli tuff, agglomerate, and subordinate porphyritic pyroxene andesite lava, and are intruded by gabbro, norite, diorite, tonalite, trondhjemite, granodiorite, and leucocratic dyke rocks, which have been named the Lemau Intrusive Complex. Some or all of these intrusives may be related to the Jaulu Volcanics; K/Ar ages are 31.8Â} 1.0 m.y., 17.5 Â} 0.6 m.y., and 13.8 Â} 0.5 m.y. The Jaulu Volcanics and Lemau Intrusive Complex are best exposed in southern New Ireland, where erosion has been deepest. Elsewhere they are exposed only along the southwestern fall of the ranges, where the limestone plateaux have been removed by erosion. The upper lower Miocene Lossuk River Beds are a thin series of clastic sedimentary rocks derived from the Jaulu Volcanics, which they unconformably overlie, and are found only in the northwest. The main limestone units are the Lelet Limestone, which forms the plateaux in the centre and northwest, and the Surker Limestone in the south. The two were probably partly lateral equivalents, but the Lelet Limestone has a longer range (lower Miocene to Pliocene or Pleistocene, compared with lower to middle Miocene). The narrow neck of land between the outcrop areas of Lelet Limestone in the northwest and Surker Limestone in the southeast is largely occupied by uppermost Miocene volcaniclastic (partly turbidite) and biogenic ooze sediments of the Rataman Formation, which are probably deep-water contemporaries of higher beds of the Lelet Limestone. The white, chalky Punam Limestone unconformably overlies the Rataman Formation along a narrow strip of the foothills near the northeastern coast of south-central New Ireland. It is Pliocene or younger. Embayments in the Punam Limestone are filled with Plio-Pleistocene sediments of the Uluputur Beds, which comprise intraformational conglomerate, lithic sandstone, and siltstone. A thick succession of fanglomerate and beach sands, in places cemented to conglomerate and sandstone, flanks eastern and western coasts of the southern, mountainous part of the island. These sediments, named the Maton Conglomerate, unconformably overlie the Jaulu Volcanics, from which they were derived, and also overlie in places the Rataman Formation and Surker and Punam Limestones. The conglomerate is overlain only by Pleistocene to Holocene coral terraces. The Weitin and Sapom Faults are the major structural features on New Ireland. Movement on the Weitin Fault may be left-lateral. New Ireland developed presumably on oceanic crust by seafloor (and possibly subaerial) volcanism in the early and middle Oligocene. A landmass emerged in the early Miocene, when the Lossuk River Beds were deposited, and then probably subsided steadily throughout the Miocene and early Pliocene and was rapidly uplifted in the late Pliocene and Quaternary, when a flight of terraces on the northeastern fall of the Lelet Plateau was probably cut by wave-erosion. Left-lateral faulting and crustal extension (?transform faulting) in the late Miocene may have opened a rift between central and southern New Ireland, in whic

pt. 1. Igneous and metamorphic -- pt. 2. Sedimentary rocks -- pt. 3. Igneous and metamorphic

The Kubor Anticline began as a basement fold on the northeast margin of the Australian continental block in Palaeozoic time. It is bounded in the north by the New Guinea Mobile Belt (Bain, 1973; Dow et al 1973), a tectonically active zone within younger continental crust which accreted to the northern edge of the continent in Mesozoic time. Uplift of the northern edge of the older continental block resulted in gravity sliding, folding, and thrusting of the overlying Tertiary and uppermost Mesozoic rocks (Papuan Fold Belt), but the basement and the lower part of the cover rocks were only broadly folded and faulted (e.g. Kubor Anticline). Within the Mobile Belt the rocks are strongly deformed and intensely faulted. The oldest rocks exposed are low-grade greenschists formed by regional metamorphism of sedimentary and volcanic rocks of probable Palaeozoic age (Omung Metamorphics). They crop out only in the core of the Kubor Anticline, where they are intruded by acid to basic large plutons and small stocks (Kubor Granodiorite) of probable Late Permian age.In the west and northeast, the Kubor Granodiorite is conformably overlain by small patches of Upper Permian or Triassic limestone and arkose (Kuta Formation). Upper Triassic dacites and basalts (Kana Volcanics) are also unconformable on the metamorphic and plutonic rocks, but are not in contact with the Kuta Formation.The basement, Kuta Formation, and Kana Volcanics are overlain unconformably by the upper part of the Wahgi Group (about 7000 m of Upper Jurassic to Upper Cretaceous clastic and volcanic rocks), and the same sequence forms the limbs of the anticline.The southern and western limbs of the Kubor Anticline are overlain with paraconformity by upper Palaeocene? mudstone and sandstone (Pima Sandstone) and Eocene-Oligocene limestone (Nebilyer Limestone) respectively. At the east end of the northern limb, the Upper Cretaceous rocks are overlain with slight unconformity by about 300 m of Eocene-Oligocene foraminiferal limestone (Chimbu Limestone), which forms the base of the sequence in the Yaveufa Syncline. The Eocene-Oligocene limestones are everywhere overlain by Miocene limestone or elastics. The Nebilyer Limestone at the western closure of the Kubor Anticline is overlain by fine elastics with interbedded limestone, marl, and mudstone (Aure Beds) which grade southwards into massive shelf limestone (Darai Limestone).The northern limb of the Kubor Anticline is cut by the Bismarck Fault Zone along the southern margin of the New Guinea Mobile Belt. The Bismarck Fault Zone is 20 km wide and consists of a disturbed zone of subparallel anastomosing faults, thrusts, and tight overturned folds. There is at least 3000 m of vertical displacement (north side up) spread over the width of the fault zone in the vicinity of Mount Wilhelm. No economic mineral deposits are known in the Kubor area.

This Bulletin describes the brachiopod fauna of the Devonian and Carboniferous (Frasnian to early Namurian) platform sediments of the Bonaparte Gulf Basin in northwestern Australia (Fig. 1). It is part of a comprehensive study of the Bonaparte Gulf Basin begun by the Bureau of Mineral Resources in 1963, and follows an earlier study by Thomas (1970), started in the mid-1950's, on brachiopods from the Carnarvon, Canning, and Bonaparte Gulf Basins. Thomas's material from the Bonaparte Gulf Basin, with the exception of that from the Septimus Limestone at Mount Septimus, came largely from samples collected in reconnaissance surveys. Other earlier work on brachiopods from the Bonaparte Gulf Basin includes that of Veevers (1959b) on rhynchonellids and a productacean, and Thomas (1965) on Delepinea. A comprehensive description of the Devonian and Carboniferous geology of the basin is given by Veevers, Roberts (1968).

This Bulletin presents the taxonomy, temporal stratigraphy, palaeogeography, and ecology of the Middle Cambrian agnostid trilobites beginning with their arrival in the Templetonian and reaching an acme of diversification in Undillan time; agnostids of the latest Middle Cambrian were described earlier (bpik, 1961b, 1967). The material described now contains numerous complete specimens which supplied information regarding the morphology and function of the agnostid skeletons so far not attainable with certainty from disjointed sclerites. The nine named and one unnamed (the initial Templetonian) zones are integrated into four geographically named stages, completing the scale of stages by starting with the Ordian and leading into the early Upper Cambrian the. continuous sequence of stages reads; Ordlan, Templetonian, Floran, Undillan, Boomerangian; followed by the early Upper Cambrian Mindyallan and Idamean. The scale of the zones of the agnostid species is the pivot of the biostratigraphic documentation; it is the time scale A. H. Westergaard introduced in 1946 in Sweden. I have implemented this scale in Australia in the field and in unpublished and published reports for over two decades, but 'on parole', in advance of the descriptions and illustrations of the relevant fossils which are presented here.

Legacy product - no abstract available

Standard curves for the interpretation of magnetic anomalies due to thin finite dykes were computed for various ratios of dyke length (measured down the dip) to depth of burial. Families of curves for a given field inclination and dip of dyke are produced for various ratios of dyke length to depth of burial. The curves so produced are suitable for interpretation of anomalies in the intensity of the vertical, horizontal, and total field.

The Victoria River region, in the northwestern Northern Territory, is underlain by Precambrian rocks and flanked to the east, south, and west by Lower Cambrian volcanics and younger sedimentary rocks. The Precambrian rocks include a deformed belt of basement metamorphics, granites, and acid volcanics, all overlain by sandstone, in the northwest; and a stable platform (the Sturt Block) overlain by slightly deformed sedimentary rocks in the centre and southeast. The rocks in the deformed belt range in age from Archaean to Adelaidean (late Proterozoic). On the Sturt Block are several Proterozoic groups of sandstone, siltstone, and dolomite. The sequences developed are all shallow-water deposits, and are separated by several regional unconformities. They are overlain by late Adelaidean tillites and associated fluvioglacials. Only minor production of tin, gold, and barite has been recorded, and the major resource presently being exploited is groundwater.