Elsevier Encyclopedia of Geology

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the Palaeozoic Lachlan Orogen. Extensive eruption of

continental flood basalts (Kalkarinji large igneous pro-

vince) of the 510-My-old Antrim Plateau Volcanics

and the Table Hill Volcanics in northern and western

Australia may reflect further mantle plume activity

coincident with this collision.

Mineral Deposits

The Proterozoic rocks of Australia are endowed with

substantial mineral resources, containing significant

deposits of iron ore, manganese, uranium, gold,

copper, lead, zinc, silver, nickel, and diamond

(Figure 8)(see Mineral Deposits and Their Genesis).

World-class hematite deposits (Mount Whaleback,

Tom Price) have been produced by enrichment of

the banded iron formations of the Hamersley Basin

during the Palaeoproterozoic. The highest grade low-

P deposits (62–69% Fe), have been interpreted as the

product of burial metamorphism of original super-

gene enrichment prior to 1840 Ma. More recently,

they have been reinterpreted as the product of hypo-

gene processes related to the expulsion of fluids

into the foreland of the Ophthalmian Orogeny

(2200 Ma). Proterozoic iron ore deposits have also

been mined in the Palaeoproterozoic iron formations

of the Hutchison Group in the Gawler Craton, and

from enrichment of ferruginous placer deposits in the

upper Kimberley Group in the Kimberley Basin (Koo-

lan Island). Manganese has been mined from super-

gene deposits (Woodie Woodie) associated with

Palaeoproterozoic karst developed on dolomites in

the eastern Hamersley Basin.

‘Unconformity-related’ uranium ( Au  platinum

group elements) deposits (Rum Jungle, Alligator

River) are found in Palaeoproterozoic sedimentary

successions overlying predominantly Archaean base-

ment rocks in northern Australia, and may be related

to interaction of highly oxidized, acidic and Ca-rich

meteoric brine with reduced basement fluids. Similar

deposits have been found elsewhere in the Australian

Proterozoic, including Kintyre, where Neoprotero-

zoic metasedimentary rocks overlie Palaeopro-

terozoic basement. Metasomatic U deposits and the

metamorphic-related Mary Kathleen deposit occur in

Palaeoproterozoic rocks of the Mount Isa Inlier.

Gold is found in a number of settings throughout

the Proterozoic, and historic production is related to

generally small lode-gold occurrences and associated

alluvial deposits. Major gold (Cu) mines have been

developed at Telfer in the Yeneena Basin, and at

The Granites in the Granites–Tanami Complex. Min-

eralization is centred on metasedimentary rocks in

structural domes and is hypogene, related to the

emplacement of granitic pluton(s) near a periodically

reactivated, regional-scale, fluid-focusing structure,

often a strike–slip fault. ‘Proterozoic Cu–Au deposits’

are found associated with iron oxide in the Tennant

Creek Inlier, at Olympic Dam in the northern Gawler

Craton, and in the Mount Isa Inlier (Ernest Henry).

There is usually a spatial and temporal relationship

between this style of deposit and granite intrusion

(e.g., Olympic Dam and the 1590-My-old Hiltaba

Suite). Cu mineralization at Mount Isa is regarded

as syn-deformational, late metamorphic, and is a

separate event from Pb–Zn–Ag mineralization. The

Mount Isa orebody is a world-class example of strati-

form sediment-hosted Pb–Zn–Ag mineralization, pro-

duced by oxidized fluids moving through the sediment

pile and being deposited either by seafloor exhalative

processes or within the sediments. A similar orebody

is present at McArthur River. The Broken Hill ore-

body is generally regarded as a metamorphosed

example of stratiform sediment-hosted minerali-

zation, although syn-metamorphic, skarn-type pro-

cesses may have modified it. Volcanic-hosted massive

sulphide (VHMS) Pb–Zn mineralization has been

found at Koongie Park in the Halls Creek Orogen.

Nickel mineralization in the Proterozoic, together

with platinum group elements, Cu, and V, is generally

associated with layered mafic–ultramafic intrusions

such as those in the Halls Creek Orogen (Sally

Malay). Large, layered intrusions are also present in

the Musgrave Complex (Giles Complex–Nebo and

Babel deposits), the Albany–Fraser Orogen (Fraser

Complex), and the Arunta Inlier.

The Argyle diamond mine, which is the world’s

largest, is developed on the 1200-My-old AK1

lamproite pipe intruded into the Halls Creek

Orogen. Proterozoic diamondiferous kimberlites

from 815 Ma are present in the Kimberley Basin

(see Igneous Rocks: Kimberlite).

Further Reading

Australian Geological Survey Organisation (1998) Geology

and mineral potential of major Australian mineral pro-

vinces. AGSO Journal of Australian Geology and

Geophysics 17(3): 1–260.

AUSTRALIA/Proterozoic 221

Australian Geological Survey Organisation (1998) Explor-

ation models for major Australian mineral deposit types.

AGSO Journal of Australian Geology and Geophysics

17(4): 1–313.

Cawood PA and Tyler IM (2004) Assembling and reactivat-

ing the Proterozoic Capricorn Orogen: lithotectonic

elements, orogenies, and significance. Precambrian

Research 128: 201–218.

Collins WJ and Shaw RD (eds.) (1995) Time limits on

tectonic events and crustal evolution using geochron-

ology: some Australian examples Precambrian Research

71: 1–346.

Direen NG and Crawford AJ (2003) The Tasman Line:

where is it, what is it, and is it Australia’s Rodinian

breakup boundary? Australian Journal of Earth Sciences

50: 491–502.

Drexel JF and Parker AJ (1993) The Geology of South

Australia: Volume 1. The Precambrian. Geological

Survey of South Australia, Bulletin 54. Adelaide:

Geological Survey of South Australia.

Fitzsimons ICW (2003) Proterozoic basement provinces of

southern and south-western Australia, and their correl-

ation with Antarctica. In: Yoshida M, Windley BF, and

Dasgupta S (eds.) Proterozoic East Gondwana: Super-

continent Assembly and Breakup. Geological Society of

London, Special Publication 206, pp. 93–130. London:

Geological Society of London.

Geological Survey of Western Australia (1990) Geology

and Mineral Resources of Western Australia. Western

Australia Geological Survey, Memoir 3. East Perth:

Geological Survey of Western Australia.

Glikson AY, Stewart AJ, Ballhaus CG, Clarke GL, Feeken

EHJ, Leven JH, et al. (1996) Geology of the Western

Musgrave Block, Central Australia, with Particular

Reference to the Mafic–Ultramafic Giles Complex. Austra-

lian Geological Survey Organisation, Bulletin 239.

Canberra: Australian Geological Survey Organisation.

Hoatson DM and Blake DH (2000) Geology and Economic

Potential of the Palaeoproterozoic Layered Mafic–

Ultramafic Intrusions in the East Kimberley, Western

Australia. Australian Geological Survey Organisation,

Bulletin 246. Canberra: Australian Geological Survey

Organisation.

Hunter DR (1981) Precambrian of the Southern Hemi-

sphere. Developments in Precambrian Geology 2.

Amsterdam: Elsevier.

Korsch RJ (ed.) (2002) Thematic issue: geodynamics of

Australia and its mineral systems: technologies, syntheses

and regional studies. Australian Journal of Earth Sciences

49(4): 593–771.

Myers JS, Shaw RD, and Tyler IM (1996) Tectonic evolu-

tion of Proterozoic Australia. Tectonics 15: 1431–1446.

Powell C McA and Meert JG (eds.) (2001) Assembly

and breakup of Rodinia. Precambrian Research

110(1-4): 1–386.

Southgate PN (ed.) (2000) Thematic issue: Carpentaria–Mt

Isa zinc belt: basement framework, chronostrati-

graphy and geodynamic evolution of Proterozoic suc-

cessions. Australian Journal of Earth Sciences 47(3):

337–657.

Walter MR (ed.) (2000) Neoproterozoic of Australia.

Precambrian Research 100(1-3): 1–433.

Phanerozoic

J J Veevers, Macquarie University, Sydney, NSW,

Australia

Introduction

This account of Phanerozoic (544–0 Ma) Australia is

told through a timetable of events (Figure 1), a set of

fold-belt cross-sections (Figure 2), and a set of maps,

which stretch from the initial Pan-Gondwanaland

phase to the tectonics of today (Figures 3–27).

Phanerozoic Australia developed through three

stratitectonic regimes (uniform plate tectonics and

climate at similar or slowly changing latitude),

which generated depositional successions of distinct

facies that are bounded by unconformities at the

margins and by stratigraphical lacunas in the inter-

ior (Figure 1). These stratitectonic regimes are

summarized in Table 1.

p0015Terranes successively broke off the west and north-

west along divergent margins with rim basins. The

eastern convergent margin grew by accretions of arc-

subduction complexes during successive rollback of

the trench. Changes of regime were driven by global

events (see Gondwanaland and Gondwana; Austra-

lia: Tasman Orogenic Belt): the 544 Ma aftermath of

the Pan-Gondwanaland collisional rotations and the

onset of an active Pacific margin; the 320 Ma colli-

sional merger of Gondwanaland and Laurussia to

form Pangaea and the subsequent far-field contrac-

tional stress in central Australia, with ensuing tecton-

ics driven by Pangaean-induced heat; and the 99 Ma

change in the azimuth of subduction of the Pacific

Plate from head-on to side-swipe.

The 650–580 Ma collision of East Gondwanaland

and West Gondwanaland resulting from the closure

of the Mozambique Ocean, together with con-

tinued Pan-Gondwanaland contraction until 500 Ma,

generated the Mozambique Orogenic Belt and an

222 AUSTRALIA/Phanerozoic

orthogonal belt through Prydz Bay to Cape Leeuwin,

with distributed thrusting and associated meta-

morphism in the rest of Australia. These events,

together with the inception of subduction of the

Palaeo-Pacific Plate beneath Antarctica–Australia at

about 550 Ma, inaugurated Phanerozoic Australia.

The events along the Pacific margin during the

Palaeozoic are shown in the set of cross-sections in

Figure 1 Timetable of events during the past 600 Ma. Columns from left to right are divergent margins (northwest (NW) with break-off

of terranes and west (W) represented by the Carnarvon Basin), depositional facies (glacial, coal, carbonate, evaporites, volcanics),

and southern region (S), the centre (C), across the Tasman Lines to the Tasman Fold Belt System in the east (E) and north-east (NE).

Under ‘events’, the palaeolatitude of Alice Springs is plotted and the chief deformations are listed. Under ‘regime’, the last

Neoproterozoic supersequences and the three Phanerozoic regimes are indicated. Under ‘Pangaea’, the stages of Pangaea B and

A are indicated and the 320 Ma merger is marked by a filled circle. BU, breakup; carb, carbonate; evaps, evaporites; PRN, Petermann

Ranges Nappe; QLD, Queensland; SFS, seafloor spreading; volcs, volcanics. Reproduced with permission from Veevers JJ (ed.) (2000)

Billion-Year Earth History of Australia and Neighbours in Gondwanaland. Sydney: GEMOC Press.

AUSTRALIA/Phanerozoic 223

Figure 2 Cross-sections of the lithosphere of the Tasman Fold Belt System developing between the fixed Proterozoic Craton and the

active Pacific Plate. Ratio of vertical to horizontal scales is 1 : 1; the vertical scale has ticks every 10 km; the horizontal scale has ticks

every 100 km. CC, continental crust; CUM, continental upper mantle; OUM, oceanic upper mantle; CURN, Curnamona Craton; MC,

microcontinent. Reproduced with permission from Veevers JJ (ed.) (2000)

Billion-Year Earth History of Australia and Neighbours in

Gondwanaland

. Sydney: GEMOC Press.

224 AUSTRALIA/Phanerozoic

Figure 2. The initial dispersal of microcontinents by

growth of a marginal basin and their return by closure

of the basin were followed by subduction, generating

a magmatic arc behind which granites were emplaced

in an extended region. When the subducted slab shal-

lowed, the crust was shortened; when it steepened,

the trench rolled back in front of a growing marginal

basin.

The events across Australia and neighbouring

Antarctica are shown in plan view in the set of

palaeogeographical figures.

Latest Neoproterozoic–Earliest

Cambrian (550–530 Ma)

The Uluru regime was inaugurated by collisions in

West Gondwanaland and subduction in Antarctica,

which deformed central and north-western Australia

to produce mountain ranges and intervening basins

where coarse arkose was deposited at the foots of the

mountains, as at Uluru (Figure 3). In the south-west,

the Prydz-Leeuwin Belt was terminally metamorph-

osed, and its periphery was intruded by a swarm of

dykes.

In the south-east, the Kanmantoo Marginal Basin

grew by back-arc spreading behind the subducting

Figure 3 Latest Neoproterozoic–earliest Cambrian (550–530

Ma) palaeogeography. The parallel lines crossing central-

eastern Australia are the Tasman Line (heavy broken line) and

the Tasman Toe-Line (light broken line), which mark the eastern

outcrops of the Proterozoic craton and its wedge-out, respect-

ively. KMB, Kanmantoo Marginal Basin; P-LB, Prydz-Leeuwin

Belt. Reproduced with permission from Veevers JJ (ed.) (2000)

Bil-

lion-Year Earth History of Australia and Neighbours in Gondwanaland

Sydney: GEMOC Press.

Figure 4 Early and Middle Cambrian (530–510 Ma) palaeo-

geography. Legend as in Figure 3. Reproduced with permission

from Veevers JJ (ed.) (2000) Billion-Year Earth History of Australia and

Neighbours in Gondwanaland

. Sydney: GEMOC Press.

Figure 5 Late Cambrian (510–490 Ma) palaeogeography.

Legend as in Figure 3. Reproduced with permission from

Veevers JJ (ed.) (2000) Billion-Year Earth History of Australia and

Neighbours in Gondwanaland

. Sydney: GEMOC Press.

Figure 6 Early Ordovician (490–458 Ma) palaeogeography. The

cooling Ross and Delamerian granites are shown in black.

Legend as in Figure 3. Reproduced with permission from

Veevers JJ (ed.) (2000)

Billion-Year Earth History of Australia and

Neighbours in Gondwanaland

. Sydney: GEMOC Press.

AUSTRALIA/Phanerozoic 225

Palaeo-Pacific Plate and wedged microcontinents off

the mainland in the first episode of the Tasman Fold

Belt System (Figure 2ii). In the north-east, an accre-

tionary wedge grew in front of the trench. Central

Australia was flooded by a shallow sea that lapped

over the Uluru arkose, and another arm of the sea

crossed the north. On the Antarctic side of a trans-

form fault, another accretionary wedge grew in front

of the trench and the first Ross granites were

emplaced along the Transantarctic Mountains.

Early–Middle Cambrian 530–510 Ma

Basalt flows over much of the north and centre

(Figure 4) were crossed by the Uluru Shelf, which

connected with the North China Shelf. An island in

Figure 7 Early Silurian (443–425 Ma) palaeogeography. MM,

Melbourne-Mathinna Terrane. Legend as in Figure 3. Repro-

duced with permission from Veevers JJ (ed.) (2000)

Billion-Year

Earth History of Australia and Neighbours in Gondwanaland

. Sydney:

GEMOC Press.

Figure 8 Early Devonian (418–394 Ma) palaeogeography.

Legend as in Figure 3. Reproduced with permission from

Veevers JJ (ed.) (2000)

Billion-Year Earth History of Australia and

Neighbours in Gondwanaland

. Sydney: GEMOC Press.

Figure 9 Middle and Late Devonian (394–362 Ma) palaeogeog-

raphy. COM–YAL–EDEN, Comerong–Yalwal–Eden Rift Zone;

ORD, Ord Basin; CVMP, Central Victorian Magmatic Province.

Legend as in Figure 3. Reproduced with permission from

Veevers JJ (ed.) (2000)

Billion-Year Earth History of Australia and

Neighbours in Gondwanaland

. Sydney: GEMOC Press.

Figure 10 Postulated extent of the mid-Carboniferous ice-

sheet. Reproduced with permission from Veevers JJ (ed.) (2000)

Billion-Year Earth History of Australia and Neighbours in Gondwanaland.

Sydney: GEMOC Press.

226 AUSTRALIA/Phanerozoic

the north-east was intruded by granite and deformed

behind the trench. The Kanmantoo Marginal Basin

started to close by north-eastward-directed subduc-

tion beneath an overlying volcanic arc (Figure 2iii).

In Antarctica, an accretionary wedge continued to

grow above the westward-subducting limb, and re-

lated Ross granites and marine volcanics were

erupted.

Late Cambrian (510–490 Ma)

At the tectonothermal climax of Gondwanaland,

granites stretched from the Antarctic Peninsula

through the Transantarctic Mountains to Tasmania

(Figure 5), and the Delamerian granites were gener-

ated during closure of the marginal basin to form the

Kanmantoo Fold Belt (Figure 2iv). The trench con-

tinued past north Queensland along a margin with a

wide accretionary prism that was metamorphosed

and intruded by plutons at 500 Ma.

In the west, uplift along the Darling Fault and within

the Prydz-Leeuwin Belt shed fans of Tumblagooda

sand into the nascent Perth–Carnarvon Basin. In the

north-east, the King Leopold and Halls Creek Fold

Belts were terminally metamorphosed and thrusted,

and the enclosed block was uplifted and stripped.

Early Ordovician (490–458 Ma)

p0060The Delamerian–Ross Fold Belt, the zone of deform-

ation with cooling granite (black dots), was intensely

denuded in a tropical setting in which labile minerals

and rock fragments were weathered away to provide a

copious amount of quartzose sediment downslope to

Figure 11 Latest Carboniferous–earliest Permian (302-280 Ma)

palaeogeography. Uplands are: I, ancestral Great Western

Plateau; II, Central; III, Central-Eastern; IV, ancestral Eastern

Australian foreswell; V, ancestral Kimberley Plateau; XX, Ross.

Basins are 1, Bonaparte; 2, Galilee; 3, Cooper; 4, Pedirka; 5,

Arckaringa; 6, Canning; 7, Officer; 8, Carnarvon–Perth; 9, Collie;

11, Oaklands; 12, Tasmania; 13, Sydney; 14, Gunnedah; 15,

Bowen. Bullseyes indicate glacigenic sediment in mines. Coarse

pattern, ice flow; solid blue, outcrops of glacigenic sediment;

coarse blue stipple, subsurface glacigenic sediment; fine stipple,

inferred glacigenic sediment. Red lines (west) indicate structure

formed during Extension I. Legend as in Figure 3. Reproduced

with permission from Veevers JJ (ed.) (2000)

Billion-Year Earth

History of Australia and Neighbours in Gondwanaland

. Sydney:

GEMOC Press.

Figure 12 Permian (280–258 Ma) palaeogeography. C, coal;

GOZ, Gogango Overfolded Zone; red squares, granite; red tri-

angles, tuff. Legend as in Figure 3. Reproduced with permission

from Veevers JJ (ed.) (2000)

Billion-Year Earth History of Australia and

Neighbours in Gondwanaland

. Sydney: GEMOC Press.

Figure 13 Late Permian (258–250 Ma) palaeogeography. Red

triangle, tuff. Legend as in Figure 3. Reproduced with permission

from Veevers JJ (ed.) (2000) Billion-Year Earth History of Australia and

Neighbours in Gondwanaland

. Sydney: GEMOC Press.

AUSTRALIA/Phanerozoic 227

Australia (Figure 6). Westward-directed subduction of

the Palaeo-Pacific Plate beneath Eastern Australia

generated a volcanic arc that stretched 3000 km north-

wards in front of a marginal basin (Figure 2v). Quart-

zose turbidites were shed eastwards (transversely)

from the Delamerian upland, and volcanogenic sedi-

ment was shed from the volcanic arc. Turbidites were

shed northwards (longitudinally) from Antarctica, as

shown by 700–500 Ma zircons, along the fore-arc

basin and abyssal plain in vast submarine fans, com-

parable to the modern Bengal fan. Behind the shelf,

the Larapintine Sea crossed the interior towards the

western sea, which intermittently advanced across the

Tumblagooda sand.

Figure 14 Early Triassic (250–242 Ma) palaeogeography.

Legend as in Figure 3. Reproduced with permission from

Veevers JJ (ed.) (2000) Billion-Year Earth History of Australia and

Neighbours in Gondwanaland

. Sydney: GEMOC Press.

Figure 15 Early–Middle Triassic (242–234 Ma) palaeogeog-

raphy. Red, rejuvenated and initiated faults and depositional

axes; Q, quartzose sandstone. Legend as in Figure 3. Repro-

duced with permission from Veevers JJ (ed.) (2000)

Billion-Year

Earth History of Australia and Neighbours in Gondwanaland

. Sydney:

GEMOC Press.

Figure 16 Mid-Triassic (234–227 Ma) palaeogeography.

Legend as in Figure 3. In the northern Canning Basin, an anti-

clinal axis (red line crossed by double-headed arrow) formed

between transcurrent faults (red lines) with black arrows. Repro-

duced with permission from Veevers JJ (ed.) (2000)

Billion-Year

Earth History of Australia and Neighbours in Gondwanaland

. Sydney:

GEMOC Press.

Figure 17 Late Triassic (227–200 Ma) palaeogeography. The

double-headed barbs on the trench indicate the change from

shallowly dipping to steeply dipping subduction. Legend as in

Figure 3. The red lines in the west represent faults. Reproduced

with permission from Veevers JJ (ed.) (2000)

Billion-Year Earth

History of Australia and Neighbours in Gondwanaland

. Sydney:

GEMOC Press.

228 AUSTRALIA/Phanerozoic

Early Silurian (443–425 Ma)

Closure of the marginal basins in eastern Australia

generated the Benambran and related highlands

(Figure 7 and Figure 2vi). The Rodingan uplift in

the centre shed the Mereenie Sandstone. In the Can-

ning Basin, the Sahara Formation was deposited in a

Figure 18 Early and Middle Jurassic (200–160 Ma) palaeo-

geography. The deep red shading represents basalt or dolerite

within the large igneous field (pink). Legend as in Figure 3.

Reproduced with permission from Veevers JJ (ed.) (2000)

Billion-

Year Earth History of Australia and Neighbours in Gondwanaland

Sydney: GEMOC Press.

Figure 19 Late Jurassic (160 –144 Ma) palaeogeography.

Legend as in Figure 3. Reproduced with permission from

Veevers JJ (ed.) (2000) Billion-Year Earth History of Australia and

Neighbours in Gondwanaland

. Sydney: GEMOC Press.

Figure 20 Neocomian to Aptian (140.5–115 Ma) palaeogeog-

raphy. Legend as in Figure 3. Reproduced with permission

from Veevers JJ (ed.) (2000) Billion-Year Earth History of Australia

and Neighbours in Gondwanaland

. Sydney: GEMOC Press.

Figure 21 Cenomanian (99–93 Ma) palaeogeography. Red

arrows, previous velocities; black arrows, prospective velocities

(which are unchanged in Australia but swerve through 70



in the

Pacific Plate); double line, detachment fault; yellow and tan

shading, lower-plate margin (Lord Howe Rise), white dotted

line, division of drainage; CD, Ceduna depocentre; green, eroding

uplands; oblique orange lines, south-western drainage into

Australian–Antarctic depression; red horizontal shading, Whit-

sunday Volcanic Province; red dots, 99 Ma alkaline volcanics;

light blue, carbonate deposition. Legend as in Figure 3. Repro-

duced with permission from Veevers JJ (ed.) (2000)

Billion-Year

Earth History of Australia and Neighbours in Gondwanaland

. Sydney:

GEMOC Press.

AUSTRALIA/Phanerozoic 229

restricted sea. In the Carnarvon Basin, the Ajana

Formation succeeded the Tumblagooda Sandstone.

In the Petrel Sub-Basin, salt was probably deposited

during the Silurian and Devonian. Western Tasmania

was covered by a shallow sea, while the Melbourne–

Mathinna terrane slid past on its way to docking at

400 Ma.

Early Devonian (418–394 Ma)

p0070The New Zealand terranes amalgamated at 415 Ma,

and north-east and West Tasmania amalgamated at

400 Ma (Figure 8). In south-east Australia, relocation

of the trench was accompanied by wide back-arc ex-

tension and emplacement of granite (Figure 2vii). The

Adavale Basin was initiated with flows of andesite.

Farther north, inner shallow-marine and outer deep-

marine deposits were flanked by granitic plutons. A

group of nonmarine deposits (Cravens Peak, Dulcie,

Duerdin, and Mereenie) was deposited in the centre,

salt in the Petrel Sub-Basin, aeolian and playa deposits

of the Tandalgoo Formation in the Canning Basin,

and the Kopke redbeds of the Carnarvon Basin.

Middle and Late Devonian

(394–362 Ma)

Granodiorite was erupted in North Victoria Land

during continuing westward-directed subduction

(Figure 9). Following the contractional Tabberab-

beran Orogeny, plutonic rocks were emplaced

and volcanic rocks were erupted in a broad zone in

Tasmania, Victoria, and New South Wales, which

included the Comerong–Yalwal–Eden volcanic rift.

Fluvial sediment was deposited in the Barka, Lambie,

Figure 22 Eocene (35 Ma) palaeogeography. Legend as in

Figure 3. Reproduced with permission from Veevers JJ (ed.)

(2000) Billion-Year Earth History of Australia and Neighbours in Gond-

wanaland

. Sydney: GEMOC Press.

Figure 23 Miocene (24–5 Ma) palaeogeography. Numerals in-

dicate the times (Ma) at which the terranes docked. The blue

oblique shading represents marine to nonmarine sediment.

Legend as in Figure 3. Reproduced with permission from

Veevers JJ (ed.) (2000)

Billion-Year Earth History of Australia and

Neighbours in Gondwanaland

. Sydney: GEMOC Press.

Figure 24 Pleistocene (1.8 Ma to 10 ka) palaeogeography. Re-

produced with permission from Veevers JJ (ed.) (2000)

Billion-Year

Earth History of Australia and Neighbours in Gondwanaland

. Sydney:

GEMOC Press.

230 AUSTRALIA/Phanerozoic

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