Geology of New South Wales

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Geologically the Australian state of New South Wales consists of seven main regions: Lachlan Fold Belt, the Hunter-Bowen Orogeny or New England Orogen (NEO), the Delamerian Orogeny, the Clarence Moreton Basin, the Great Artesian Basin, the Sydney Basin, and the Murray Basin. [1]

The Lachlan Fold Belt (LFB) or Lachlan Orogen is a geological subdivision of the east part of Australia. It is a zone of folded and faulted rocks of similar age. It dominates New South Wales and Victoria, also extending into Tasmania, the Australian Capital Territory and Queensland. It was formed in the Middle Paleozoic from 450 to 340 Mya. It was earlier known as Lachlan Geosyncline. It covers an area of 200,000 km2.

Clarence Moreton Basin

The Clarence Moreton Basin is a Mesozoic sedimentary basin on the easternmost part of the Australian continent. It is located in the far north east of the state of New South Wales around Lismore and Grafton and in the south east corner of Queensland. It is the part of the Great Artesian Basin that extends to the east coast in Australia's central eastern lowlands.

Great Artesian Basin

The Great Artesian Basin (GAB), located in Australia, is the largest and deepest artesian basin in the world, stretching over 1,700,000 square kilometres (660,000 sq mi), with measured water temperatures ranging from 30–100 °C (86–212 °F). The basin provides the only source of fresh water through much of inland Australia.


There are a few other sedimentary basins, the Great Artesian Basin can be broken into the Eromanga Basin in the west and the Surat Basin to the east. The Sydney Basin extends north into the Gunnedah Basin, which goes even further north into the Bowen Basin which extends into Queensland, under the Surat Basin. The New England Orogen has a few small Basins included, such as the Lorne Basin, the Myall Syncline, and Gloucester Basin. The Oaklands Basin is in the south of the state under the Murray Basin. The Darling Basin is in the state's west, but mostly covered by the Murray Basin. Gilgandra Sub-Basin and Paka Tank Trough are potential places for coal and gas. [2]

Eromanga Basin natural gas field

The Eromanga Basin is a large Mesozoic sedimentary basin in central and northern Australia. It covers parts of Queensland, the Northern Territory, South Australia, and New South Wales, and is a major component of the Great Artesian Basin. The Eromanga Basin covers 1,000,000 km² and overlaps part of the Cooper Basin.

The Surat Basin is a geological basin in eastern Australia. It is part of the Great Artesian Basin drainage basin of Australia. The Surat Basin extends across an area of 270,000 square kilometres and the southern third of the basin occupies a large part of northern New South Wales, the remainder is in Queensland. It comprises Jurassic through to Cretaceous aged sediments derived from Triassic and Permian arc rocks of the Hunter-Bowen orogeny. Towns situated above the basin, once dominated by agriculture, are experiencing a boom as mines and infrastructure in the area are expanded.

Gunnedah Town in New South Wales, Australia

Gunnedah is a town in north-eastern New South Wales, Australia and is the seat of the Gunnedah Shire local government area. In the 2016 census the town recorded a population of 9,726. Gunnedah is situated within the Liverpool Plains, a fertile agricultural region, with 80% of the surrounding shire area devoted to farming. The Namoi River flows west then north-west through the town providing water beneficial to agricultural operations in the area.

New South Wales is home to some important mining operations including Broken Hill and coal mining and burning in the Hunter and Illawarra. [3]

Broken Hill Town in New South Wales, Australia

Broken Hill is an inland mining city in the far west of outback New South Wales, Australia. It is near the border with South Australia on the crossing of the Barrier Highway (A32) and the Silver City Highway (B79), in the Barrier Range. It is 315 m (1,033 ft) above sea level, with a hot desert climate, and an average rainfall of 235 mm (9 in). The closest major city is Adelaide, the capital of South Australia, which is more than 500 km (311 mi) to the southwest and linked via route A32.

Delamerian orogeny

Lachlan Fold Belt

Rocks from the Lachlan Fold Belt are exposed through the south east and central parts of NSW, and underlie the Great Artesian Basin and the Sydney and Murray Basins at depth. The region is currently 1000 km wide, but was originally 2000 to 3000 km. The Lachlan Fold Belt was formed in the Middle Paleozoic from 450 to 340 Mya. It lies on a basement of Cambrian oceanic floor, however, most of this has been subducted leaving the sediment veneer scraped off in chevron folds. It was compressed as the Pacific plate subducted beneath the Australian continent margin. Over time the hinge point, at which the ocean bed was bent down, changed to be more out to the east, and additional ocean bed sediment was added to the continent. This also means that there is a failed subduction zone extending through New South Wales.

The Cambrian Period was the first geological period of the Paleozoic Era, and of the Phanerozoic Eon. The Cambrian lasted 55.6 million years from the end of the preceding Ediacaran Period 541 million years ago (mya) to the beginning of the Ordovician Period 485.4 mya. Its subdivisions, and its base, are somewhat in flux. The period was established by Adam Sedgwick, who named it after Cambria, the Latin name of Wales, where Britain's Cambrian rocks are best exposed. The Cambrian is unique in its unusually high proportion of lagerstätte sedimentary deposits, sites of exceptional preservation where "soft" parts of organisms are preserved as well as their more resistant shells. As a result, our understanding of the Cambrian biology surpasses that of some later periods.

The Australian Capital Territory is embedded in New South Wales in the Lachlan Fold Belt. The Narooma Terrane is another terrane abutted on the southeast corner of New South Wales which can be considered as a component of the Lachlan Fold Belt.

Geology of the Australian Capital Territory

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.

The Narooma Accretionary Complex or Narooma Terrane is a geological structural region on the south coast of New South Wales, Australia that is the remains of a subduction zone or an oceanic terrane. It can be found on the surface around Narooma, Batemans Bay and down south into Victoria near Mallacoota. It has attached itself to the Lachlan Fold Belt and has been considered as either an exotic terrane or as a part of the fold belt. Rocks are turbidites, block in matrix mélange, chert, and volcanics. The accretionary complex itself could either be the toe of a subduction zone, or an accretionary prism. It was moved by the Pacific Plate westwards for about 2500 km until it encountered the east coast of Gondwana. It is part of the Mallacoota Zone according to Willman, which in turn is part of the Eastern Lachlan Fold Belt, which is part of the Benambra Terrane.

Hunter-Bowen orogeny

The Hunter-Bowen orogeny also known as the New England Orogen contains rocks from Late Paleozoic to early Mesozoic times. It was formed as an arc-forearc zone as the Pacific Plate was subducted to the west. [4]

The PaleozoicEra is the earliest of three geologic eras of the Phanerozoic Eon. It is the longest of the Phanerozoic eras, lasting from 541 to 251.902 million years ago, and is subdivided into six geologic periods : the Cambrian, Ordovician, Silurian, Devonian, Carboniferous, and Permian. The Paleozoic comes after the Neoproterozoic Era of the Proterozoic Eon and is followed by the Mesozoic Era.

The Mesozoic Era is an interval of geological time from about 252 to 66 million years ago. It is also called the Age of Reptiles and the Age of Conifers.

Pacific Plate An oceanic tectonic plate under the Pacific Ocean

The Pacific Plate is an oceanic tectonic plate that lies beneath the Pacific Ocean. At 103 million square kilometres (40,000,000 sq mi), it is the largest tectonic plate.

Darling and Barka Basins

The Darling basin formed in the very early Devonian. Stretching the crust led to the formation of basins such as the Cobar Basin, Mount Hope Trough, Melrose Trough and Rast Trough. Where stretching was less, shelves were formed instead: Kopyje Shelf, Mouramba Shelf, Walters Range Shelf and Winduck Shelf. The Cobar Supergroup is the term used for the infill in these shelves and troughs which consisted of sediment and volcanics.

The deeper basins included turbidites. Felsic volcanic material was also erupted in the Rast and Mount Hope Troughs. The Florida, Babinda, Majuba and Mineral Hill Volcanics are found on the East side of the Kopyje Shelf. Most of the sediment however is quartz sand.

Subsequently in the early Devonian the basin content was pushed back up, and the Mulga Downs Group was deposited by rivers up until the Carboniferous Period. This formed the Barka Basin. Rock from this group is mostly quartz sandstone, with a small amount of siltstone. [5]

Sydney Basin

The Sydney Basin consists of Permian and Triassic sedimentary rocks stretching from Newcastle to Batemans Bay. [6] The land component covers 44000 km2, but there is another 5000 km2 underwater on the continental shelf. The basement consists of the Lachlan Fold Belt, and the New England Fold Belt is found to the north across the Hunter Thrust. It is a foreland basin, likely to be formed by compression loading. [7]

The first rocks formed in the Permian were the Dalwood Group and lower Shoalhaven Group. Material for this came from basaltic volcanoes to the north in the Hunter region. The Greta Coal Measures then formed in the north side in an alluvial fan from the mountains of the New England Orogen. The basin sank lower and sea water came much further inland, covering the Permian sediments and the basement further west, and the Maitland Group and upper Shoalhaven Group were deposited. The Muree/Nowra Sandstone formed in the centre of the basin. [7]

In the next stage the Hunter – Bowen Orogeny cause faulting and folding on the north side of the basin. In the Late Permian river and delta deposition formed the Tomago and Whittingham Coal Measures in the north. But deepening seawater formed the Kulnura Marine Tongue and Bulga Formation. In the southern part of the basin a delta formed the lower Illawarra Coal Measures. The Erins Vale Formation interrupts this. Marine transgression formed Dempsey Formation, Denman Formation, Bargo Claystone, and Ball Bone Formation. Beach deposition then formed Waratah/Watts Sandstone and the Darkes Forest Sandstone and Angus Place Sandstone. Over the beach land formed again with the Newcastle and Wollombi Coal Measures in the north, and upper Illawarra Coal Measures in the south. Early in the Triassic the New England Fold Belt was uplifted and an alluvial flood plain formed the Narrabeen group. The Bald Hill Claystone, which is a redbed containing laterite was formed by weathering of the Gerringong Volcanics. [7]

The Hawkesbury sandstone is the prominent rock found in Sydney, and also forming the top of escarpments in the area, such as the Illawarra escarpment. This is overlain by the fine sandstone of the Mittagong Formation [8] and the Wianamatta shale. [9]

The basin was later buried under 1 to 4 km of Jurassic and Cretaceous sediments. The Tasman Sea formed by rifting and underplating of the basin may have happened in Aptian times. This resulted in the upper sediment being completely eroded off. [7]

Great Artesian Basin

Part of the Great Artesian Basin is along the northern border of New South Wales and also extends north into Queensland. This is also known as Surat Basin. It occupies one fifth of the state of New South Wales. The eastern border extends from Bebo to Narrabri to Murrurundi to Dunedoo to Narromine. The basin was formed in the Jurassic and Cretaceous periods. [10]

The oldest Jurassic rocks in the basin are found in the northeast near the Queensland border. They are called Precipice Sandstone, [11] Evergreen Shale and Boxvale Sandstone, [12] Hutton Sandstone from Pliensbachian to Aalenian in age. [13] In the south east of the basin these deposits are known as Purlawaugh Formation which are aged between Pliensbachian to Bathonian. [14] The northern parts are then covered with coal and shale from the Injune Creek Group. [15] In the east they are covered with quartz sand, at the point where run off entered the basin called Blythesdale Group between Tithonian and Barremian [16] or Pillaga Sandstone which is now known as Pilliga Sandstone. [10] [17]

In the Cretaceous sea water entered and deposited shale from the Rolling Downs Group [18] which also contains some calcareous sandstone. Continental sediment also occasionally show in the Cretaceous. [10]

Most of the basin is covered by alluvium and lake deposits from the Cainozoic period, and this deposition continues till this day. [10]

Because the basin is an important site for artesian wells, it has been extensively drilled and much is known about the structure of the basement and geothermal temperature gradients. Prominent subsurface features are the Coonamble lobe of the Surat Basin, round around Moree and Coonamble. The Culgoa Ridge is underlain by metamorphic rocks, and is near Brewarrina. The Lila Trough is north of Bourke. The Eulo Shelf is underlain by granite and is southeast of Hungerford. The Bulloo Embayment north of White Cliffs is over 300 m deep and is disrupted on its west side by the Warratta Fault. The Quinyamble Trough extends in from South Australia. [10]

Clarence Moreton Basin

The Clarence Moreton Basin is in the far north east of the state around Lismore and Grafton, the basin extends into southern Queensland. It formed by oblique extension of the underlying Paleozoic New England Orogen basement. It consists of continental deposits, starting with a small amount of Triassic volcanic rocks and sedimentary sequences including coal beds, and then mostly Jurassic and Cretaceous sedimentary rocks. [19] The basin covers 16000 square kilometers. [20] The basin was named when the Clarence Basin (named after the Clarence River and Moreton Basin in Queensland were proved to be one structure. [19]

The first rocks in the Clarence Moreton Basin of New South Wales are the Chillingham Volcanics. These are from some time in the Triassic period, and for a band north and south of Chillingham. They consist of conglomerate at the base, Rhyolite, lithic rhyolitic tuff, and shale. [21] The Nymboida Coal measures extend from Nymboida to Kangaroo Creek. They consist of lithic sandstones (wackes, minor arenites), siltstone, polymictic conglomerate, coal, rhyolitic tuff, and basalt. The total thickness is over 1000 meters. The outcrop is 90 square kilometers, and it forms a north west trending band 29 km long on the southwest tip of the basin. [22] Fossils reveal a date of middle Triassic. A lower part is called Cloughers Creek Formation. [19] [23] The Basin Creek Formation [24] includes the coal mined at Nymboida. The Bardool Conglomerate forming a 180 m thick layer, [25] is also a unit in the coal measures. The conglomerate includes a 15 m thick layer of basalt exposed at Copes Creek. [19]

The Red Cliff Coal Measures are from late Triassic. It forms a belt 2.5 km wide and 19 km long from Buchanans Head trough Red Cliff. [26] The Evans Head Coal measure are correlated with these, but are further up the north coast at Evans Head. [27]

The basin was next uplifted and eroded and then deepened considerably and Bundamba group rocks form a complete V shape on both sides of the basin. In the northern parts the rock is mostly friable sandstone, but in the south it is divided into conglomerate below and siltstone above. The Laytons Range Conglomerate [28] rests on the basin floor and extends from Baryulgil, to Nymboida. The conglomerate often appears as a cliff. The Corindi Conglomerate is a local name for a hailstone sized gravel near Corindi. The Mill Creek Siltstone. [29] are often olive green or yellow-brown with bright red joint planes. [19]

The Marburg subgroup [30] extends for 225 km along the western side of the basin into Queensland from Corindi. It is mostly clay cemented cross bedded quartz sandstone, but this is interbedded with claystone and shale. At the base is the Blaxland Fossil Wood Conglomerate Member at Blaxlands Creek. The fossil wood is in the form of horizontal tree trunks up to 18 m long and 600 mm diameter. The fossilization process replaced the wood with limonite and hematite. [19] The Towallum Basalt is a 15-meter thick layer near Nymboida, Glenreagh and Moleton trig station overlying the Marburg formation. [19] The Walloon Coal Measures [31] forms a U shape around the east, south and west sides of the basin. It consists of claystone, shale, siltstone, arenites, and coal seams and the plant fossils in it show a Jurassic age. [31]

The next layer of rocks in the basin forming a nested U shape in its exposure is the Kangaroo Creek Sandstone. [32] This sandstone has saccharoidal texture, and glistens white and cream. This is not due to angular sand grains, but results from silica crystallization. It is up to 150 m thick. [19]

The Grafton Formation [33] is the sedimentary unit in the geographical centre of the basin. It is the youngest of the beds being between Late Jurassic and early Cretaceous. It occurs from Grafton to Casino consisting of soft sandstone, siltstone and claystone. Dolerite has intruded this at Glenugie Peak, and near Banyabba. [19]

During the Cainozoic, rifting along the east coast of Australia commenced and uplifted the eastern side of the Clarence Moreton Basin. [20] This resulted in the splitting off of the Lord Howe Rise and the opening of the ocean floor. [34]

Murray basin

Murray Basin Section.png

After Australia separated from Antarctica the Murray basin was formed. The basin floor only subsided slowly over time. [5] The basin became filled with up to 600 m of sediments during the Cenozoic. [35]

From Paleocene to Eocene the western side was flooded with sea water and deposited the Warina sand. [36] The sea withdrew and later in the Eocene silt and clay of the Olney Formation [37] were deposited. One minor sea incursion resulted in late Eocene resulted in the Buccleuch Formation [38] in South Australia. This group of deposits is termed the Renmark Group and was earlier known as Knight Group. [39]

The sea level rose again in Late Oligocene to mid Miocene forming the Murray Group of sediments, with marl and limestone in the deeper locations, and the Geera Clay [40] in the shallow waters. The rock units formed in the deeper water included the Ettric Formation, [41] the Winnanbool Formation [42] and the Mannum Formation limestone [43] with Gambier Limestone in South Australia. [44] [45] When sea level fell again in mid Miocene the deposited Geera clay and Olney Formation moved westward over the limestone. [5]

During Upper Miocene to Pliocene the sea rose and fell several times. The first sea rise formed the Murravian Gulf and resulted in clay and marl in the west called the Bookpurnong Formation, [46] and Calivil Formation [47] river and lake sand in the east. When the sea retreated in Early Pliocene, the Loxton Sands [48] also informally known as Loxton-Parilla Sands were formed on the beach on the shore of the emergent land. Locally heavy minerals have been concentrated by wave action including rutile zircon and ilmenite forming economic mining opportunities. [49]

Lake Bungunnia around 1Mya Lake Bungunnia of the Murray Basin.png
Lake Bungunnia around 1Mya

The Murray River became dammed by uplift of over 250 meters in the Grampians in Victoria during the Pleistocene about 2.5 Mya. The dam formed Lake Bungunnia, which reached 40000 km2 and deposited the Blanchetown Clay therein. [50] Higher rainfall of at least 500 mm per year kept the lake filled at first, but during later times rainfall was insufficient and saline lakes formed, depositing dolomite. Even today some saline lakes remain as a remnant of the vast lake. [51] The Murray River carved out a new path to the sea via Murray Bridge replacing its previous exit at Portland, Victoria. The lake was gone by about 0.7 Mya.

The Pooraka Formation [52] formed in the north west due to increased erosion resulting in colluvium depositing. The colluvium forms fans, cones and scree slopes, and often contains clay and breccia. In the flat areas the Shepparton Formation [53] also resulted from river deposits of floodplain clay. [5]

Most of the existing surface dates from Quaternary period. The river deposits from the east have been progressively overlaying the marine deposits further west, as the shore line receded. Within the Pleistocene deposits are three layers of sand that are aquifers, deposited during higher rainfall periods of the interglacials. The floodplain deposits from the current rivers are the Coonambidgal Formation, however this term is used informally for the older Pleistocene flood deposits as well. [54] During the dryer glacial periods the area was arid. [55]

Oaklands basin

The Oaklands Basin covers approximately 3 800 square kilometres in the Riverina district of southern New South Wales, between the towns of Mulwala, Jerilderie, Griffith, Coleambly, Oaklands and Albury. This Permo-Triassic basin trends north-northwest-south-southeast and is concealed beneath the south-eastern portion of the Murray Basin. The basin overlies the Ovens Graben (Ovens Valley Graben in Victoria) which extends from the Murrumbidgee River west of Darlington Point in New South Wales to Wangaratta in Victoria. It is approximately 25 km wide at Oaklands and approximately 15 km wide at its northern extent. The Oaklands Basin hosts to more than 1000 m thick sediments. The basin was first discovered in 1916 when water drillers discovered coal near Coorabin. Coal has been the main focus for exploration within the basin since this time. Extensive coal exploration drilling has been undertaken, mostly in the Coorabin area. In addition two coal drilling programs by the NSW Department of Industry, designed to help define the limits of the basin, have resulted in wide-spaced drilling coverage over most of the basin. Petroleum exploration within the basin has been minimal, consisting of a small number of geophysical surveys and two stratigraphic wells. In 2009 four new lines of high quality 2D seismic have been acquired by DTIRIS (formerly the NSW Department of Industry and Investment). This survey has further delineated the boundaries of the basin, established the thickness of the sediment fill and imaged the structures of the Ovens Valley Graben along the margin and central portion of the basin. [56]

Volcanic rocks

New South Wales has 26,000 km2 of volcanic rocks from Cainozoic period. In the north east major outcrops of volcanic rocks are found between Warialda to Glen Innes and south to Armidale, the Liverpool Range, Barrington Tops, Nandewar Range near Narrabri, the Warrumbungles, and the Tweed Volcano. [1]

Geological history

In the Cambrian and earlier period only the far west of New South Wales existed in its present form. It was joined to what is now Western North America in the Rodinia supercontinent. North America was detached opening up the Pacific Ocean. In the Ordovician period, sediment deposited on the newly formed sea floor, and in the Silurian a back arc basin behind a chain of volcanoes was formed and then accreted back onto the east coast of Australia to form the Lachlan Fold Belt. The main structure in this is north-south, and this is reflected nowadays with the orientation of rivers and mountain ranges.


Collecting fossils is legal in New South Wales under the New South Wales Mining Act with ownership applying to the land owner. [57] Opalised fossils about 100 Mya occur at Lightning Ridge. [58] The Wellington Caves contain megafauna fossils from 4 Mya to 30,000 years old. These include the marsupial lion and giant kangaroo. [59]

At Canowindra is the most important fish fossil site in the world. It dates from 360 Mya in the Devonian and includes Groenlandaspis, Canowindra grossi, Remigolepis walkeri and Bothriolepis yeungae. A museum is there called Age of Fishes Museum. At Cuddie Springs is a fossil site containing Diprotodon and the Thunder Bird.

The Griman Creek Formation contains Cretaceous dinosaur fossils. [60]

Economic geology


A variety of mines occur in New South Wales, including Broken Hill Ore Deposit the world's richest zinc and silver mine; Bowdens Silver Deposits near Mudgee; Cadia-Ridgeway Mine 20 km south of Orange; Lake Cowal Campaign and Barrick Gold 125 km sw of Parkes; CSA Mine near Cobar mines copper; Endeavour Mine extracts zinc, is 43 km nw of Cobar; Ginko Mineral Sand Deposit is 30 km west of Pooncarie; Murrawombie Mine; Hillgrove Gold Mine 23 km east of Armidale; [61] Mineral Hill 67 km NNW of Condobolin; Northparkes is 26 km north of Parkes mining copper; Peak Gold Mine 8 km southeast of Cobar; Peak Hill Gold Mine 50 km north of Parkes; Prungle Mineral Sand Project 50 km north east of Euston; Tritton 18 km north of Hermidale; Twelve Mile Mineral Sand Project 40 km east of Pooncarie. [62]


The oldest coal seam fire in the world has been burning for 6000 years at Burning Mountain near Wingen, New South Wales. [63]

The Newcastle earthquake killed 13 people on 28 December 1989. [64]



New South Wales Department of Mines and Agriculture The Copper-Mining Industry of New South Wales 1899 CARNE(1899) The Copper-Mining Industry.jpg
New South Wales Department of Mines and Agriculture The Copper-Mining Industry of New South Wales 1899


The Department of Mines commenced in late 1874, and the Geological Survey of New South Wales was brought into existence on 1 January 1875. Charles Smith Wilkinson was its first supervisor. In the 1950s to 1970s the administering body for mines was the New South Wales Department of Mines or New South Wales Department of Mines and Agriculture. Before 2004 New South Wales Department of Mineral Resource After 2004 until July 2009 mining in New South Wales was administered by the New South Wales Department of Primary Industries. [65] and then New South Wales Department of Industry & Investment.

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Geology of Tanzania

The geology of Tanzania began to form in the Precambrian, in the Archean and Proterozoic eons, in some cases more than 2.5 billion years ago. Igneous and metamorphic crystalline basement rock forms the Archean Tanzania Craton, which is surrounded by the Proterozoic Ubendian belt, Mozambique Belt and Karagwe-Ankole Belt. The region experienced downwarping of the crust during the Paleozoic and Mesozoic, as the massive Karoo Supergroup deposited. Within the past 100 million years, Tanzania has experienced marine sedimentary rock deposition along the coast and rift formation inland, which has produced large rift lakes. Tanzania has extensive, but poorly explored and exploited natural resources, including coal, gold, diamonds, graphite and clays.

The geology of Morocco formed beginning up to two billion years ago, in the Paleoproterozoic and potentially even earlier. It was affected by the Pan-African orogeny, although the later Hercynian orogeny produced fewer changes and left the Maseta Domain, a large area of remnant Paleozoic massifs. During the Paleozoic, extensive sedimentary deposits preserved marine fossils. Throughout the Mesozoic, the rifting apart of Pangaea to form the Atlantic Ocean created basins and fault blocks, which were blanketed in terrestrial and marine sediments—particularly as a major marine transgression flooded much of the region. In the Cenozoic, a microcontinent covered in sedimentary rocks from the Triassic and Cretaceous collided with northern Morocco, forming the Rif region. Morocco has extensive phosphate and salt reserves, as well as resources such as lead, zinc, copper and silver.

The geology of Alberta encompasses parts of the Canadian Rockies and thick sedimentary sequences, bearing coal, oil and natural gas, atop complex Precambrian crystalline basement rock.

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.

The geology of Afghanistan includes nearly one billion year old rocks from the Precambrian. The region experienced widespread marine transgressions and deposition during the Paleozoic and Mesozoic, that continued into the Cenozoic with the uplift of the Hindu Kush mountains.

The geology of Bulgaria consists of two major structural features. The Rhodope Massif in southern Bulgaria is made up of Archean, Proterozoic and Cambrian rocks and is a sub-province of the Thracian-Anatolian polymetallic province. It has dropped down, faulted basins filled with Cenozoic sediments and volcanic rocks. The Moesian Platform to the north extends into Romania and has Paleozoic rocks covered by rocks from the Mesozoic, typically buried by thick Danube River valley Quaternary sediments. In places, the Moesian Platform has small oil and gas fields. Bulgaria is a country in southeastern Europe. It is bordered by Romania to the north, Serbia and Macedonia to the west, Greece and Turkey to the south, and the Black Sea to the east.


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