Initiation of brittle faults in the upper crust: a review of field observations

Crider, Juliet G.; Peacock, David

doi:10.1016/j.jsg.2003.07.007

Cited by 196 publications

(78 citation statements)

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“…However, typical fault thickness-displacement scaling relationships indicate that the Pataxós fault and Jucurutu fault (the faults for which we have good constraints on fault core thickness) probably accommodated hundreds of metres to kilometres of displacement (e.g. Childs et al 2009).…”

Section: Regional Context: Cariri-potiguar Rift Trendmentioning

confidence: 95%

Scale-dependent influence of pre-existing basement shear zones on rift faulting: a case study from NE Brazil

Kirkpatrick

Bezerra

Shipton

et al. 2013

JGS

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This version is available at https://strathprints.strath.ac.uk/43272/ Strathprints is designed to allow users to access the research output of the University of Strathclyde. Unless otherwise explicitly stated on the manuscript, Copyright © and Moral Rights for the papers on this site are retained by the individual authors and/or other copyright owners. Please check the manuscript for details of any other licences that may have been applied. You may not engage in further distribution of the material for any profitmaking activities or any commercial gain. You may freely distribute both the url (https://strathprints.strath.ac.uk/) and the content of this paper for research or private study, educational, or not-for-profit purposes without prior permission or charge.Any correspondence concerning this service should be sent to the Strathprints administrator: strathprints@strath.ac.ukThe Strathprints institutional repository (https://strathprints.strath.ac.uk) is a digital archive of University of Strathclyde research outputs. It has been developed to disseminate open access research outputs, expose data about those outputs, and enable the management and persistent access to Strathclyde's intellectual output.Journal of the Geological Society, London, Vol. 170, 2013, pp. 237 -247. doi: 10.1144 Rifting in intra-continental areas will commonly interact with a framework of pre-existing deformed zones. Although new structures form, structural inheritance may influence the location and geometry of tectonic deformation because strained rocks can act as weak zones localizing subsequent deformation (e.g. Watterson 1975;Sykes 1978;Handy 1989;Holdsworth et al. 2001). In particular, basins along rift margins are often inferred to be influenced by pre-existing structures (e.g. Daly et al. 1989;Lee & Hwang 1993;van Wees & Beekman 2000;Scheck-Wenderoth & Lamarche 2005). The connection between basins and pre-existing structures is frequently based on the similarity of the trends of seismically imaged rift faults to basement tectonic trends observed onshore (e.g. Roberts & Holdsworth 1999;Wilson et al. 2006). However, assessing the direct relationship between rift faults and pre-existing structures is often difficult because the basement is overlain by syn-to post-rift formations. The effect of pre-existing structures on fault architecture at scales of tens to hundreds of metres is less clear. Some studies suggest that pre-existing foliations resulting from crystal-plastic deformation exert a strong influence on fault zone architecture during later deformation (e.g. Beacom et al. 2001;Butler et al. 2008). Experimental work indicates that foliated rocks are mechanically anisotropic (Donath 1964;Shea & Kronenberg 1993), suggesting that foliations impart mechanical anisotropy or planes of weakness into the country rock that may be exploited by subsequent fracturing. However, analogues for the deeper sections of rift faults are rarely exposed, and the specific impacts of mechanical anisotropy for fault structures at exposure scale are con...

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Section: Regional Context: Cariri-potiguar Rift Trendmentioning

confidence: 95%

Scale-dependent influence of pre-existing basement shear zones on rift faulting: a case study from NE Brazil

Kirkpatrick

Bezerra

Shipton

et al. 2013

JGS

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“…For details of the tectonic and sedimentary history of Kilve, see Peacock and 97 Sanderson (Peacock and Sanderson, 1991, 1992. The throws on faults F1 and F2 98 decrease laterally and terminate within pre-existing veins (Crider and Peacock, 2004). The 99 magnitude of continuous deformation (reverse drag or fault propagation folding) around 100 these faults is negligible, and the tips can be located with a high degree of accuracy from 101 (throw) displacement vs. distance plots (Fig.…”

Section: Outcrop Scale Examples -Kilve 95mentioning

confidence: 99%

Geological controls on fault relay zone scaling

Long

Imber

2011

Journal of Structural Geology

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The full-text may be used and/or reproduced, and given to third parties in any format or medium, without prior permission or charge, for personal research or study, educational, or not-for-prot purposes provided that:• a full bibliographic reference is made to the original source • a link is made to the metadata record in DRO • the full-text is not changed in any way The full-text must not be sold in any format or medium without the formal permission of the copyright holders.Please consult the full DRO policy for further details. suggests that the primary control on relay aspect ratio (overlap/separation) is a scale-12 invariant process, such as the stress interaction between the overlapping fault tips as 13 suggested by previous authors. Within the compiled global dataset host rock lithology does 14 not appear to be a first-order control. Much of the observed scatter can be attributed to the 15 spread of measurements recorded from individual relay zones, which relates to the evolving 16 three-dimensional geometry of the relay zone as displacements on the bounding faults 17 increase. Relay ramps exposed at two localities where the faults cut layered sedimentary 18 sequences display mean aspect ratios of 8.20 and 8.64 respectively, more than twice the 19 global mean (4.2). Such high aspect ratios can be attributed to the relay-bounding faults 20 having initially been confined within competent layers, facilitating the development of large 21 overlap lengths. The presence of pre-existing structures (veins) at fault tips may also 22 enhance fault propagation, giving rise to increased overlap lengths. 23 Keywords: 24Relay zone scaling; mechanical stratigraphy; fault interaction; aspect ratio; and stress field. 25 26 27

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“…4). Differences along strike are caused by lateral coalescence of several segments (see also Needham et al, 1996;Marchal et al, 2003), whereas differences towards depth might be caused by vertical coalescence of several segments (Mansfield and Cartwright, 2001;Marchal et al, 2003), or by lithological inhomogeneities (Crider and Peacock, 2004), or a combination of both.…”

Section: Fault Corrugations and Displacement Calculationsmentioning

confidence: 99%