Except where noted and discussed otherwise, the classification followed in this report adopts the current formal stratigraphic nomenclature from the Australian Stratigraphic Unit Database (Geoscience Australia, 2012). Figure 19 is a stratigraphic column for the Galilee subregion. The Galilee Basin stratigraphy is after McKellar and Henderson (2012), and the Eromanga Basin stratigraphy after Ransley et al. (2012).
For Figure 19, the stratigraphy is subdivided into three chronostratigraphic intervals: the Late Carboniferous to Early Triassic (Galilee Basin), Middle Jurassic to Middle Cretaceous (Eromanga Basin) and the Cenozoic. The Galilee Basin stratigraphy is further subdivided into three geographical regions, because of the structural influence on the paleogeography of the basin. The northern section includes units around the northern margin of the Galilee Basin as well as the Lovelle Depression. The eastern section covers the Koburra Trough, Aramac Trough and westwards to the Maneroo Platform. The southern section applies to areas of Galilee Basin south of the Barcaldine Ridge.
The Galilee Basin stratigraphy presented in this report is based on the most recent compilation of McKellar and Henderson (2013). Galilee Basin stratigraphic units for most part unconformably overlie the older geological basement terranes and the Adavale, Belyando and Drummond basins. Conformable stratigraphic relations may exist in places between Late Carboniferous Galilee and Drummond basins (Van Heeswijck, 2010).
Galilee Basin stratigraphy is complicated by local variations in the timing of deposition in different parts of the basin. Broadly there are two major depositional intervals; the Late Carboniferous to Early Permian Joe Joe Group and a Late Permian to Middle Triassic sequence. The Late Permian to Middle Triassic sequence includes the: Betts Creek beds, Rewan Group, Clematis Group and Moolayember Formation. A significant unconformity separates the Lower and Upper Permian sedimentary sequences. Further information on paleogeography and stratigraphy of the Galilee Basin is documented in Scott et al. (1995), Hawkins and Green (1993) and Wells (1989).
Joe Joe Group
Lake Galilee Sandstone (Late Carboniferous): fine- to medium-grained quartzose sandstone with minor mudstone. It is the basal unit for the Koburra Trough and outcrops along the eastern margin of the Galilee Basin ; Bradshaw et al., 2009). The maximum stratigraphic thickness is 260 m.
Jericho Formation (Late Carboniferous): consists of diamictite, conglomerate, and sandstone with interbedded siltstone. This formation records up to three glacial – interglacial events, with interglacial sediments deposited in lacustrine to fluvial environments (Jones and Fielding, 2008). The Jericho Formation outcrops along the eastern margin of the Galilee Basin, but also occurs in the Koburra Trough and southern Galilee Basin. The Jericho Formation is up to 760 m thick and includes the Oakleigh Siltstone Member. It was recognised as a distinct seismic facies (G1) by Van Heeswijck (2010).
Jochmus Formation (Early Permian): volcanic-lithic sandstones with interbedded silty tuff. It includes the Edie Tuff Member. The Boonderoo beds, which outcrop along the north-eastern margin of the Galilee Basin, are an equivalent of the Upper Jericho and Jochmus formations (McKellar and Henderson, 2013). Much of the Jochmus Formation was deposited in fluvial environments with minor glaciogenic influence. It occurs in the Koburra Trough, Aramac Depression, and the Lovelle Depression (Hawkins and Green, 1993) but has a restricted distribution in the southern Galilee Basin (Bradshaw et al., 2009). It has a maximum recorded thickness of around 750 m and was recognised as a distinct seismic facies (G2) by Van Heeswijck (2010).
Aramac Coal Measures (Early Permian): Dominated by sandstone with coal and mudstone interbeds. They only occur in the northern Galilee Basin and its extent was defined by drill intersections and seismic surveys. The distribution of the Aramac Coal Measures is restricted to the Aramac Trough, small depressions in the Galilee Basin around the margin of Maneroo Platform, and the Lovelle Depression. It is a lateral equivalent to the Upper Jochmus Formation. Although the Aramac Coal Measures have been significantly truncated by erosion, it can still be up to 250 m thick.
A significant unconformity occurs between the Early and Late Permian sequences. This was a period of non-deposition and erosion.
Weston beds (Permian): An informal stratigraphic unit consisting of sandstone that is unconformably bounded between the Aramac Coal Measures and Betts Creek beds. It is restricted to the Lovelle Depression.
Betts Creek beds (Late Permian): Interbedded siltstone, mudstone, coal, and sandstone deposited in fluvial and coastal plain environments (Bradshaw et al., 2009). The Betts Creek beds outcrop along the north-east margin of Galilee Basin and also occur in the Koburra Trough, Lovelle Depression and west of Maneroo Platform (Hawkins and Green, 1993). It was recognised as a distinct seismic facies (G3) by Van Heeswijck (2010).
The Betts Creek beds have been correlated with sedimentary rocks in the Bowen Basin. From oldest to youngest, these are the Colinlea Sandstone, Peawaddy Formation, Black Alley Shale and Bandanna Formation. These rock units have also been identified in southern Galilee Basin. Further information on their distribution can be found in Section 184.108.40.206.
Allen and Fielding (2007) identified six transgressive-regressive stratigraphic sequences within the Betts Creek beds, and correlated them with sequences in the Bowen Basin. Sequence 6 in the Betts Creek beds is thought to correlate with the Bandanna Formation. Allen and Fielding (2007) considered the Betts Creek beds to have been deposited at a time when there was little accommodation space available for sediment deposition within the Galilee Basin, suggesting minimal tectonic influence on its depositional architecture.
Colinlea Sandstone (Late Permian): medium to coarse-grained sandstone with interbedded siltstone mudstone and coals deposited in fluvial to lacustrine environments.
Peawaddy Formation and Black Alley Shale (Late Permian): the Peawaddy Formation is predominantly sandstone with minor siltstone, mudstone and coal deposited in marginal marine to deltaic environments (Hawkins and Green, 1993). The Black Alley Shale consists of dark grey to black shale and siltstone, interbedded with light green-grey tuff and fine-grained sandstone.
The Peabody Formation and Black Alley Shale thin onto the Barcaldine Ridge and are largely restricted in distribution to the southern Galilee Basin (Wells, 1989).
Bandanna Formation (Late Permian): interbedded sandstone, siltstone, mudstone and coal deposited in paludal, fluvial and lacustrine environments. Only the Black Alley Shale and Bandanna Formation have been identified in the Powell Depression (Hawkins and Green, 1993).
This figure has been optimised for printing on A3 paper (297 mm x 420 mm).
Rewan Group and Dunda beds (Early Triassic): consists of interbedded light grey sandstone and grey-green mudstone (Hawkins and Green, 1993). It was recognised as a distinct seismic facies (G4) by Van Heeswijck (2006).The Dunda beds are a predominantly sandy facies that is conformable with upper sections of the Rewan Group. The Dunda Beds outcrop along the north-eastern margin of the Galilee Basin and occur in the vicinity of the Koburra Trough.
Clematis Group (Early – Middle Triassic): unconformably overlies the Rewan Group and consists predominantly of sandstone with minor siltstone, mudstone and conglomerate deposited in braided fluvial environments. This is an equivalent of the Warang Sandstone.
Warang Sandstone (Early – Middle Triassic): Up to 700 m thick quartz-rich sandstone with interbedded siltstone and mudstone. It is a basin margin facies prevalent across much of the far northern Galilee Basin and parts of the Lovelle Depression (Hawkins and Green, 1993; Scott et al., 1995). The Warang Sandstone is coeval with the Rewan Group, Clematis Group and the lower Moolayember Formation. The upper Moolayember Formation conformably overlies the Warang Sandstone.
Moolayember Formation (Middle Triassic): consists mostly of siltstone and mudstone deposited in lacustrine and fluvial environments. It conformably overlies the Clematis Group and blankets much of the Galilee Basin and Maneroo Platform (Hawkins and Green, 1993) and is the uppermost stratigraphic unit of the Galilee Basin sequence.
The Eromanga Basin constitutes most of the sedimentary cover over the Galilee Basin (Figure 14 to Figure 16). A significant unconformity, representing approximately a 65 million year period of non-deposition, separates rocks of the Galilee and Eromanga basins. This section only focuses on major stratigraphic groups of the Eromanga Basin. Further detail can be found in Ransley et al. (2012). In the Galilee subregion, the Eromanga Basin sequence is at its thickest in the Powell and Lovelle depressions (up to 1800 m), which suggests that these Galilee Basin depositional centres were actively subsiding during deposition of the Jurassic and Cretaceous Eromanga sequences (Wells, 1989). In contrast, subsidence had ceased in the Koburra Trough as the Eromanga Basin sedimentary rocks do not thicken above it.
From oldest to youngest the Eromanga Basin sequences include:
Ronlow beds (Middle Jurassic – Early Cretaceous): quartzose sandstone with minor siltstone, mudstone and coal deposited in fluvial to floodplain environments. It overlies parts of the northern Galilee Basin and outcrops along the eastern margin of the Eromanga Basin as far south as Barcaldine.
‘Ronlow beds’ is an informal stratigraphic name (Geoscience Australia, 2012), but the rocks are an equivalent of the Hutton Sandstone-Hooray Sandstone-Cadna-owie Formation, which occur in other parts of the Galilee subregion. Several depositional hiatuses are present in the Late Jurassic to Early Cretaceous section of the Ronlow beds (Cook et al., 2013).
Hutton Sandstone, Hooray Sandstone Cadna-owie Formation: (Middle Jurassic – Early Cretaceous): The Hutton Sandstone consists mainly of quartzose sandstone with minor siltstone and mudstone interbeds deposited in braided fluvial environments (Draper, 2002). The Birkhead Formation, Westbourne Formation and the Adori Sandstone, conformably overlie the Hutton Sandstone.
The Birkhead Formation consists of interbedded sandstone and siltstone with minor shale. The Adori Sandstone is mostly sandstone with minor siltstone, and the Westbourne Formation is dominated by siltstone and shale. The Birkhead Formation was deposited in fluvial and lacustrine settings, whereas braided fluvial systems dominated during deposition of the Adori Sandstone. The Westbourne Formation was predominantly deposited in a lacustrine setting (Draper, 2002).
The Hooray Sandstone is predominantly quartzose sandstone deposited in a braided fluvial environment. This unit transitions into the Cadna-owie Formation, which consists of fine-grained sandstone with siltstone and silty mudstone beds. The Cadna-owie Formation was deposited in a shallow marine environment and is conformably overlain by the Rolling Downs Group.
Rolling Downs Group (Early Cretaceous to base of Late Cretaceous). The Rolling Downs Group includes the Wallumbilla and Toolebuc formations, Allaru Mudstone, and the Mackunda and Winton Formations. The bulk of Eromanga outcrop in the Galilee subregion is assigned to the Rolling Downs Group.
The Wallumbilla Formation to Allaru Mudstone sequence consists predominantly of shale and mudstone with minor impure limestone and volcanic-lithic sandstone. These units were deposited in shallow to deep marine environments and represent a significant marine transgressive phase across the Eromanga Basin.
The Mackunda Formation consists of interbedded volcanolithic feldspathic sandstone, siltstone, and mudstone with minor limestone. It was deposited in shallow marine to marginal marine environments during the final regression in the Eromanga Basin.
The Winton Formation consists of interbedded volcanolithic feldspathic sandstone, siltstone, mudstone and coal. Deposition of the Winton Formation marks the return to terrestrial environments following the earlier marine transgression. The lower sections were deposited in a series of estuarine, deltaic and fluvial environments, whereas the upper sections were deposited in fluvial to lacustrine environments (McKellar and Draper, 2013). The Winton Formation contains a significant assemblage of dinosaur fossils including the famous Winton dinosaur tracks.
In the Galilee subregion, significant erosion and intense weathering occurred during the Late Cretaceous to Early Palaeogene (Early Cenozoic). This resulted in the formation of the Morney weathering profile, which consists of up to 95 m of kaolinised deeply weathered sediments capped by 5 m of silcrete. Sedimentation recommenced in the Late Paleocene with the main stratigraphic units being:
Glendower Formation (Late Paleocene – Middle Eocene): comprises up to 70 m of quartz sandstone, pebble conglomerate, sandy conglomerate and subordinate siltstone and mudstone with a well-developed upper silcrete. It occurs as an irregular elongate valley-fill tract that extends across the Galilee subregion from near Hughenden to south-west of Longreach. From Longreach it develops into a sheet-like deposit that covers much of south-western Queensland, as well as the south-western Galilee subregion. The Glendower Formation has been variously correlated with (Grimes, 1980; Draper, 2002), or included in (Senior, 1979) the Eyre Formation (Callen et al., 1995), which is a widespread (commonly lignitic) fluvial deposit in the geological Lake Eyre Basin of South Australia.
Old Cork beds (Late Paleocene): the sub-circular Old Cork Basin occurs west of the Cork fault over the Lovelle Depression of the Galilee Basin and contains generally flat-lying sediments with extensive silicification and ferruginisation of the upper part of the sequence. The basal Old Cork beds comprise up to 78 m of freshwater (lacustrine deposited) limestone and mudstone with subordinate silty sandstone, calcareous sandstone and sandy siltstone (Cook, 2013).
Mueller Sandstone (Eocene) and Werite beds: comprises up to 9 m of coarse-grained fluvial-deposited pebbly sandstone and pebbly conglomerate, which unconformably overlies the Old Cork beds in the Old Cork Basin (Cook, 2013).
Similar Paleogene continental lacustrine, paludal and fluvial sediments occur in the Springvale Basin at the north-western margin of the Galilee subregion. It outcrops as the Werite beds at the eastern margin of the Lovelle Depression (Cook, 2013).
Whitula Formation (Miocene): comprises up to 160 m of interbedded fluvial and lacustrine conglomerate, quartzose sandstone, siltstone and mudstone which is partially gypsiferous and lignitic. It unconformably overlies Cretaceous rocks and the Paleocene Glendower Formation. Similar sediments are recognised in the Springvale Basin (Horse Creek Formation) at the north-western margin of the Galilee subregion.
Sturgeon Basalt (Pliocene - Pleistocene): overlies the Glendower Formation near Hughenden (Cook, 2013). The Sturgeon Basalt is a part of the Sturgeon basalt province. Geomorphic evidence suggests that Sturgeon basalt province was formed by at least three major episodes of volcanism, each volcanic episode was separated by a period of erosion (Cohen et al., 2013).
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- 1.1.1 Bioregion
- 1.1.2 Geography
- 1.1.3 Geology
- 1.1.4 Hydrogeology and groundwater quality
- 1.1.5 Surface water hydrology and water quality
- 1.1.6 Surface water – groundwater interactions
- 1.1.7 Ecology
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