Geology of the Australian Capital Territory

Last updated
Australia grew around three fused pieces of very ancient continental crust (cratons). Australian rock ages-MJC.png
Australia grew around three fused pieces of very ancient continental crust (cratons).

The geology of the Australian Capital Territory includes rocks dating from the Ordovician around 480 million years ago, whilst most rocks are from the Silurian. During the Ordovician period the region—along with most of eastern Australia—was part of the ocean floor. The area contains the Pittman Formation consisting largely of Quartz-rich sandstone, siltstone and shale; the Adaminaby Beds and the Acton Shale. [1]


Most of the younger rocks are pyroclastic deposits from explosive volcanic eruptions, but the Yarralumla Formation is a sedimentary mudstone/siltstone formation that was formed around 425 million years ago.

In the 1840s fossils of brachiopods and trilobites from the Silurian period were discovered at Woolshed Creek near Duntroon by the Reverend William Branwhite Clarke. [2] At the time these were the oldest fossils discovered in Australia, though this record has since been far surpassed. Other specific geological places of interest include the State Circle cutting and the Deakin anticline. [3] [4]

Limestone outcrop at Acton LimestoneOutcropActonACT.JPG
Limestone outcrop at Acton

The early European name for the district was "Limestone Plains". In 1820, following the discovery of Lake George and the Yass River, Governor Lachlan Macquarie decided to send a party, with provisions for one month, to discover the Murrumbidgee River. Joseph Wild was accompanied by James Vaughan, a constable, and Charles Throsby Smith, a nephew of the explorer Charles Throsby. Detailed instructions had been given to the explorers by Charles Throsby, who had accompanied the Lake George exploration party earlier in the year. They were provided with acid to test for limestone. On 7 December 1820, Smith recorded in his journal:

... Came on to one of the plains we saw at 11 o’clock. At half past 1, came to a very extensive plain, fine Rich Soil and plenty of grass. Came to a Beautiful River plains that was running thro’ the plains in a S.W. direction, by the side of which we slept that night. When we made the Hut this evening, we saw several pieces of stone that had been burnt by all appearances. I then examined some of it, which proved to be limestone. ... [5]

There is, however, little limestone evident at the surface in the district. There is an outcrop at Acton, near the Museum of Australia, by the shores of Lake Burley Griffin. These formations became exposed when the ocean floor was raised by a major volcanic activity in the Devonian forming much of the east coast of Australia.

Much of the western and southern parts of the Australian Capital Territory (ACT) are made from granite-like rocks. These are from the Murrumbidgee Batholith intruding during the late Silurian or early Devonian times.

Tectonic context

Tectonics explains the large-scale structure of the Earth's crust and its constituent rocks in terms of blocks moving along faults, uplifted into horsts or downthrown into grabens. The ACT is positioned on the Australian continent, which was once a part of the supercontinent Gondwana. The ACT is in the Tasmanides, the deformed rocks of the orogen that make up the core of the old mountain range that makes up the Australian continent east of the Tasman Line. These rocks are an addition onto the Proterozoic core of the continent. The Tasmanides are the result of compression, horizontal shortening, and vertical thickening of various "terranes" such as small continental fragments and volcanic island arcs that were plastered against the original continental margin as a result of plate tectonic movements.

The Tasmanides also extended into Antarctica in the south and northern China on the north, as these continental units were attached to Australia at the time, in Gondwana. [6]

The ACT is part of the Eastern Lachlan Fold Belt, which is located on a terrane that is called the Benambra Terrane in Victoria, but the Molong-Monaro Terrane in New South Wales.

Canberra region structure

also known as Canberra-Yass Synclinorial Zone East

also known as Canberra-Yass Synclinorial Zone west

Geological history


A plate with a continent fragment on board bumped into the east coast of what is now Australia, forming the Delamerian Orogeny. The remains of the mountains of this orogeny can be found near Broken Hill and in eastern South Australia, western Victoria, and western Tasmania. This happened between 520 and 480 million years ago up to the Cambrian period. No associated ocean floor has been preserved by obduction in the ACT.

During the Palaeozoic era at least a few thousand kilometres of ocean floor were subducted, taking of the order of a hundred million years. Sediments were deposited in the ocean floor in the form of fans formed by turbidity currents off the side of a continental slope. The flow was in the northerly direction, indicating that the continental slope was to the south. These deposits occurred during the Ordovician period. The ocean floor was distant from the continental source of the sediment. Towards the end of this period there were isolated parts where no turbidity currents reached and only fine clay and animal organic and silica debris were deposited into oxygen-depleted deep water. This ocean basin has been called the Monaro Basin. To the north west was a volcanic chain of islands, the Macquarie arc, with an associated submarine trench.

The subducting Pacific plate was old, cold and dense, easily sinking into the mantle at a steep angle. The hinge zone of the plate also migrated oceanwards over time. So the trench retreated oceanwards, and the old trench and ocean floor become part of the continental plate. Volcanoes formed inwards from the trench. The part of the oceanic plate attached to the continent was compressed, the suboceanic crust was severely shortened and thickened as well, giving rise to a duplex structure. This happened at the end of the Ordovician period and in the Early Silurian. The sediments were heavily folded and overthrusted resulting in severe crustal shortening. In the Canberra area the sediments were raised above sea level and eroded. The land to the west (around Wagga Wagga) was raised higher. An unconformity resulted between the Pittman Formation and the State Circle Shale and Black Mountain Sandstone deposited on top.

Silurian deposition

State Circle Shale and Black Mountain Sandstone deposited in a marine environment as turbidites. The source of the Black Mountain sand was near by from the west, from the Wagga Wagga area. The Canberra area was on the proto-Canberra-Yass Shelf. East of Canberra deep water of the Monaro Basin remained in the Captains Flat area.

A second unconformity occurred after the Black Mountain Sandstone was uplifted and eroded at the end of the early Silurian. This was called the Quidongan Deformation. The Canberra formation was deposited in shallow water with limestone, and shale forming. There were some small volcanic activities at this stage with dacite and ashstone layers included.

Several stages of volcanic activity followed. The first stage with Paddys River Volcanics, Walker Volcanics in west Canberra, Hawkins Volcanics in the north and Ainslie Volcanics in the north east had acidic lava volcanoes erupting. The next stage was Mount Painter Volcanics in middle Canberra, and Colinton Volcanics south of Queanbeyan and near Williamsdale. Then came a pause in volcanism at the start of the Upper Silurian with the Yarralumla Formation and Yass Formation sedimentary deposits. Volcanic activity resumed with Deakin Volcanics in the north west and south of Canberra. First rhyodacite was erupted followed by tuff, more rhyodacite, tuff with some underwater sediments, and finishing with rhyolite. At least four large eruptions made up this volcanic deposit. Over the top of this in the west near the Murrumbidgee River there was a further massive volcanic eruption, called Laidlaw Volcanics.

West of the Murrumbidgee is another different geological setting. The tectonic block is called the Cotter Horst. This was probably in a different position relative to Canberra, compared to the present. From here, ocean floor turbidite deposits occurred in the Ordovician period. The sediments were deeply buried by being compressed and faulted down. Melting occurred in deep sediments and in the basaltic oceanic crust beneath. The magmas mingled and intruded upwards. The Murrumbidgee Batholith was formed, with several intrusions. The faults were reversed and the granites from the batholith became elevated.


Dyke of teschenite TescheniteDyke1.jpg
Dyke of teschenite

Small granite intrusions injected the rocks in the Canberra Graben around 408 million years ago. The Molong-Monaro Terrane was carried into position on the east coast of Australia.

The Bowning Deformation caused the north–south faulting and long folding in the area surrounding the ACT. This deformation was connected with the attachment of the terrane to the continent. During this stage metamorphism occurred. In the Canberra Graben and Cullarin Block, metamorphism mostly reached the upper greenschist stage, with shallow burial and temperature below 350 °C. This changed the volcanics and sediments with sericitisation, saussuritisation, conversion of plagioclase to albite, and conversion of biotite to chlorite, titanite, epidote and opaque minerals. On the western margin in southwest Belconnen, Duffy, and Kambah in the Laidlaw and Walker Volcanics the temperature was lower and prehnite-pumpellyite facies was achieved. This was not sufficient to convert plagioclase to albite.

More intense metamorphism occurred to the east of the Googong Dam, east of the ACT on the Molonglo Range and Yarrow Peak and Taliesin Hills. Psammitic schist and pellitic schist occur there. Within this region, there are two parallel belts of knotted schist even more strongly heated to over 525 °C. The temperature gradient in the area was high at 70 °C per kilometre.

In the east side of the Cullarin Block, in the east-pointing finger of the ACT, the Tabberabberan Orogeny also reached the upper greenschist facies again. East–west pressure caused ruptures forming the Winslade and Deakin Faults and other northwest- or northeast-trending faults.

A dyke of olivine teschenite intruded into the Red Rocks Gorge area of the Murrumbidgee River. The Kosiusko uplift elevated the land in the Snowy Mountains and Southern Highlands areas. This uplift reactivated the Murrumbidgee Fault, the Queanbeyan Fault and the Lake George Fault.


Minor mining operations have occurred historically throughout the region, both for precious metals including gold, silver, lead, and copper, and for construction materials. However the only commercial operations to continue at the present day are the Stockmans Quarry at Pialligo which excavates Camp Hill Sandstone, and a large Quarry on Mount Mugga Mugga which excavates Mugga Mugga Porphyry for use as construction gravel e.g. for road surfaces, and in concrete.

A deposit of galena and copper carbonate was tunneled in the Balconnel Gold Mine around 1894. No significant gold was ever found there. The mine was 200 m downstream from the Molonglo River on the Murrumbidgee River with coordinates 35°S deg 14' 38.3", 148°E deg 58' 13.6". [7]

Paddys River Mine or Cowley copper mine is located 700 m upstream on Paddys River. The host rock is a skarn where Shannons Flat Adamellite baked limestone from the Paddy's River Volcanics. The bulk of the mineral here is magnetite, but other sulfide and minerals of copper, lead zinc and silver attracted miners. Thomas Coyle operated the mine in 1895, producing 2.6 tons of copper and 26.1 kg of silver. In 1907 the Cowley Copper Syndicate Ltd started more work cutting two more adits and winzes. However it was abandoned by 1909 as the ore was too low grade. More than a million tons of magnetite remain. Many minerals such as aurichalcite, bronchanite, caledonite, cerussite, hemimorphite, hydrozincite, linarite, native silver, rozenite, and zincsilite have been found at the location. [8]



Pittman Formation

Chemical Analysis

oxide% or ppm
Rb168 ppm
Sr64 ppm
Pittman Formation

The Pittman Formation was described originally by Öpik in 1958 who named it after the Pittman Valley, southeast of Aranda, Australian Capital Territory. It is entirely of Ordovician age and about 800 metres thick near Canberra, but at Captains Flat it is over 1,200 metres thick. The lower levels are greywacke, exposed east of Queanbeyan and north are very thick and heavily overturned and thrusted. At Etheridge Creek, the type locality is a repeating pattern of sandstone, micaceous sandy shale, mudstone, black argillaceous and radiolarian chert. In the sandstone beds there are occurrences of graded bedding, clay pellets, and current bedding. Fossils of graptolites, radiolarians, conodonts, and occasionally brachiopods and sponges are found. The geological formation east of Queanbeyan used to be known as the Muriarra Formation. This alternates between sandstone with a high quartz content and mica, and phyllite. Radiolarian chert is found in the central section. The railway forms the border between Queanbeyan in NSW and Oaks Estate in the ACT. West of the Queanbeyan railway station is a cutting where folding has overturned the beds, with axes dipping to the east at 50 degrees. 300 metres of thickness is exposed in this cutting. Llanvirnian age (Pygodus serrus conodont zone). Fossils found include Phyllograptus anna, Trigonograptus ensiformus, Pterograptus, Didymograptus, Isograptus, Hallograptus from the Darriwillian age. Near the top of the formation are fossils Dicellograptus sextans, D divaricatus, D salopiensis, which are Gisbornian.

Chemical analysis reveals low concentrations of sodium, calcium and strontium because of the low feldspar content.

The Ordovician turbidites, consisting of greywacke, feldspathic sandstone, micaceous siltstone, micaceous shale, chert, and phyllite, are very similar in all parts of the Tasman Orogen, including New Zealand and the Transantarctic Mountains. Detrital zircons from the turbidites have been isotopically dated with age ranges of 0.46 and 0.60 Gya, 1.0 and 1.2 Gya, and at ~1.8 Gya, ~2.2 Gya and ~2.7 Gya. These do not match the age of zircons from the interior of the Australian Shield, so the source of the sediments is from another continent. The other evidence from the Ordovician sediments are chemical composition indicates granitic source, with the absence of feldspar. Secondly the fine grained nature shows the sediments have been transported a long way from their ultimate, source, and could have been second cycle, derived from sedimentary rocks. [9] [10]

At the time these sediments were deposited the location was at least 3,000 km from the Australian continent. Underneath there is no Proterozoic continental basement, instead these sediments are lying on top of oceanic crust.

Acton Shale

Acton Shale is a grey to black thinly laminated siliceous shale containing graptolites. It is generally leached, and frequently silicified. The colour of the beds alternates between grey and black, but where weathered, it changes to whitish grey. The graptolites appear on the bedding planes as black films. In Canberra, the Acton Shale appears in several outcrops in Acton, in two bands through Aranda, through Bruce near the Calvary Hospital, on the Bruce Ridge behind Lyneham. Also another band starts under the University of Canberra in Belconnen, and heads north east through Lawson and Giralang and folded and faulted into several bands in Crace on Gungahlin Hill. Another band is found on the west side of Queanbeyan, extending north to Dundee, and south around the east side of Jerrabomberra Hill. Acton shale is only preserved in the cores of synclines, being eroded from uplifted parts. Brachiopods, conodonts and sponges fossils are rarely found. The beds are up to 60 metres thick and appear high in the Pittman Formation. The age range is Gisbornian to Bolindian of the Ordovician period. Lower beds contains fossils like Dicranograptus nicholsoni. Upper beds contain Climacograptus bicornbis, Chastatus, C tubuliferis, Dicellograptus elegans, and Dicranograptus hians which are late Eastonian in age.

The sediments making the Acton Shale were deposited in the ocean in a reducing environment starved of oxygen, and lacking fresh sediment.

Late Early Silurian

State Circle Shale

The State Circle Shale was named by Öpik in 1958. It is named after the street where it was described. Its age is Llandoverian. Its lithology is shale, mudstone, siltstone and minor sandstone. In the type location there is about 60 metres of non-calcareous sandy shale and dark grey shale with beds of fine-grained sandstone. Between Kings Avenue and Commonwealth Avenue, there is a good outcrop on State Circle, consisting of buff-coloured laminated siltstone and shale with fine sandstone beds contorted by slumping. Its top is an unconformity, with Camp Hill Sandstone lying on top. There is probably up to 200 metres thickness of this shale. The shale was deposited in the deep sea as turbidites. It can be found in Yarralumla, Parkes, Acton, north and south of Black Mountain, and from Lawson, to Crace and Ngunnawal. [11]

Black Mountain Sandstone

Black Mountain Sandstone is deposited on top of State Circle Shale conformably. It is made up from thick beds of grey quartz sandstone mostly, but has some beds included of siltstone and grey shale. The grain size is fine to medium. It was originally named by Öpik after the mountain—Black Mountain where it is found. Originally it was believed to be Ordovician, but is actually from the Silurian period, late Llandoverian epoch. Some of the slopes of Black mountain are covered in fanglomerate. The deposition was in a marine proximal turbidite fan, with the turbidity current flowing to the east. There are no fossils, but there is some sedimentary structure including plane, cross or convolute laminations, load casts, slump units and flute moulds.

Tidbinbilla Quartzite

Tidbinbilla Quartzite has been modified by granite intrusions close by. It consists of medium grained sandstone, partly silicified and changed to quartzite. Belts of silstone and sandstone are included becoming more frequent at the top. The exposure is 300 metres thick. Low down there is a 2-metre thick bed of ashstone across a broad area that can be used as a marker bed.

Late Middle Silurian

Canberra Formation

In the 1840s fossils of brachiopods and trilobites from the Silurian period were discovered at Woolshed Creek near Duntroon. At the time these were the oldest fossils discovered in Australia, though this record has now been far surpassed. These fossils were from the Canberra Formation. In the past these rocks were known as the Canberra Group with components of Turner Shale, Riverside Formation, and City Hill Shale.

Canberra Formation can be found in the east part of South Canberra in Fyshwick, Kingston, Barton and Parkes. It is also found through North Canberra, excluding Campbell and Russell. It occurs through most of Gungahlin apart from Crace and Nicholls. The beds extend north in a wide band to 35 deg 03S near Bald Hill. [12]

Narrabundah Ashstone is a member of the Canberra formation [12] and is found is eastern Narrabundah and in a geological monument along Fairbairn avenue. Ashstone is a fine grained tuff. [13] In addition to the ashstone the Canberra Formation has layers of green-grey to reddish dacite, also tuff, quartz andesite, but mostly it is calcareous shale, limestone or sandstone. Much is deeply weathered, which has posed difficulties for building foundations.

Walker Volcanics

Walker Volcanics appear as purple or greenish-grey dacitic ignimbrite. These volcanics contain chloritised cordierite and some have garnet. They are Wenlock age. They occur in southern Belconnen including Macquarie, Weetangera, Hawker, Page, Scullin, Higgins, Holt and the Pinnacle. [14]

Hawkins Volcanics

Hawkins Volcanics is a green-grey dacite or dacitic tuff. These volcanics contain chloritised cordierite, and some have garnet. Their age is Ludlow to Wenlock. The volcanics occur in northern Belconnen, in Dunlop, Fraser, Spence, Mount Rogers, Flynn, Melba and Hall. Maximum thickness is 1770 m. [15]

Ainslie Volcanics
Ainslie Volcanics oxide & element chemistry
orderoxide% or ppm

Named after Mount Ainslie, Australian Capital Territory where their type location occurs, the Ainslie Volcanics are composed of Dacitic ignimbrite and minor volcaniclastic and argillaceous sediments. The lithology is bluish grey dacitic tuff, which can be massive or foliated, also dacitic agglomerate and shale. These volcanics contain chloritised cordierite and some have red almandine garnet. Jasper is found on low hills on the north side of the Molonglo River. The thickness is at least 700 metres. The magma was formed by melting an aluminium-rich pelitic sediment. The eruption came from a volcano into shallow sea water. The deposits built above sea level as they progressed. The underlying sediments now make up the Canberra Formation. Between Hall and Namina Hill on Spring Range, the Mount Painter Volcanics lie unconformably on top. These rocks date from the Late Wenlockian epoch of the Silurian period. They were formed about the same time as the Walker Volcanics and Paddys River Volcanics.

The Ainslie Volcanics occur on Mount Ainslie, Mount Majura, and in a band extending from Bonshaw and Harman north to the east of Woolshed Creek, through Majura and at least to Gooroo Hill and Old Joe on the NSW border. On Mount Ainslie the sequence starts with dacitic tuff, banded dacitic tuff, massive dacitic tuff, fifty metres of agglomeratic tuff, massive dacitic tuff, fifty metres of ashstone and topped with massive dacitic tuff. The rocks on top of the eastern ridge is altered.

Mount Painter Volcanics

This was named after Mount Painter in Canberra by Öpik, however he called it a porphyry. [16] The description is a massive dark bluish-grey dacitic crystal tuff containing garnet and chloritised cordierite. There is a local appearance of agglomerate and pumice. There are prominent quartz and feldspar phenocrysts.

Xenoliths include jasperised sediments and there are some beds of tuffaceous siltstone and sandstone. It was mostly deposited from the air without water.

Mount Painter Volcanics overlie the Walker Volcanics unconformably. The top is also an unconformity with Yarralumla Formation and Deakin Volcanics and Yass Formation. The age is of Late Wenlock epoch or early Late Silurian. These rocks form a belt from Coppins Crossing towards Narrabundah and Jerrabomberra Creek. [17]

Yarralumla Formation

In an intervening phase in volcanism predominantly sediments were deposited. Yarralumla Formation was named after the suburb of Yarralumla by Öpik in 1958. It consists mainly of mudstone which may be cemented by lime, or originally derived from tuff. There are some beds inserted of quartz sandstone or limestone. The bottom of the formation is on top of the Mount Painter Volcanics. The top of the formation grades up into pyroclastics from the Deakin Volcanics. [18]

Deposition occurred in a shallow marine environment with a delta. The sea level was relative higher during this depositional phase compared with the earlier and later subaerial volcanic deposit periods. Its age is early Ludlow. This has been determined by shelly marine fossils, and a tonalite intrusion southwest of Red Hill with age determined as 417±8 Mya. Outcrops occur on Red Hill (the hill) and throughout Deakin, Australian Capital Territory and in southern Yarralumla, and also Hughes, Australian Capital Territory. The formation extends from Red Hill and Woden in the South to Yarralumla and Lake Burley Griffin in the north. The formation is evidence of the last major period when eastern Australia was still covered by shallow seas. It shows fossil evidence of trilobites, coral and primitive crinoids.

Another band stretches from Lyons, Australian Capital Territory north north west towards the Molonglo River. There may also be a patch in Symonston, Australian Capital Territory. Exposures can be seen at the Deakin Anticline [19] —with pale brown siltstone; and also at the Yarralumla brickworks [20] with olive-green calcareous mudstone.

Yass Subgroup

Dated early Ludlow to Wenlock. This may outcrop in Belconnen and Florey. The composition is calcareous and tuffaceous shale, sandstone, ashstone and limestone. These volcanics lack cordierite or garnet. [21]

Deakin Volcanics
Deakin Volcanics chemistry
orderoxide% or ppm
12Ba540 ppm
14Rb210 ppm
15Zr125 ppm
16Sr100 ppm
Banded Tuff from the Deakin Volcanics DVbandedTuff.jpg
Banded Tuff from the Deakin Volcanics
Deakin Volcanics rhyodacite modified to green colour Deakin Volcanics Green rhyodacite.jpg
Deakin Volcanics rhyodacite modified to green colour
Deakin Volcanics red tuff Deakin Volcanics red tuff.jpg
Deakin Volcanics red tuff

The Deakin Volcanics can be seen in the road cutting along the Tuggeranong Parkway between Hindmarsh Drive and Cotter Road. The visible base shows a weathered repeating sequence of interbedded rhyodacitic ignimbrite, sandstone, siltstone and red and yellow shale. Southwards the section passes up into a massive and partly banded rhyodacitic ignimbrite. The bottom of the Deakin Volcanics is exposed on nearby Heysen Street. At least 400m thickness of beds are exposed in the Parkway cutting. The Tuggeranong area has the thickest deposits. Rock types in the Deakin Volcanics are rhyodacitic ignimbrite, lava (Mugga Mugga Porphyry Member), tuff, tuffaceous shale and minor quartz sandstones and volcanic breccia-units show reddish brown alteration. The unit is of Early Ludlovian age. The rock on Mount Rob Roy and Pemberton Hill used to be known as Tuggeranong Granite, but is actually ignimbrite. The ignimbrite forms escarpments, with the lower-lying land being underlain by tuff. The Deakin Volcanics can be found south of the Deakin Fault between Belconnen and Charnwood and MacGregor. It also is found through Weston Creek north of Chapman and Fisher, through Woden apart from Curtin, and across to Hume, and south through Tuggeranong. The different colours found in the rocks are due to weathering, the red being from hematite, and the green from clay minerals such as celadonite. The pink crystals are potash feldspar.

The Mugga Mugga Porphyry is a lava flow. It is blue or mauve grey in a mass. The rock is veined with calcite, light green epidote, and deep red hematite. The phenocrysts are quartz, grey plagioclase, pink potash feldspar in lesser amounts and flakes of biotite. It is dated at 414±9 Mya. The Federal Golf Course Tonalite introduces some veins and saccharoidal galena.

Laidlaw Volcanics
Ignimbrite from the Red Rocks Gorge has a strong red colour RedRockIgnimbrite.png
Ignimbrite from the Red Rocks Gorge has a strong red colour

The Laidlaw volcanics are a rhydacitic ignimbrite in the form of pale to dark grey rhyodacitic to dacitic crystal tuff. They are the top layer of Volcanics in the ACT. The Laidlaw Volcanics occur in a band along the Murrumbidgee River to the south west of Canberra, and also north west of Belconnen. They exist in the suburbs of Latham, Chapman, Kambah, and Greenway. The volcanics are of Ludlovian age 420.7±2.2 m.y. and have been used to set an absolute date for the Ludlow epoch. They are up to 850 metres thick. [22]

Some shale and water deposited tuff occur to the west of Pine Island and Point Hut Crossing. North west of Mount Stromlo, on Uriarra Road, there is an occurrence of limestone over a few square kilometres.


Porphyrytic intrusions occur throughout the area.

Middle Silurian intrusions could be volcanic necks. A coarse green grey rhyodacitic intrusive outcrops over one square kilometre west of Holt in the Walker Volcanic sediments. It is likely to be the magma chamber for the uppermost eruption of Walker Volcanics.

A coarse green grey rhyodacitic intrusive with white prominent feldspar crystals appears between the arms of Lake Ginninderra, McKellar, Evatt, Nine Elms, east Spence, and Nichols. This covers a few square kilometres. A small outcrop of the same material occurs in Cook and Jamison Center. This rock matches the upper layer of the Hawkins Volcanics.

East and north east of Watson is an intrusion of grey and cream dacite. This may correspond to the lower layer of the Ainslie Volcanics.

Late Silurian to early Devonian intrusions could also be volcanic necks. If so they have been responsible for the Laidlaw Volcanics. They are all unnamed. The first three intrude Laidlaw Volcanics.

A coarse rhyodacitic intrusive outcrops to the north west of Charnwood intrudes Laidlaw Volcanics, with about half a square kilometre of surface area.

A line of outcrops of coarse pink-brown rhyodacitic porphyry outcrops on the north side of Canberra on Forster Hill, MCquoids Hill and Neighbour Hill, and on East side of Mount Taylor.

A distorted band of coarse grey rhyodacitic porphyry occurs along the Murrumbidgee River from 1 to 4 kilometres south of Point Hut Crossing.

Another pink and green rhyolite porphyry occurs in Holder, Weston and Lyons. It intrudes Deakin Volcanics.

Glebe Farm Adamellite

A coarse porphyritic micro-adamellite was intruded sometime from late Silurian to early Devonian. It intrudes the Hawkins Volcanics in Belconnen in Flynn, Melba, McKellar, the Town Center and Bruce.

Sutton Granite

Also known as the Greenwood Granite, the Sutton Granite is a medium grained granite intruding the Pittman formation in the hills to the north east of Canberra Airport. The outcrop covers 4 square kilometres in the ACT. It was intruded during the late Silurian and is dated at 410+4Mya. The colour is pale grey with mineral white feldspar, milky grey quartz, black biotite, and with hornblende rich xenoliths. Minor minerals are apatite and zircon. The surrounding Pittman formation rocks have been metamorphosed in a contact aureole to hornfels and spotted schist. A magnetic high matches the location indicating the presence of magnetite.

Adaminaby Beds
Adaminaby Beds outcrop south of the ACT Adaminaby Beds.jpg
Adaminaby Beds outcrop south of the ACT

The Adaminaby Beds were formed from quartz turbidite capped with black shale. It consists mainly of fine to medium grained quartz rich sandstone and some mostly thin beds of siltstone, shale and slate. The sediments occur in a band on the west side of the ACT on Bulls Head, Mount Franklin, Mount Ginini and along the upper parts of the Cotter River. A separate outcrop extends into the ACT from the south in the area of the Gudgenby River. Yet another outcrop is on the Bullen Range.

Paddys River Volcanics

The Paddys River Volcanics consist of dacite and tuff with some shale phyllite and limestone. They occur to the west of the Bullen range, along the lower parts of the Paddys River. They were deposited on top of the Ordovician Adaminaby Beds, and intruded by Shannons Flat Adamellite.

Uriarra Volcanics

The Uriarra Volcanics consists of dacite lava flows and pyroclastic deposits of tuff. A fine ashstone bed called the Tarpaulin Creek Ashstone Member outcrops in an approximate north–south line and acts as a marker within the volcanics. Tuff and flows above and below the ashstone member contain obvious pink feldspar crystals. The tuff shows bedding, and the flows have banded flow structure. The Cotter Porphyry to the north of the Cotter Dam is actually a dacite flow. There is a limestone lens north of Uriarra Crossing. The outcrop goes from Mountain Creek Road in the west to the Murrumbidgee river in the east. It extends a few kilometres to the north of the ACT border and south to the Winslade Fault near the Cotter River. A wedge extends to the south south west, which includes Pierces Creek.

Late Silurian to Middle Devonian

Murrumbidgee Batholith

The Murrumbidgee Batholith formed by melting different sediments to the Ordovician Pittman Formations, as the granites contain more feldspar elements Ca, Na and K. At Cooma there is migmatite where the sediments have been partially melted in order to produce the plutonic rocks in the batholith. Variations in their composition are explained by partial mixing with melted oceanic crust. The batholith was largely crystallised before emplacement, and made space for intrusion by displacement rather than dissolution.

Clear Range Granodiorite
Clear Range Granodiorite

Mineral Composition

Microcline K-feldspar8.9%

Clear Range Granodiorite covers 475 square kilometres from Tharwa to Thredbo on the west side of the Murrumbidgee batholith on Clear Range. Clear Range ridge forms the ACT border in the south east. Described as foliated with numerous inclusions. The inclusions are metamorphosed sediments and are common in biotite. It contains quartz and microcline feldspar and brown biotite and also muscovite. It has more biotite and plagioclase than Shannons Flat Granodiorite. The muscovite is distinctly foliated and there is also blue quartz. Texture is fine to medium grained. Close to the Murrumbidgee Fault the texture is mylonitic and the rock is easily weathered.

Shannons Flat Granodiorite

Shannons Flat Granodiorite is poor in xenoliths and is coarse grained. It was intruded after the clear Range Granodiorite.

Shannons Flat Granodiorite from the Tidbinbilla Tracking Station ShannonsFlatAdamellite.png
Shannons Flat Granodiorite from the Tidbinbilla Tracking Station
Shannons Flat Granodiorite

Mineral Composition

Microcline K-feldspar21.0%
Tharwa Adamellite

Mineral Composition

Microcline K-feldspar29.7%
Tharwa Adamellite

The Tharwa Adamellite resembles Shannons Flat Adamellite, but with more strongly zoned plagioclase (An50-20) contains microcline, it is poor in xenoliths and is coarse grained.

Booroomba Leucogranite

Booroomba Leucogranite is found at Mount Tennant and Booroomba Rocks. The total outcrop is 52 square kilometres. It is coarsely crystalline and pale in comparison to other granites.[ citation needed ] Muscovite occurs in unweathered rock. This leucogranite intrudes Clear Range Granodiorite and Shannons Flat Granodiorite.

It is low in iron and calcium, and higher in potassium than other Murrumbidgee Batholith intrusions.

Olivine Teschenite from Red Rocks Gorge
Black teschenite from the Red Rocks Gorge Teschenite3.png
Black teschenite from the Red Rocks Gorge

A dyke of teschenite occurs in the Red Rocks Gorge near Allens Creek. It is oriented northwest–southeast and heads towards Kambah Pool Area. A similar dyke also outcrops on the west side of the Murrumbidgee River near Pine Island. The dyke is less than 0.5 metres thick. The rock is black, showing up well against the reds and browns of the Laidlaw Volcanics.

The rock consists of microphenocrysts of olivine altered to serpentine, pinkish brown titanaugite, brown kaersutite amphibole, and about 15% magnetite, embedded in a colourless analcime groundmass. Kaersutite contains titanium and has a formula near NaCa2(Mg4Ti)[Si6Al2O22]O(OH).

The dyke is believed to be Tertiary in age.


Layers found from seismic waves

In the ACT the Moho depth is about 46–47 km below sea level. South south east of Canberra to the Tasman Sea is a region of lower Moho depth than the surrounding south-east Australia. [23] Seismic P-waves travel at 8.1 km/s in the mantle below this boundary. Above the Moho is an underplated layer with P-wave speeds of 6.7 to 7.0 km/s between 22 and 47 km. Above this layer is rock with speeds of 6.4 to 6.6 km/s from 22 to 15 km deep probably made from basic igneous rocks that were once oceanic crust. Above 15 km depth the P-wave speed is from 6 to 6.2 km/s and likely to be Ordovician turbidites as seen at the surface. [23]

Magnetic field

Magnetic deviation through the centre of Canberra was measured at 12.00 degrees east in 1985. The contours run North east. Each year it shifts 2.2 minutes to the east. Magnetic field in all three components is measured continuously at a station in Canberra and made available online.

Magnetic Field Components at Civic at the [24] end of 2013:

 Magnetic declination D = 12.273°  field strength F = 58096 nT Magnetic inclination I = -65.856°  dD = -0.008 deg/yr dF = -28 nT/yr dI = 0.014 deg/yr

Gravity field

The gravity anomaly over the ACT has been measured and published on the 1:100000 Canberra Geological Map. High level points in the gravity field occur at the head of Yass River just north of the east finger of the ACT of –320  μm·s−2. 1 μm·s−2 is 0.1  milligals, so this level is –32 milligals. Another high of –330 μm·s−2 is just north of the northernmost point of the ACT. The contours in the ACT run NW–SE. At the Canberra GPO is about −440, at Scriviner Dam −510, at Lake Tuggeranong Dam −600, and Banks −590. The western end of Kambah has the lowest level in Canberra at −610. Oaks Estate is −400, the highest levels in the metropolitan area are at Watson and Mitchell at −350, and at Mulligans Flat at −345. This means that a 50 kg person, if measured on a force scale rather than on a balance, would apparently weigh 1.3 grams more in Watson, than they would in western Kambah. [25]

A sensitive gravity measuring station is positioned on Mount Stromlo. This can measure changes in the gravity field over time.

The gravity lows are due to the Murrumbidgee Batholith which is compose of lighter rocks. [23]

Heat flow

Temperature gradients in the Canberra area vary from 20 to 30 °C/km. At Blundell's Cottage heat flow is 73 mWm−2 with a gradient of 27 °C/km. [23]


The ACT is moving 24 degrees east of north with a velocity of 54.5 mm/yr along with the rest of the Australian plate. It is sinking at a rate of 3.5 mm per year. [26]


Most soils in the ACT are Podzols. They have a duplex structure with red or brown clayey layer. Typical thicknesses are 2 metres.

Related Research Articles

The Llano Uplift is a geologically ancient, low geologic dome that is about 90 miles (140 km) in diameter and located mostly in Llano, Mason, San Saba, Gillespie, and Blanco counties, Texas. It consists of an island-like exposure of Precambrian igneous and metamorphic rocks surrounded by outcrops of Paleozoic and Cretaceous sedimentary strata. At their widest, the exposed Precambrian rocks extend about 65 miles (105 km) westward from the valley of the Colorado River and beneath a broad, gentle topographic basin drained by the Llano River. The subdued topographic basin is underlain by Precambrian rocks and bordered by a discontinuous rim of flat-topped hills. These hills are the dissected edge of the Edwards Plateau, which consist of overlying Cretaceous sedimentary strata. Within this basin and along its margin are down-faulted blocks and erosional remnants of Paleozoic strata which form prominent hills.

<span class="mw-page-title-main">Deakin, Australian Capital Territory</span> Suburb of Canberra, Australian Capital Territory

Deakin is a suburb of Canberra, Australian Capital Territory, Australia. Development began in the 1920s, although the vast majority of the suburb was built after 1945. It is a largely residential suburb. It includes the official residence of the Prime Minister, The Lodge, and the Royal Australian Mint.

Symonston is a primarily industrial and agricultural suburb of Canberra, Australian Capital Territory, Australia. Symonston is named after Sir Josiah Symon a Legislator, Federalist and one of the Founders of the Constitution of Australia.

Melba is a residential suburb in the Belconnen district of Canberra, located within the Australian Capital Territory, Australia. The suburb of Melba is named after Dame Nellie Melba (1861–1931), the first internationally recognised Australian opera soprano. The streets are named after composers, singers and other musically notable Australians or people with strong Australian connections.

<span class="mw-page-title-main">Belconnen, Australian Capital Territory</span> Suburb of Canberra, Australian Capital Territory

Belconnen is the most inner suburb of the larger district of Belconnen in Canberra, Australia. Sharing its name with the larger district which encapsulates it, the suburb is surrounded with well developed infrastructure, and planning which allows it sunset views from the Brindabellas on its western side. The suburb contains important amenities for the District of Belconnen including the Belconnen Town Centre and Lake Ginninderra as well as its own well populated residential areas. It is bounded by Ginninderra Drive, Aikman Drive, Eastern Valley Way, Belconnen Way and Coulter Drive. It has a number of parks such as Margaret Timpson Park, Eastern Valley Oval, and on the foreshores of Lake Ginninberra, Diddams Close Park and John Knight Memorial Park.

<span class="mw-page-title-main">Lawson, Australian Capital Territory</span> Suburb of Canberra, Australian Capital Territory

Lawson is a suburb in the Belconnen district of Canberra, located within the Australian Capital Territory, Australia. The suburb is surrounded by Baldwin Drive, Gundaroo Drive and Ginninderra Drive. It lies next to the suburbs of McKellar, Giralang, Kaleen, Bruce and Belconnen.

<span class="mw-page-title-main">Curtin, Australian Capital Territory</span> Suburb of Canberra, Australian Capital Territory

Curtin is a suburb in Canberra, Australia, part of the Woden Valley district; its postcode is 2605.

<span class="mw-page-title-main">Hughes, Australian Capital Territory</span> Suburb of Canberra, Australian Capital Territory

Hughes is a suburb in the Canberra, Australia district of Woden. The postcode is 2605. The area of the suburb is 1.81 km2.

<span class="mw-page-title-main">Lyons, Australian Capital Territory</span> Suburb of Canberra, Australian Capital Territory

Lyons is a suburb in the Canberra, Australia district of Woden. The postcode is 2606.

<span class="mw-page-title-main">Kambah, Australian Capital Territory</span> Suburb of Canberra, Australian Capital Territory

Kambah is the northernmost suburb in the district of Tuggeranong, Canberra. It is located just south of Mount Taylor in the Canberra Nature Park. It is located north of the suburbs of Greenway and Wanniassa. It is bounded by Sulwood Drive to the north and Athllon Drive to the south-east.

<span class="mw-page-title-main">Williamsdale, Australian Capital Territory</span> Town in Australian Capital Territory

Williamsdale is the name sometimes given to the unbounded locality situated immediately on the north-west side of the Australian Capital Territory border abutting the locality of Williamsdale in the Southern Tablelands region of New South Wales, Australia. The Monaro Highway and the former Bombala railway pass through the area. A railway station saw service until 1975. The postcode is 2620. The Australian Capital Territory portion is located in the District of Tuggeranong.

<span class="mw-page-title-main">Geology of Jersey</span>

The geology of Jersey is characterised by the Late Proterozoic Brioverian volcanics, the Cadomian Orogeny, and only small signs of later deposits from the Cambrian and Quaternary periods. The kind of rocks go from conglomerate to shale, volcanic, intrusive and plutonic igneous rocks of many compositions, and metamorphic rocks as well, thus including most major types.

<span class="mw-page-title-main">Geology of Tasmania</span> Overview of the geology of Tasmania

The geology of Tasmania is complex, with the world's biggest exposure of diabase, or dolerite. The rock record contains representatives of each period of the Neoproterozoic, Paleozoic, Mesozoic and Cenozoic eras. It is one of the few southern hemisphere areas that were glaciated during the Pleistocene with glacial landforms in the higher parts. The west coast region hosts significant mineralisation and numerous active and historic mines.

Williamsdale is a locality situated immediately on the south-east side of the New South Wales border abutting the locality of Williamsdale in south-eastern Australian Capital Territory, Australia. The Monaro Highway and the former Bombala railway pass through the village. A railway station saw service from 1891 until 1975. The postcode is 2620.

<span class="mw-page-title-main">Hebridean Terrane</span> Part of the Caledonian orogenic belt in northwest Scotland

The Hebridean Terrane is one of the terranes that form part of the Caledonian orogenic belt in northwest Scotland. Its boundary with the neighbouring Northern Highland Terrane is formed by the Moine Thrust Belt. The basement is formed by Archaean and Paleoproterozoic gneisses of the Lewisian complex, unconformably overlain by the Neoproterozoic Torridonian sediments, which in turn are unconformably overlain by a sequence of Cambro–Ordovician sediments. It formed part of the Laurentian foreland during the Caledonian continental collision.

<span class="mw-page-title-main">Geology of the Lake District</span>

The geology of England's Lake District is dominated by sedimentary and volcanic rocks of mainly Ordovician age underpinned by large granitic intrusions. Younger sedimentary sequences outcrop on the edges of the Lake District area, with Silurian to the south, Carboniferous to the north, east and west and Permo-Triassic to the west and east. The entire area was covered by a Mesozoic sequence that was eroded off during Paleogene uplift related to the opening of the North Atlantic. During the Quaternary the area was affected by repeated glaciations, which sculpted the current mountainous landscape.

The geology of Ohio formed beginning more than one billion years ago in the Proterozoic eon of the Precambrian. The igneous and metamorphic crystalline basement rock is poorly understood except through deep boreholes and does not outcrop at the surface. The basement rock is divided between the Grenville Province and Superior Province. When the Grenville Province crust collided with Proto-North America, it launched the Grenville orogeny, a major mountain building event. The Grenville mountains eroded, filling in rift basins and Ohio was flooded and periodically exposed as dry land throughout the Paleozoic. In addition to marine carbonates such as limestone and dolomite, large deposits of shale and sandstone formed as subsequent mountain building events such as the Taconic orogeny and Acadian orogeny led to additional sediment deposition. Ohio transitioned to dryland conditions in the Pennsylvanian, forming large coal swamps and the region has been dryland ever since. Until the Pleistocene glaciations erased these features, the landscape was cut with deep stream valleys, which scoured away hundreds of meters of rock leaving little trace of geologic history in the Mesozoic and Cenozoic.

The geology of Utah includes rocks formed at the edge of the proto-North American continent during the Precambrian. A shallow marine sedimentary environment covered the region for much of the Paleozoic and Mesozoic, followed by dryland conditions, volcanism and the formation of the basin and range terrain in the Cenozoic. Utah is a state in the western United States.

Geology of Uzbekistan

The geology of Uzbekistan consists of two microcontinents and the remnants of oceanic crust, which fused together into a tectonically complex but resource rich land mass during the Paleozoic, before becoming draped in thick, primarily marine sedimentary units.

The geology of Yukon includes sections of ancient Precambrian Proterozoic rock from the western edge of the proto-North American continent Laurentia, with several different island arc terranes added through the Paleozoic, Mesozoic and Cenozoic, driving volcanism, pluton formation and sedimentation.


  1. "Geoscience Australia". Australian Government. Retrieved 2007-10-11.{{cite journal}}: Cite journal requires |journal= (help)
  2. ACT Heritage Council: Woolshed Creek Fossil Site Archived 2008-07-25 at the Wayback Machine 2004
  3. "State Circle Cutting, State Ccl, Parkes, ACT, Australia (Place ID 13321)". Australian Heritage Database . Australian Government . Retrieved 2007-10-11.
  4. "Deakin Anticlines, Macgregor St, Deakin, ACT, Australia (Place ID 13312)". Australian Heritage Database . Australian Government . Retrieved 2007-10-11.
  5. "1301.0 - Year Book Australia, 1931 — Special Article - Canberra Past and Present". Australian Bureau of Statistics. January 1931. Retrieved 2007-10-11.{{cite journal}}: Cite journal requires |journal= (help)
  6. Plate tectonic processes in the southwest Pacific: a spatial and temporal context Barry Drummond, B. L. N. Kennett, R. J. Korsch, B. R. Goleby & P. A. Symonds Penrose Conference March 1999
  7. Mark (2006). "The Balconnel Gold Mine". Archived from the original on 28 December 2013. Retrieved 28 December 2013.
  8. McQueen, Ken G.; J. R. Caldwell; P. W. Millsteed (July 1988). "Primary and Secondary Minerals at the Paddy's River Mine, Australian Capital Territory". Australian Mineralogist. 3: 83–100.
  9. Crustal Evolution in Southeastern Australia: A Zircon Viewpoint Ian S. Williams and Bruce W. Chappell
  10. Basement of the Lachlan Fold Belt: the Evidence From S-Type Granites B. W. Chappell, GEMOC ANU
  11. "Place ID 105733". Australian Heritage Database . Australian Government.
  12. 1 2 "Definition card for: Canberra Formation". Geoscience Australia. 1990. Retrieved 28 December 2013.
  13. "Definition card for: Narrabundah Ashstone Member". Geoscience Australia. Retrieved 28 December 2013.
  14. "Stratigraphic Search Walker Volcanics". Geoscience Australia. Retrieved 28 December 2013.
  15. "Stratigraphic Search Hawkins Volcanics". Geoscience Australia. Retrieved 28 December 2013.
  16. A. A. Öpik, "The Geology of the Canberra City District", chapter in Canberra, a nation's Capital, ed H. L. White 1954 Angus and Robertson, p. 143
  17. "Definition card for: Mount Painter Volcanics". Geoscience Australia. Retrieved 28 December 2013.
  18. Geoscience Australia database record
  19. Heritage Register Archived 2008-07-25 at the Wayback Machine
  20. "Yarralumla Brickpits, Yarralumla, ACT Profile". Archived from the original on 14 August 2008. Retrieved 6 January 2019.
  21. "Australian Stratigraphic Units Database, Geoscience Australia".
  22. The Laidlaw Volcanics: a Late Silurian point on the geological time scale by D. Wyborn and M. Owen, W. Compston and I. McDougall in Earth and Planetary Science Letters Volume 59, Issue 1, June 1982, pp. 90–100
  23. 1 2 3 4 Finlayson, D. M. (2008). A Geological Guide to the Canberra Region and Namadgi National Park. Geological Society of Australia (ACT Division). pp. 91–92. ISBN   9780646487342.
  24. "Australian Geomagnetic Reference Field Computation". Geoscience Australia. Retrieved 28 December 2013.
  25. 1:100000 Canberra Geological Map
  26. P. Tregoning:Is the Australian Plate deforming? A space geodetic perspective Geological Society of Australia Special Bulletin 22, 2003, p. 46