Neoproterozoic stratigraphy of the Centralian Superbasin, Australia

Walter, Malcolm R.; Veevers, J. J.; Calver, Clive R.; Grey, Kathleen

doi:10.1016/0301-9268(94)00077-5

Cited by 249 publications

(204 citation statements)

References 64 publications

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“…Examples include the late Mesoproterozoic to early Neoproterozoic successions in the North Atlantic , and the Neoproterozoic Centralian Supergroup of Central Australia, which was deformed during the late Neoproterozoic Peterman and Palaeozoic Alice Springs orogenies (Collins & Teyssier 1989;Walter et al 1995;Sandiford & Hand 1998;Hand & Sandiford 1999;Cawood & Korsch 2008). These examples are associated with the transformation of Rodinia into Gondwana, and the deformation and metamorphism of the sedimentary successions overlaps with events at the plate margin edges of these supercontinents (e.g.…”

Section: Classification Of Orogens In Space and Timementioning

confidence: 99%

Accretionary orogens through Earth history

et al. 2009

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Accretionary orogens form at intraoceanic and continental margin convergent plate boundaries. They include the supra-subduction zone forearc, magmatic arc and back-arc components. Accretionary orogens can be grouped into retreating and advancing types, based on their kinematic framework and resulting geological character. Retreating orogens (e.g. modern western Pacific) are undergoing long-term extension in response to the site of subduction of the lower plate retreating with respect to the overriding plate and are characterized by back-arc basins. Advancing orogens (e.g. Andes) develop in an environment in which the overriding plate is advancing towards the downgoing plate, resulting in the development of foreland fold and thrust belts and crustal thickening. Cratonization of accretionary orogens occurs during continuing plate convergence and requires transient coupling across the plate boundary with strain concentrated in zones of mechanical and thermal weakening such as the magmatic arc and back-arc region. Potential driving mechanisms for coupling include accretion of buoyant lithosphere (terrane accretion), flat-slab subduction, and rapid absolute upper plate motion overriding the downgoing plate. Accretionary orogens have been active throughout Earth history, extending back until at least 3.2 Ga, and potentially earlier, and provide an important constraint on the initiation of horizontal motion of lithospheric plates on Earth. They have been responsible for major growth of the continental lithosphere through the addition of juvenile magmatic products but are also major sites of consumption and reworking of continental crust through time, through sediment subduction and subduction erosion. It is probable that the rates of crustal growth and destruction are roughly equal, implying that net growth since the Archaean is effectively zero.Classic models of orogens involve a Wilson cycle of ocean opening and closing with orogenesis related to continent-continent collision. These imply that mountain building occurs at the end of a cycle of ocean opening and closing, and marks the termination of subduction, and that the mountain belt should occupy an internal location within an assembled continent (supercontinent). The modern Alpine -Himalayan chain exemplifies the features of this model, lying between the Eurasian and colliding African and Indian plates (Fig.

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Section: Classification Of Orogens In Space and Timementioning

confidence: 99%

Accretionary orogens through Earth history

et al. 2009

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“…To this end we briefly summarize some salient ideas about these basins. The interested reader can find more comprehensive accounts in Lambeck (1983), Lindsay et al (1987), Korsch and Lindsay (1989), Lindsay and Korsch (1991), Shaw et al (1991), Walter and Gorter (1994), Walter et al (1995) and Q14:1 Sandiford et al (2002). In one of the earliest accounts (Lambeck 1983) the formation of the central Australia basins was attributed to long high amplitude (c.10 km) lithospheric-scale buckling, largely on the basis of the Nielsen & Hansen (2000).…”

Section: Styles Of Inversion In Naturementioning

confidence: 99%

“…However, subsequent workers (e.g., Teyssier 1985) have demonstrated that the gravity pattern largely reflects late structuring of the basin during inversion (Shaw et al 1991;Sandiford 2002) and therefore does not provide an unequivocal constraint on the earlier basin-forming process. Consequently almost all subsequent analyses have emphasized the role of extensional processes in basin formation (e.g., Lindsay et al 1987;Korsch & Lindsay 1989;Shaw et al 1991;Walter & Gorter 1994;Walter et al 1995;Sandiford Q14:1 et al 2002). The current consensus is that the main rifting associated with basininitiation stage occurred at .800 Ma.…”

Section: Styles Of Inversion In Naturementioning

confidence: 99%

Lower crustal rheological expression in inverted basins

Sandiford

Hansen

McLaren

2006

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Although lithospheric modelling has provided extraordinary insights into the processes that shape the continental crust, considerable uncertainty surrounds the basic rheology that governs behaviour at geological timescales. In part, this is because it has proved difficult to identify the geological observations that might discriminate, or unify, models of lithospheric rheology. In particular, the relative strength of lower crust and upper mantle remains a contentious aspect of continental lithospheric rheology. We show that various models for lower crustal rheology may produce distinct patterns of inversion in extensional sedimentary basins, consistent with some of the observed natural variability of inversion styles. Inversion of basin interiors, as is common in European Mesozoic basins, is favoured by a lithospheric rheology more sensitive to lateral thermal structure than to changes in the depth of the Moho, consistent with there being little strength contrast between the lower crust and upper mantle in these settings. In contrast, inversion of basin margins, particularly involving basinward verging structures, is consistent with a rheological sensitivity to the depth of Moho as would apply for a lower crust much weaker than the upper mantle. We use an example from central Australia to demonstrate this later response, together with thermochronologic data that suggests that a relatively weak lower crust in this setting may reflect abnormally high geothermal gradients.

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“…The general absence of facies changes and thickness variations in the sediments adjacent to these boundaries, and the continuity of stratigraphy between basins (e.g. Walter et al 1995), provides a compelling argument for the former continuity of these basins. The formerly more or less continuous basin that is assumed to have covered almost the entire Central Australian region through the Neoproterozoic, prior to its fragmentation into the present series of structural-remnant basins, has been termed the Centralian Superbasin.…”

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confidence: 99%

Tectonic feedback, intraplate orogeny and the geochemical structure of the crust: a central Australian perspective

Sandiford

Hand

McLaren

2001

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The geological record of intraplate deformation in central Australia implies that past tectonic activity (basin formation, deformation and erosion) has modulated the response of the lithosphere during subsequent tectonic activity. In particular, there is a correspondence between the localization of deformation during intraplate orogeny and the presence of thick sedimentary successions in the preserved remnants of a formerly widespread intracratonic basin. This behaviour can be understood as a kind of 'tectonic feedback', effected by the longterm thermal and mechanical consequences of changes in the distribution of heat producing elements induced by earlier tectonism. From a geochemical point of view, one of the most dramatic effects of intraplate orogeny in central Australia has been the exposure, in the cores of the orogens, of deep crustal rocks largely depleted in the heat producing elements. The geochemical structuring of the crust associated with the erosion of the heat-producing upper crust resulted in long-term cooling of the deep crust and upper mantle with associated lithospheric strengthening. This is illustrated here by mapping the consequences of deformation and associated tectonic responses onto the h-q c plane, where h is the characteristic length-scale for heat production distribution, and q c is the total crustal heat production.

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Neoproterozoic stratigraphy of the Centralian Superbasin, Australia

Cited by 249 publications

References 64 publications

Accretionary orogens through Earth history

Accretionary orogens through Earth history

Lower crustal rheological expression in inverted basins

Tectonic feedback, intraplate orogeny and the geochemical structure of the crust: a central Australian perspective

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