Tag Archives: geology

Boulder lags in Rosetta Bay at Victor Harbor, South Australia

Overview

The significance of strewnfields of large granite erratics throughout the Inman Valley was discussed in an earlier note (Milnes, 2019). They essentially pinpoint outcrop or subcrop of in-situ glacigene diamictite from which they have been exhumed, or within which they still remain partly encased. The diamictite is generally plastered over smoothed and striated Cambrian Kanmantoo Group bedrock.

Good examples of these boulder lags occur on the beach at Rosetta Bay and were recognized early on as glacial erratics eroded from glacial till (for example, Howchin (1910; Fig. 1). Milnes (2019) located and photographed remnants of the source diamictite underlying these boulder lags (Figs 2, 3). However, recent drone photographs taken in the area by Isaac Forman (Serio.com.au) have shown that significant boulder lags occur on the landward side of Wright Island (Fig. 4) and, based on the forms visible beneath the sea surface, may also exist on the seabed in the Bay between the shore and the Island.

One implication of this observation is that the bedrock (Petrel Cove Formation, Cambrian Kanmantoo Group) is at a relatively shallow depth and that the glacial till from which the boulders were eroded (or within which they may be partly embedded) remains close to the sea floor. Another is that the early held view that the granite landforms (particularly Wright Island and Rosetta Head) were ice-moulded during the Permian glaciation about 300 million years ago is probably correct. And, finally, it may still be possible to find direct evidence of glacial pavements on parts of these granite landforms, like that discovered fortuitously many years ago at Port Elliot (Milnes & Bourman, 1972).

Lag of erratics overlying and being exhumed from diamictite adjacent to boat ramp.

Detail of granite and other boulders (probable erratics forming a lag weathered out of Permian glacigenes).

Fig. 1 (L) – Map from Howchin (1910) showing location of erratics in Rosetta Bay. Fig. 2 (C) -Boulder lag of mainly granite erratics on the beach near the boat-ramp, Rosetta Bay. Fig. 3 (R) – Boulder lag of granite and other rock-type erratics on the beach at Petrel Cove.

SERIO-0796-Wright-Island

Fig. 4 – Isaac Forman (Serio.com.au) drone photo of Wright Island and the seabed on its landward side showing the boulder lag of granite erratics on the landward side of the Island and similar forms on the seabed (centre left).

References

Howchin, W., 1910, The glacial (Permo-Carboniferous) moraines of Rosetta Head and King’s Point. Transactions and Proceedings and Report of the Royal Society of South Australia 34, pages1-12; plates 1-17.

Milnes, A.R., 2019, What’s the significance of the large granite erratics scattered through the Inman Valley in South Australia? https://earthnotesblog.wordpress.com/2019/07/25/

Milnes, A.R., BOURMAN, R.P., 1972), A Late Palaeozoic glaciated granite surface at Port Elliot, South Australia. Trans. R. Soc. S. Aust. 96, 149-155.

Dr Tony Milnes

What’s the significance of the large granite erratics scattered through the Inman Valley in South Australia?

Leave a reply

Overview

The earliest studies of glacial sediments and landforms of the Inman Valley, starting with Selwyn (1859), made much of the smoothed and striated bedrock pavements (which we now know to have been generated by the westward movement of ice sheets from continental regions that abutted southern Australia around 300 million years ago), and the large granitic and other erratics scattered throughout the valley. Much of the available information at the time, and hypotheses attached to it, were summarized by Professor Walter Howchin in 1926. Howchin’s map of the Inman Valley showed the locations of large boulder erratics (principally coarse grained, porphyritic granite similar to that exposed along the coast at Encounter Bay) and striated bedrock pavements, on which the directions of movement of the glacial ice could be measured. As might be expected, in-situexposures of glacigene sediments were observed directly overlying the pavements in some of these localities. Howchin remarked on the fact that changes in the courses of the Inman River and subsidiary streams over time continued to variously expose and also obscure rock pavements and overlying glacial deposits, and this situation has continued to the present day.

As well as at sites at which conspicuous large erratics occurred and striated bedrock pavements were located, Howchin assigned the sedimentary fill throughout the Inman Valley and adjacent areas to ‘Permo-Carboniferous’ glacigene deposits. This was partly due to borehole data that indicated diamictitic fill above bedrock in parts of the valley, but also because there were exposures of diamictite associated with the scattered striated pavements and erratics shown on his map (Fig. 1). This view was promulgated by successive geologists and dominates even the most recent geological maps of the area. However, as pointed out by Bourman & Milnes (2016), the fill in the valley is complex. It includes the remnants of glacigene deposits extensively eroded and reworked during Mesozoic and Cainozoic times as well as younger fluvial and alluvial deposits such as the peaty sediments of Pleistocene marshlands and sandy sediments resulting from post-European settlement erosion and aggradation. The soils map of the area (Fig. 2) is a good indication of this complexity as it presents at the modern landsurface.

: Enhanced map of ‘greater’ Inman River valley by Howchin (1926) showing his locations of erratics (red dots) and striated pavements (with directions of ice movement – purple arrows). Region coloured in yellow was assigned to ‘Permo-Carboniferous glacial’ deposits; other coloured areas are bedrock of various types and ages.

: Map of soils in the Inman Valley & surrounds showing locations of erratics (red dots – Howchin 1926; purple dots – recent field observations). Yellow indicates the dominant soil type – ‘G3: Thick sand over clay’ which corresponds closely to Howchin’s ‘Permo-Carboniferous glacial’ deposits and is promulgated on recent geological maps on which the soil mapping was based. Red = areas of ‘L1: Shallow soil on rock’ where bedrock is exposed or close to the surface on the steep slopes. Green = areas of ‘K: shallow to moderately deep acidic soils on rock’. Brown colours = areas of ‘F2: Sandy loam over poorly structured brown or dark clay’ soils, ‘E3: Brown or grey cracking clay’ soils, and F1: Loam over brown or dark clay in the modern stream valleys.

Erratic strewnfields

Recent field observations demonstrate that the strewnfields of large, mostly granite erratics (Howchin’s 1926 map, to which there are more recently added occurrences shown in Fig. 2), essentially pinpoint outcrop or subcrop of in-situglacigene diamictite from which they have been recently exhumed, or within which they still remain partly encased. The diamictite is generally plastered over smoothed and striated Cambrian Kanmantoo Group bedrock and may be ‘lodgement till’. Good examples of this are on the beach at Rosetta Bay, in dam excavations east of Mt Alma road, in the Inman River channel at Inman Valley township and for some kilometres eastwards, and at the site known as ‘Glacier Rock’. Elsewhere, Permian glacigene sediments have long been eroded and substantially reworked, and the granite erratics that have been exhumed from them have largely disintegrated and the weathering products dispersed. The stages in this process can be observed in some granite erratics now being exhumed from glacigene diamictite. Weathering and disintegration of granite erratics in association with Permian glacial diamictites does not occur to anywhere near the same extent in coastal environments, such as on beaches at Rosetta Bay, just north of Port Vincent and at Port Moorowie on Yorke Peninsula, and at Hallett Cove south of Adelaide.

Diamictites

Howchin (1926) referred to the diamictite as ‘.. glacial sandstone and boulder clay..’ and it is quite distinctive, as shown in the accompanying photographs. In locations near the coastline, for example in Rosetta Bay, the diamictite tends to be bluish in colour, with some bleaching and iron-staining, suggesting that weathering is not pervasive. In the main part of the Inman Valley, however, and particularly in the river channel, exposures are generally yellowish-white and bleached of colour. In the earliest reports (Tate et al., 1898), the glacigene sediments were described as being to be so dark in colour that they were thought to be potentially coal-bearing, and this led to exploration drilling of three bores in Back Valley by the Victor Harbour Coal Company. Carbonaceous glacigene sediments are known elsewhere, for example at Port Moorowie on southern Yorke Peninsula, but have not been observed recently in the Inman Valley. The beds of glacial origin that Howchin (1926)²referred to as being typically ‘.. tenacious blue clays..’ have also not been observed recently although the diamictite that is periodically exposed at low tide in Rosetta Bay and which underlies the conspicuous lags of large granite erratics, is bluish in colour.

The sandy-clay matrix of bluish-coloured diamictite is dominantly quartz, with feldspars and muscovite or biotite. Unexpectedly, in the samples examined so far, the clay is dominated by poorly crystalline 14Åmontmorillonitic material: no kaolinite was observed.

Collection of granite erratics in large strewnfield west of Mt Alma road

Lag of erratics overlying and being exhumed from diamictite adjacent to boat ramp.

‘Isolated’ granite and other erratics.

Smoothed & striated bedrock pavement overlain by diamictite containing large granite erratics (dropstones) in valley wall.

$Diamictite beneath erritic lag adjacent to boat ramp. Note blue-grey colour of clayey grit matrix, mabundant small granite and other clasts, goethite staining and carbonate-filled fractures. 50c coin for scale.$

Diamictite beneath erritic lag adjacent to boat ramp. Note blue-grey colour of clayey grit matrix, mabundant small granite and other clasts, goethite staining and carbonate-filled fractures. 50c coin for scale.

Diamictite as in previous photos

1. Strewnfield of large granite erratics west of Mt Alma. 2. Lag of granite & metamorphic rock erratics on diamictite, Rosetta Harbor. 3. Lag of granite & other erratics over diamictite, bed of Inman River, east of village. 4. Disintegrating granite erratic eroding from diamictite, Strangways Hill. 5. Large granite erratic in diamictite on glaciated pavement, Glacier Rock. 6. Large granite & other erratics embedded in diamictite on glaciated pavement, bed of Inman River, east of village. 7. Bluish sandy-clay diamictite (‘lodgement till’) beneath lag of granite erratics, Rosetta Harbor. 8. Bluish sandy-clay diamictite with embedded granite & other clasts, Rosetta Harbor.

Summary

The strewnfields of large granite and other erratics in the Inman Valley are considered to represent vestiges of extensive Permian glacial diamictite. Remnants of these sediments in localities along the north-central and eastern parts of the valley have been exposed close to the ice-moulded bedrock walls and floor that have been progressively exposed by erosion. As downwasting continues, it is expected that the large granitic erratics now exposed in the boulder lags will gradually weather and disintegrate, as is common in terrestrial environments. New occurrences could emerge if riverine erosion exposes more of the original bedrock valley. On the other hand, rising sea-levels may trigger aggradation and the burial of the now exposed strewnfields of erratics, the associated diamictites, and the underlying glaciated bedrock pavements.

Although there have been many investigations of facets of the Permian glaciation, including landforms and sedimentary deposits, starting as early as Selwyn (1859)¹, evidence of post-Permian geological processes in the Inman Valley up until the Quaternary has not been recognised. Some soil mapping linked with Howchin’s (1926) observations and more recent data reported by Bourman & Milnes (2016)²is the most recent information. Opportunities to discover more of the history of this complex landscape clearly exist.

References

Selwyn R.C., 1859, Geological notes of a journey in South Australia from Cape Jervis to Mount Serle, No. 20, p. 4.

Howchin W., 1926, Geology of the Victor Harbour, Inman Valley and Yankalilla districts, with reference to the great Inman Valley glacier of Permo-Carboniferous age. Transactions of the Royal Society of South Australia, 50, p. 89-116.

Bourman, R.P. & Milnes, A.R., 2016, The geology and landforms of the Inman River Catchment. Report to Inman River Catchment Landcare Group, Government of South Australia Department of Environment, Water and Natural Resources, December 2016. 237pp.

Tate R., Howchin W., David T.W.E., 1898, On the evidence of glacial action in the Port Victor and Inman Valley districts, South Australia. Report of Research Committee No. 5, Australasian Association Advancement Science, 7^thmeeting, Sydney 1898, p. 114-127.

Dr Tony Milnes

Sir Douglas Mawson, University of Adelaide

Leave a reply

Overview

Douglas Mawson was born on May 5, 1882 at Shipley in Yorkshire and migrated in 1884 to Australia with his parents Robert and Margaret and older brother William. From 1895 to 1898, William and Douglas attended Fort Street Model Public School in Sydney, one of the best public secondary schools in Australia. From 1899 to 1901, Douglas Mawson studied Mining Engineering at the University of Sydney, graduating on April 19, 1902. Mawson’s best results were in geology under the influence of TW Edgeworth David, the charismatic Professor of Geology at the time. This was the start of a lifelong friendship and professional association, which ended only on David’s death on August 28, 1934 (Corbett 1998, 2000).

In 1902 Mawson commenced a Bachelor of Science degree, majoring in geology. This was interrupted by him spending several months (April to September 1903) studying the geology of the New Hebrides (modern Vanuatu) at the behest of Edgeworth David. Mawson graduated with a Bachelor of Science in early 1905 and commenced an appointment as Lecturer in Mineralogy and Petrology at the University of Adelaide on March 1, 1905. The only other geologist at Adelaide University at the time was 60 year old Walter Howchin.

After arrival in Adelaide, Mawson was very active and in particular studied the geology of the Broken Hill area and the neighbouring Olary area in South Australia. Here Mawson found Precambrian rocks that he considered to have been deposited by glacial action. He wished to see modern glacial activity and in late 1907 contacted Edgeworth David, and through him, Ernest Shackleton, the leader of the 1907-1909 British Antarctic Expedition (BAE). As a result, he was appointed as physicist to the expedition. The BAE was based on Ross Island. Highlights of this expedition for Mawson were participation in the first ascent of Antarctica’s only active volcano, the 3794m high Mt Erebus, and membership of the first party (with Edgeworth David and Alistair Mackay) to reach the vicinity of the South Magnetic Pole. David and Mawson returned to Australia as heroes.

Later in 1909, Mawson found time to continue his Broken Hill studies and completed his doctorate before the end of the year. While working in Broken Hill, Mawson met Paquita Delprat, a daughter of Guillaume Delprat, the General Manager of BHP, whom he later married. Mawson visited London in late 1909 and unsuccessfully tried to persuade Scott to land him at Cape Adare, in order to study the geology of the area. He then organised the Australasian Antarctic Expedition (AAE), the story of which has been well documented by Mawson (1964), Ayres (1999), Hall (2000), Fitzsimons (2011) and particularly by Riffenburgh (2011) who gives the most comprehensive account. The AAE was most notable for Mawson surviving and struggling back to the base at Commonwealth Bay after the deaths of Belgrave Ninnis and Xavier Mertz, his sledging companions on the Far Eastern Party. The boat had already left and Mawson was obliged to stay in Antarctica for another twelve months with six members of his party, led by Cecil Madigan, who had stayed behind. As part of the AAE, bases were also established on Macquarie Island and the Shackleton Ice Shelf. The AAE saw the first use of radio communications with Antarctica.

Mawson was knighted in 1914. He was in the UK from 1916 as part of the war effort, returning to Adelaide in April 1919 where he was appointed Professor of Geology and Mineralogy at the University of Adelaide in 1921, a position he held until his retirement in 1952. For the next few years Mawson was involved in raising funds to pay off the debts of the AAE and in organising the publication of the scientific reports resulting from the expedition. He was an enthusiastic field geologist and did considerable field work in the Broken Hill/Olary and Flinders Ranges areas, usually accompanied by students.

In the summers of 1929-30 and 1930-31, Mawson led the ship-based British, Australian and New Zealand Antarctic Research Expedition (BANZARE) using the Discovery, the ship used by Scott in his first expedition in 1901-04. This was a largely marine science, oceanography and biology expedition, but included landing on Heard Island and a visit to Mawson’s old headquarters at Commonwealth Bay. On the second voyage, Mawson claimed formal possession of King George V Land on behalf of Britain. This is the basis of the present Australian claim to what is termed the Australian Antarctic Territory, which represents about 40% of Antarctica.

Mawson continued his field work in the Flinders Ranges in the 1930s and 1940s. He was a driving force in the establishment of ANARE (Australian National Antarctic Research Expeditions) that still runs the Australian Antarctic research activities. He continued to publish research papers until his death on October 14, 1958.

Memorabilia

The University of Adelaide and the adjacent South Australian Museum have displays where Mawson memorabilia can be viewed.

The Tate Museum in the Mawson Laboratories in the University at the corner of Frome Road and Victoria Drive has a display showcasing Mawson’s Antarctic activities on its southern wall. Some of the rocks collected on the Australasian Antarctic Expedition of 1911-14 are housed in the display cases and there is a substantial further collection in the basement crypt archive (where some sample boxes containing these specimens are as yet unopened). One of the AAE sledges is on the north wall of the Tate Museum.

On North Terrace, at the entrance to the University just west of the Bonython Building, there is a bust of Mawson which was unveiled in 1982 on the occasion of the Fourth International Symposium on Antarctic Earth Sciences, held in Adelaide to commemorate the centenary of Mawson’s birth. At the foot of the bust are two large boulders: one is charnockite from near Mawson Station in Antarctica and the other is pegmatite from Arkaroola in the northern Flinders Ranges.

A recently revamped Australian Polar Exhibit at the South Australian Museum, just to the west along North Terrace, deals with Mawson’s three visits to Antarctica, as well as his work in the Flinders Ranges. There are numerous artifacts from this work as well as some general information on Antarctica. There is also reference to the other two major Australian polar explorers from the pre-World War II era, namely Hubert Wilkins and John Rymill, both of whom were born in South Australia.

Selected references

Ayres, P, 1999. Mawson. A life. (The Miegunyah Press, Carlton South).
Cooper, BJ & Jago, JB, 2007. Mawson’s earliest (1906) report on the geology of the Flinders Ranges. Transactions of the Royal Society of South Australia, 132, 167-174.
Corbett, DWP, 1998. Douglas Mawson: The geologist as explorer. Records of the SouthAustralian Museum, 30,107-136.
Corbett, DWP, 2000. A staunch but testing friendship: Douglas Mawson and T.W.Edgeworth David. Records of the South Australian Museum, 33,49-70.
Fitzsimons, P, 2011. Mawson and the Ice Men of the Heroic Age: Scott, Shackleton andAmundsen. (William Heinemann, North Sydney).
Hall, L, 2000. Douglas Mawson: The life of an explorer. (New Holland, Sydney).
Jacka, FJ, 1986. Mawson, Sir Douglas (1882-1958). Australian Dictionary of Biography. (http://adb.anu.edu.au/biography/mawson-sir-douglas-7531).
Jago, JB & Pharaoh, MD, 2016. Pre-Antarctic Mawson in South Australia and western New South Wales. Transactions of the Royal Society of South Australia, 140, 107-128.
Jago, JB, Pharaoh, MD & Wilson-Roberts, CL, 2005. Douglas Mawson’s first major geological expedition: The New Hebrides, 1903. Earth Sciences History, 24,93-111.
Mawson, D, 1915. The Home of the Blizzard. 2 volumes. (William Heinemann, London).
Mawson, P, 1964. Mawson of the Antarctic. (Longmans, London).
Riffenburgh, B, 2011. Aurora. Douglas Mawson and the Australian Antarctic Expedition1911-14. (The Erskine Press, Norwich).
The Adelie Blizzard: Mawson’s Forgotten Newspaper, 1913, edited by Archie McLean. Reproduced by The Friends of the State Library of South Australia, 2010.

Author: Professor Jim Jago, School of Natural and Built Environments, University of South Australia. jim.jago@unisa.edu.au

Gulf St Vincent & Adelaide beaches

Leave a reply

Over the last million years in southern Australia, sea levels have fluctuated between about 120m below present sea level, during the Ice Ages, to about 2m above during the interglacials. As humans first arrived in Australia more than 50,000 years ago, the sea level fluctuated between 60 and 40m below present, and vast coastal areas were exposed for settlement. Gulf St Vincent has a maximum depth of 40m so, during those times, it had the form of a flat landscape of alluvial plains veneered with calcrete and covered by thin sandy soils and sporadic desert dunes gently sloping towards a central oblong saline swamp (Fig. 1).

Around 30,000 years ago the Earth plunged into a severe Ice Age that lasted until about 15,000 years ago, with sea levels dropping to 120m below present. A warming climate then caused rising sea levels, so that by around 9,700 years ago the sea encroached into the land to form the Gulf (Fig. 2). Continued climate warming and further sea level rise progressively filled the Gulf. The warm shallow seas enabled prolific growth of algae and marine grasses that were nurseries to a rich ecology of fish, shellfish, starfish, sponges, calcareous algae and some corals. Sand-sized foraminifera were abundant, especially in the nearshore and intertidal zones (corresponding to the mangrove-rich areas north of Adelaide).

By around 6,500 years ago the sea had reached its present level and the Gulf achieved its current shape. Abundant shells and shell grit were deposited to form a meter-thick veneer of calcareous sediment covering the now drowned landscape. Predominant south-southwesterly winds created waves that eroded these sediments, for example around Port Norlunga and Maslins Beach, and quartz sand winnowed from them mixed together with more recent shell grit to create the modern beaches (Figs 3, 4). Some quartz sands came from more ancient deposits that are now exposed at Hallett Cove.

Frequent southwesterly storms drove coastal sands northward from Marino Rocks and Glenelg to form a coastal dune series that enclosed the Patawalunga and Westlake depression. This wave-dominant dune system continued to grow northward creating the present Le Fevre Peninsula where around 10m of sand has accumulated (Fig. 5).

European settlement since 1836 has altered the coastal zone by building on or removing most sand dunes, thus allowing storms to attack roads and residences. Placement of rocky rip-rap with the aim of protecting the shoreline has in fact increased wave turbulence and lowered the beach profile by removing additional sand. Replenishment of beach sands to maintain amenity is a continuing Government-funded activity. Tennyson Dunes is one of a few tiny remnants that provide a glimpse of the original Adelaide metropolitan coastline.

References

Bourman RP, Murray-Wallace CV, Harvey N. 2016. Coastal Landscapes of South Australia.Available as a free ebook from www.adelaide.edu.au/press.

Fuller MK, Gostin VA. 2008. Recent coarse biogenic sediments of Gulf St Vincent.InSA Shepherd et al. (eds) Natural History of Gulf St Vincent. Ch.3 , 29-37. (Royal Society of South Australia).

Harvey N, Belperio AP, Bourman RP. 2001. Late Quaternary sea-levels, climate change and South Australian coastal geology. InV Gostin (ed.) Gondwana to Greenhouse: Australian Environmental Geoscience. Geol. Soc. Aust. Spec. Publ. 21, 201-213. (Geological Society of Australia: Sydney).

James NP, Bone Y. 2011. Neritic Carbonate Sediments in a Temperate Realm, (Springer Science+Business Media).

www.tennyson.org.au

Author: Dr VA Gostin

Fossil shells at Stansbury, South Australia, record a higher sealevel 125,000 years ago

Leave a reply

Subsamples were taken of a collection of fossil shells recovered from a depth of around 3 m in trenches excavated in the Oyster Point Caravan Park by local contractors to improve drainage. Several of the fossils (Fig. 1) had been identified by SA Museum personnel and assigned to species including bivalves Katelysia scalarina and Sanguinolaria (Psammotellina) biradiata, and the large gastropod Turbo (Dinassovica) jourdani. All species are still living around the Australian coast, but these shells are clearly ancient and belong to a time when the coastal cliffs at Stansbury stood inland of the caravan park and the township and are now represented by the base of the hill that runs from the cemetery, northwards behind the town centre, and joins the current shore cliffs near the primary school oval. The seas, of which the fossil shells are a legacy, covered all of the lowland eastwards of these ancient cliffs. The cliffs themselves are in fact cut into much older marine deposits, as can be seen behind the jetty and elsewhere along the coast. These relate to the Tertiary period between 3 to 23 million years ago when much of Yorke Peninsula was inundated by sea.

Shell subsamples of two of the species (Katelysia scalarina and Sanguinolaria (Psammotellina) biradiata) were dated in the laboratories of the School of Earth & Environmental Sciences at the University of Wollongong by Professor Colin Murray-Wallace and his colleagues. They used a technique called Amino Acid Racemisation (AAR) and found that the shells are about 125,000 years old. Professor Murray-Wallace can be confident of this dating because he and his colleagues have much experience in determining the ages of ancient Quaternary coastlines of southern Australia and their fossils (see Further reading).

Sea levels 125,000 years ago (Fig. 2) were up to 2m above current sea level, as this time was part of an interglacial period (formally called the ‘Last Interglacial’) when ice in Antarctica and elsewhere had melted somewhat due to warmer global temperatures. This accounts for the encroachment of the seas into the embayment now occupied by much of Stansbury township, and the formation of the old cliff-line. The marine and coastal deposits generated at this time, and which occur widely around South Australian coasts, are referred to the Glanville Formation.

It might be of interest to note that several earth scientists, including Professor Murray-Wallace, have written a book on the coastal landscapes of South Australia. This is currently in press and should be available soon. It includes a chapter on the entire coast of Yorke Peninsula, including Stansbury. As well, a student from the School of Earth & Environmental Sciences at the University of Wollongong (Tsun-You Pan, visiting from Taiwan), and supervised by Professors Murray-Wallace and Bourman, has recently commenced a PhD research project on the Last Interglacial coasts and their deposits on southern Yorke Peninsula and may be able to report in future on his findings on these materials, including the Stansbury Caravan Park fossils.