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The Precambrian Rocks of Tasmania, Part I, Dolerites of the North-West Coast of Tasmania

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The Precambrian Rocks of Tasmania, Part I, Dolerites of the North-West Coast of Tasmania PAPERS AND PHOCEEDINGS OF TlIfti ROYAL SOCIF~TY OF TASMANIA, VOLUME 91 THE PRECAMBRIAN ROCKS OF TASMANIA, PART I, DOLERITES OF THE NORTH-WEST COAST OF TASMANIA By ALAN SPRY Department of Geology, University of Tasmania (With 4 Text Figures and 2 Plates) ABSTRACT Previous Literature At least 30 small bodies of dolerite have been The presence of these basic dykes was first found intruding sediments of the Pre-Cambrian recorded by Twelvetrees 0903, 1905) who found Rocky Cape Group along the coast between Sulphur them at Burnie, Boat Harbour and Rocky Cape. Creek and Crayfish Creek. The igneous bodies are Stephens (909) also briefiy mentioned the same chiefly sills although dykes also occur. The bodies in his notes on a traverse along the north­ dolerites are characterized by strong deuteric alter­ west coast. ation which led to the formation of secondary tremolite-actinolite, chlorite, zoisite, albite, calcite, sericite, sphene, leucoxene, serpentine, and prehnite. COUNTRY ROCKS These rocks show petrological and chemical affini­ ties with dolerites of a similar age in Western The dolerites intrude a group of unfossiliferous and South Australia. They have certain features sediments which extend from Penguin to Smithton. in common with the lavas of the Cambrian Dundas These sediments consist chiefly of quartzites and Group, but the possibility that these bodies acted slates with siltstones, dolomites and a little con­ as feeders to the flows is discounted on structural glomerate. They were referred to broadly as the and chemical grounds. "Rocky Cape quartzites" by Twelvetrees (1903, 1905), but examination now shows that the sedi­ ments constitute a group. Thus the Rocky Cape INTRODUCTION Group is here defined as those sediments, chiefly quartzites, slates, dolomites and siltstones outcrop­ The dolerites occur as small bodies, ranging in ping intermittently from Penguin to Smithton and size from a few inches to 400 feet in thickness lying unconformably below the Dundas Group (at and, as they are less resistant to weathering than Penguin). Its thickness is in excess of 10,000 feet the sediments they intrude, most are only revealed and while the detailed stratigraphy is not yet in the coastal rock platform. They outcrop sporadi­ known, a number of formations have been recog­ cally along the coast from Blythe Heads to Crayfish nized. A small area of coarse mica-schist along the Creek, but the greatest concentration is between Inglis River, shown in fig. 1, may lie unconformably Burnie and Cooee Point so that it is intended to below this group but the base of the Rocky Cape use the term Cooee Dolerite to refer to this group Group has not yet been seen. The formations are of igneous rocks as a whole. It is believed that discussed in order (tentative only) from oldest to similar rocks occurring in the vicinity of French­ youngest. man's Cap are part of this group and that as mapping of the Pre-Cambrian continues, more will be found. The Cooee Dolerites thus represent a distinct period of igneous activity, probably late in .Burnie Quartzite and Slate the Pre-Cambrian. Evidence shown later in this This formation contains those quartzites and paper indicates that the Middle to Upper Cambrian slates outcropping along the foreshore at West volcanism was a later and distinct episode. A Burnie. It appears to outcrop from east of Howth widespread period of basic to ultrabasic activity to Doctor's Rocks, except where covered by a super­ earlier in the Pre-Cambrian is represented by ficial layer of later material. The formation is amphibolites, &c., and the Interview River dyke probably several thousand feet thick and consists swarm described by Spry and Ford (957) belongs mostly of a monotonous repetition of thin slates to this episode. and quartzites. The argillites are dark-grey to black siltstones or slates which show a cleavage which is strongly developed in some specimens but Acknowledgements lacking in others. Some contain abundant clastic The author is grateful to W. St. C. Manson of the mica and others are graphitic. Many of the coarser Tasmanian Department of Mines who carried out siltstones exhibit cross-bedding, scouring and other the four chemical analyses which are published by intraformational structures. The quartzites are courtesy of the Director of Mines. B. May and A. generally light-coloured, quartzose, and massive, Rundle assisted in the field work. flaggy or thinly bedded with occasional cross bed­ For "Pre-Cambrian" read .. Precambrian" throughout the paper. 81 R.S.-6. 00 l" RECENT ~ ALLUVIUM d BEACH SANDS SEE FIG TERTIARY ~BASALT, SCALE 0,, $E.DlfiJENrS o 2 4 6 8 MILES ! I ! j =:d PERMtAN SEDIMENTS ." ORDOVICIAN :>;l t<J (") 10,/'"00 IOWEN CONGLOMeRA TE > HARBOUR '< PRECAMBR!AN @ :>;l CAPE I.~D I DOLERITE ;; Z ~ ROCKY CAPE GROUP :>;l o ~SCHlsr (") i"j rn o 5678 SPECtMEN NUMBERS "l STRIKE AND DIP >-3 >rn ;x ANTICL!NE ;;:: > Z F :; :>;l >-3 FIG. I.-Regional geological map showing the, distribution of the Precambrian reeks and in particular of the dolerites. Some boundaries after Loveday (1956). ALAN SPRY 83 ding. Thin sections of many quartzites show that Bluff Quartzite they contain angular quartz fragments and this fact, together with their association with some beds This is a 1500 foot thick quartzite, light in colour, of sub-greywacke, indicate that they are not normal thinly bedded at the top, but massive towards the ortho-quartzites (Pettijohn, 1949). Some arenite base, with coarse cross-bedding and ripple marks layers contain abundant angular slate fragments (plate D. It overlies the Cowrie Siltstone and lies up to eight inches long and the location of these below the Port Quartzite and Slate. It is litho­ intraformational breccias is shown in fig. 3. logically indistinguishable from the Cave Quartzite (defined below) and this causes great difficulty in The lack of recognizable marker horizons, to­ mapping this area. gether with the close folding and faulting (see fig. 3) prevents the accurate measurement of the' thickness of this formation. The beds generally dip to the west (see fig. 1), but small folds are abundant and these are asymmetrical with the steeper limb Port Slate and Quartzite either to the east or west, but with a general fiat plunge in a direction 230'. Faults are common and This formation is named after the small harbour cause difficulty in interpreting the structure, and on the eastern side of Rocky Cape, this being shown are frequently associated with zones of contortion. as "The Port" on old maps of the area. It lies between the older Bluff Quartzite and the younger The phyllites at Somerset are more altered and Cave Quartzite. It consists of 1500 feet of alter­ are strongly cleaved with a distinct lineation due nating slates and quartzites. The argillites are grey to crenulation, but there appears to be a complete to black laminated slates and slatey siltstones con­ transition into the less altered beds at Burnie. taining abundant intraformational structures such These phyllites are overfolded towards the south as sandy lenses, mud pellet conglomerate and slump in the quarry on the Somerset-Waratah road, half structures. The quartzites are generally thinly a mile south of Somerset and several other places bedded. on the wave-cut platform near Somerset. Black River Dolomite The Burnie Slate and Quartzite is separated Cave Quartzite from the sediments in the Rocky Cape area by a cover of Permian sediments and Tertiary lacustrine The quartzite which forms the extremity of Rocky beds and volcanic rocks, consequently the relation­ Cape is called the Cave Quartzite from the Rocky ships between the sediments of the two areas is not Cape Caves which occur within it. It overlies the known. The oldest bed named in this' paper from Port Slate and Quartzite but the upper limit is not the Rocky Cape area is the thin (50 feet) grey to visible. It consists of 1500 feet of light coloured, buff dolomite which outcrops at the bridge where thickly bedded quartzite with some cross-bedding the Bass Highway crosses the Black River. It is and ripple marks. The quartzite on the cliffs east brecciated and silicified in parts. A small area of of Sisters Beach and at Jacob's Boat Harbour is dolomite at the eastern end of Sisters Beach may be probably this formation. Exposed in a raised sea the same formation. The Black River Dolomite cave half a mile east of Sisters Beach is a conglom­ underlies the Cowrie Siltstone and overlies the un­ erate which is named the Sisters Conglomerate, named siltstones which occur to the south up the being a member within the Cave Quartzite. The Black River where they are folded into a series conglomerate occurs as two closely spaced horizons of anticlines and synclines about half a mile across, one of which is about 18 feet thick and the other with axes running approximately east-west. about three feet thick. There are coarse and fine phases but the well-rounded boulders (which are always quartzite identical with that above and be­ Cowrie Siltstone low) range up to 18 feet long. The type of locality for this and the following The quartzite at the eastern end of Sisters Beach three formations is on the southern part of the is of interest as it contains the only trace of organic western side of Rocky Cape as shown in fig. 3. life in the Rocky Cape Group. Plate II shows a The name is taken from Cowrie Pt. and it is con­ specimen of "worm tracks". sic:ered that the formation occurs all the way along the coast from Rocky Cape to Black River although The Cave Quartzite may be equivalent to the it cannot be proved at present that there is not a Bryant Hill Quartzite named by Carey and Scott fault separating the Cowrie Pt.
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