Displacements, segment linkage and relay ramps in normal fault zones

Peacock, David; Sanderson, David J.

doi:10.1016/0191-8141(91)90033-f

Cited by 804 publications

(513 citation statements)

References 14 publications

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“…The most common form of such interactions is when sub-parallel faults overlap, such that the interacting tips lie within the stress shadows of the adjacent fault. The displacement profiles in such cases become asymmetric: the peak slip region is shifted towards the interacting tip and the FTT at that end becomes steeper than that of the distal end [Peacock and Sanderson, 1991;Contreras et al, 2000]. This occurs because the FTT at the interacting tip must overcome both the rupture resistance and the stressdrop of the adjacent fault [Willemse, 1997;Scholz, 2002, pp.…”

Section: Methodsmentioning

confidence: 99%

Slip tapers at the tips of faults and earthquake ruptures

Scholz

Lawler

2004

Geophysical Research Letters

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[1] Slip gradients near the tips of earthquake ruptures and faults are typically linear. For non-interacting faults or earthquake ruptures, tip tapers are scale invariant, and about 1 -2 orders of magnitude larger for faults than for earthquakes. For fault tips interacting with other faults, the taper can be as much as a factor of 10 greater than for non-interacting faults. For earthquake ruptures, taper is also greater by as much as a factor of 10 for tips of rupture segments in the interior of the main rupture, tips in which the earthquake has propagated to the end of the fault, and tips which interact with the stress-drop of a previous earthquake on the same fault. Tip taper for faults increases with the strength of the wall rock. These observations are consistent with fracture mechanics models in which inelastic deformation occurs in a volume surrounding the crack tip.

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Section: Methodsmentioning

confidence: 99%

Slip tapers at the tips of faults and earthquake ruptures

Scholz

Lawler

2004

Geophysical Research Letters

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“…Baudon and Cartwright, 2008a;2008b;Cartwright et al, 1995;Dawers and Anders, 1995;Gupta and Scholz, 2000;Peacock and Sanderson, 1991;Young et al, 2001); (ii) throw backstripping that is the product of subtracting values of the shallower horizon from deeper horizons, which shows how fault propagates within the interval between the shallower and deeper horizons (e.g., Dutton and Trudgill, 2009;Morley et al,, 2007); (iii) throw-depth (T-z) profiles, which record fault throw for all interpreted horizons and yield information that can be used to interpret the vertical propagation history of faults (Baudon and Cartwright, 2008a, 2008b, 2008cCartwright et al, 1998;Hongxing and Anderson, 2007); (iv) strike projection of fault throw, which allows the 3D fault growth history to be investigated (Walsh and Watterson, 1991); time-thickness maps, created by calculating the difference in TWT between two horizons to tracks spatial variations in subsidence, are used to determine fault activity during those time intervals.…”

Section: Methodsmentioning

confidence: 99%

Influence of fault reactivation during multiphase rifting: the Oseberg area, Northern North Sea rift

Deng¹,

Fossen²,

Gawthorpe³

et al. 2017

Preprint

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Multiphase rifts tend to produce fault populations that evolve by the formation of new faults and reactivation of earlier faults. The resulting fault patterns tend to be complex and difficult to decipher. In this work we use seismic reflection data to examine the evolution of a normal fault network in the Oseberg Fault Block in the northern North Sea Rift System -a rift system that experienced Permian -Early Triassic and Middle Jurassic -Early Cretaceous rifting and exhibits N-S, NW-SE and NE-SW oriented faults.Both N-S-and NW-SE-striking faults were established during the Permian -Early

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“…Evidence from outcrops and exposures in mines suggest that slip along individual faults is non-uniform and generally increases from 0 at the tips to a maximum somewhere along the fault [Peacock and Sanderson, 1991 The frictional strength of a fault is likely to vary along its length. Fault ends are transition zones from unbroken rock ahead of the fault to well-developed sliding surfaces along the fault (Figure 3a) and frictional strength is believed to decrease within a small region close to the tip.…”

Section: Slip and Frictional Strength Along Faultsmentioning

confidence: 99%

Fracture localization along faults with spatially varying friction

Cooke¹

1997

J. Geophys. Res.

123

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Abstract. Opening-mode splay fractures have been observed within clusters near fault tips. The spatial distribution of splay fractures along faults influences fluid flow and lends insight into the mechanical processes of faulting. Slip gradients along faults produce stress concentrations which promote the development of opening-mode splay fractures along faults. Since the slip distribution depends on the distribution of frictional strength along faults, spatial variations in the frictional properties may influence fracture localization. Variations in friction coefficient along faults can reduce the stress singularities at fault tips and promote the development of multiple fractures inwards from the fault tips. The conditions that promote splay crack localization are examined using analytical and numerical fault models. Single splay fractures develop at locations of abrupt friction coefficient change and/or at fault tips when the friction coefficient near the tips is less than a critical value. Fault models with linearly increasing friction coefficient toward the fault tip promote the development of multiple splay fractures within broad zones near the tip.

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Displacements, segment linkage and relay ramps in normal fault zones

Cited by 804 publications

References 14 publications

Slip tapers at the tips of faults and earthquake ruptures

Slip tapers at the tips of faults and earthquake ruptures

Influence of fault reactivation during multiphase rifting: the Oseberg area, Northern North Sea rift

Fracture localization along faults with spatially varying friction

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