The Sydney Basin bioregion covers the central, western and southern portions of the geological Sydney Basin (simply referred to henceforth throughout this section as the Sydney Basin) (Figure 23). The Hunter subregion of the Northern Sydney Basin bioregion (see Section 1.1.3 of companion product 1.1 for the Hunter subregion ) abuts the Sydney Basin bioregion to the north, and corresponds to the northern part of the Sydney Basin. The Sydney Basin bioregion covers the full extent of the Southern and Central coalfields of the Sydney Basin, as well as most of the Western Coalfield (Figure 23). While the southernmost extents of the Hunter and Newcastle coalfields also intersect the Sydney Basin bioregion (Figure 23), resource prospects are considered limited in this part of the bioregion and they are not discussed in detail here. The Central Coalfield, which historically has been mined (e.g. Sydney Harbour Colliery at Balmain between 1897 and 1931; ), is also not discussed in detail here as there is currently no future planned coal resource development. Consequently, Southern and Western coalfields are the main focus of this section, with rock and stratigraphy descriptions for the Hunter and Newcastle coalfields presented in product 1.1 for the Hunter subregion (not discussed in this product). As can be seen in Figure 24, the surface geology of the Sydney Basin bioregion is dominantly Permian to Triassic, with some older rocks and younger Cenozoic alluvium.
The Sydney Basin contains rocks of Late Carboniferous to Middle Triassic age . These rocks are a mixed assemblage of marine and non-marine sedimentary rocks, predominantly siliclastics and coals. The maximum thickness of the basin’s entire sedimentary sequence varies between 4.5 and 6 km. The Sydney Basin initially formed as a rift basin, and subsequently experienced thermal subsidence and foreland basin development stages . The basin spans approximately 20% of the NSW coastline, covering approximately 400 km from just south of Durras in the south to just north of Newcastle (Cadman et al., 1998, p. 141; Ward and Kelly, 2013). The basin occurs both onshore and offshore (see Figure 23; ), with approximately 36,000 km2 onshore and 28,000 km2 offshore . The Sydney Basin forms part of a much greater late Paleozoic to early Mesozoic sedimentary basin complex known as the Sydney-Gunnedah-Bowen Basin (SGBB) (Figure 23, Figure 25).
This so-called ‘super basin’ spans from central Queensland in the north to the NSW central coast, with the Sydney Basin forming the southernmost portion (Figure 25; Brakel, 1991, p. 10; Cadman et al., 1998, p. 141; Haworth, 2003; Ward and Kelly, 2013; Geoscience Australia, 2015a). Throughout much of its development, the SGBB formed in a back-arc tectonic setting, adjacent to a subduction zone . identified three dominant phases of basin development: early Permian extension, thermal subsidence in the middle Permian and later foreland loading during the late Permian, which continued into the Middle Triassic.
(a) Location of the geological Sydney Basin on the coast of eastern Australia and (b) the five coalfields of the onshore geological Sydney Basin
To the north of the Sydney Basin the Gunnedah Basin sits on the north-western side of the Liverpool Range where recognisable differences in basin stratigraphy have been defined (Brakel, 1991, p. 10; Stewart and Alder, 1995; Cadman et al., 1998, p. 143). Earlier work on the Sydney and Gunnedah basins had placed this basin divide further to the south-east at the Mount Coricudgy Anticline where basin strata are thinner (Brakel, 1991, p. 10; Tadros 1993; Cadman et al., 1998, p. 141). The Sydney Basin extends easterly to the continental shelf (Brakel, 1991, p. 10; Haworth, 2003), and to the north the basin terminates at the Hunter-Mooki Thrust Fault (Brakel, 1991, p. 10). To the west, much of the basin has been eroded, and now terminates where it abuts the older rocks of the Lachlan Fold Belt (Brakel, 1991, p. 11).
The older (prior to late Permian) sedimentary rocks of the Sydney Basin were originally deposited due to glacially influenced marine sedimentation, with some volcanic influence and minor terrestrial deposition (Brakel, 1991, p. 14; Ward and Kelly, 2013). These terrestrial units are more common in the north of the Sydney Basin and are generally considered coal-bearing . Younger sediments (late Permian and younger) are dominantly terrestrial and more coal-rich and are considered to be of greatest economic importance in the Sydney Basin . There are notable differences in rock types across the basin and, as such, stratigraphic divisions are made separately for the five coalfields. Sedimentation in the Late Carboniferous and early Permian formed the oldest preserved units, and probably continued without significant disruption into the Jurassic, although subsequent widespread erosion has removed all traces of strata from the Middle Triassic to the Jurassic – hence the existence of these rocks is speculative . Early Permian marine transgression over much of the basin was followed by a late Permian regression; with the lower Permian marine sequences overlain by widespread coal-bearing units (Brakel, 1991, pp. 14–21). The main exception to this occurred in the northern-most portion of the basin where a middle Permian regression locally formed the Greta Coal Measures (Brakel, 1991, pp. 14–21). The lower Permian strata thicken to the north of the basin whereas the late Permian and Triassic strata thin northwards . All strata thin over the western margin of the basin where the basement rock is topographically higher, Figure 26.
The Sydney Basin is divided into several major structural zones, including a series of north to north-east trending ridges and troughs in the north-east of the basin (Figure 27). The central Sydney Basin, commonly referred to as the Inner Sydney or Cumberland Basin (Bembrick et al., 1973; Jones and Clark, 1991; Haworth, 2003; Branagan, 2009; Bray et al., 2010) is a structural low, reflected in the topography, surrounded by a series of elevated plateaux (Figure 27; Haworth, 2003). This particular sub-basin is largely urbanised and is described as the lowest lying structural feature of the Sydney Basin . The surrounding topographic highs (including the Woronora, Blue Mountains and Hornsby plateaux) form structural barriers that isolate the central basin .
The Cranky Corner, Gloucester and Myall basins sit outside the northern boundary of the Sydney Basin, but have at times been referred to as detached pockets of remnant Sydney Basin (Korsch et al., 2009; Ward and Kelly, 2013; Brakel, 1991, p. 10). refers to the Myall Basin (also referred to as Myall Syncline) as an outlier of the Sydney Basin. The Cranky Corner and Gloucester basins are currently recognised as separate basins containing stratigraphy of a similar age to the Sydney Basin. The hydrogeological Botany Basin is also of note due to its importance to hydrology (Griffin, 1963, p. 6) though it has had limited use throughout geological literature. In terms of location, the Botany Basin sits to the immediate south of the City of Sydney, encompassing part of Sydney itself and the suburbs of Marrickville, Botany, Randwick, Rockdale and Sutherland Shire (Griffin, 1963, p. 8) and extends into Botany Bay. The basin is approximately 8 x 8 km at its maximum width and length. The geology of the Botany Basin is that of a trough feature, largely filled with Triassic aged deposition (Douglas Partners, 2007, p. 5).
The Lapstone Monocline, Kurrajong Fault, Lochinvar Anticline, Kulnura Anticline and Lake Macquarie Syncline form the dominant north-trending basin structures . These structures are the result of either tectonic movement during the Permian and Triassic or the reactivation of older basement structures (Stewart and Alder, 1995; Belvin et al., 2007; Ward and Kelly, 2013). In the southern part of the Sydney Basin there are also some synclines, anticlines and faults that trend north-westerly . The Blue Mountains Shelf and the Illawarra Shelf are separated from the rest of the basin by a series of faults and monoclines thought to represent a possible older basement structural feature (Harrington and Brakel, 1981, p. 10; Brakel, 1991, pp. 11–12). The remaining Sydney Basin can be thought of as a series of troughs and ridges (Brakel, 1991, p. 11). During the Permian, when coals were being deposited, the Dome Belt (a series of anticlines and dome structures) of the Hunter Valley region is interpreted to have been forming (Brakel, 1991, p. 12).
Source: . Deep 3D structure of the Sydney Basin using gravity modelling, Danis et. al., Australian Journal of Earth Sciences. Copyright © Geological Society of Australia, reprinted by permission of Taylor & Francis Ltd, www.tandfonline.com on behalf of Geological Society of Australia. This figure may not be reproduced without the express permission of Australian Journal of Earth Sciences, http://www.tandfonline.com/toc/taje20/current.
The Southern Coalfield is a large syncline feature at the southernmost end of the Sydney Basin (Hutton, 2009, p. 44). Strata within the coalfield mostly dip between 2 and 5 degrees, although dips of less than 2 degrees also occur (Hutton, 2009, p. 44). Internal to the Southern Coalfield’s synclinal structure, anticlines and synclines are noted, with the two largest forming the Camden Syncline and the Woronora Ridge; the latter of which is technically a series of anticlines and synclines (Hutton, 2009, p. 44). Although internal anticline and syncline structures are recognised, the dominant structural feature within the coalfield consists of a series of north-west to north-east trending faults (Hutton, 2009, p. 44). The north-westerly faults have throws of up to 90 m whereas the north-easterly en-echelon faults have throws of up to 15 m (Hutton, 2009, p. 44). Internal divisions within the Southern Coalfield have been proposed by several authors (Bembrick et al., 1973; Scheibner, 1999) focusing on the magnetic lineaments of the major faults such as the Lapstone Monocline Fault System, the Nepean Fault Zone, the Oakdale Fault System and the Bargo Fault (Hutton, 2009, p. 44). Most faulting in this coalfield is considered to be normal, with strike-slip, reverse and high angle faults (less commonly) documented (Hutton, 2009, p. 44). Jointing and doming related to igneous features also occur (Hutton, 2009, p. 44).
The Western Coalfield is marked by a series of north-trending monoclines that form the dominant structural features of the basin, with some associated faulting (Hutton, 2009, p. 51). The Mount Tomah Monocline is the dominant structural feature of the Western Coalfield and separates the Wollar and Blue Mountains shelves from the Murrurundi Trough and the Macdonald Trough (Yoo et al., 2001, p. 57). The Mount Coricudgy Anticline is a basement growth structure sitting 2 km above the base of the Macdonald Trough (Yoo et al., 2001, p. 57). The other prominent structural feature is the Lapstone Structural Complex, a north-trending monocline and fault system within the Macdonald Trough . The Kurrajong Fault is a major high-angle reverse fault within the coalfield which dips eastwards . Localised small throw faults are evident in some locations (Hutton, 2009, p. 51).
Product Finalisation date
- 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
- Contributors to the Technical Programme
- About this technical product