Deformation mechanisms — recognition from natural tectonites

Knipe, R. J.

doi:10.1016/0191-8141(89)90039-4

Cited by 308 publications

(102 citation statements)

References 115 publications

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“…Cataclasis involves grain fracturing and can reduce the porosity and the 318 permeability as well as increase the capillary threshold pressure of rocks 319 within fault zones (e.g., Antonellini and Aydin, 1994; Antonellini and Aydin, 320 1995; Borg et al, 1960;Engelder, 1974;Knipe, 1989). During the process of 321 cataclasis, the porosity and permeability are reduced because the cataclasis 322 results in the collapse of porosity and the reduction of grain size (Fisher and 323 (Fisher 427 and .…”

Section: Cataclasis 317mentioning

confidence: 99%

A review of fault sealing behaviour and its evaluation in siliciclastic rocks

Pei

Paton

Knipe³

et al. 2015

Earth-Science Reviews

110

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8Faults can be either conduits or retarders for fluid flow. As the presence of 9 faults increases the risks for hydrocarbon exploration, the sealing behaviour 10 of a fault zone has been a focus for geological studies in the past 30 years. 11Due to the widespread occurrence of fault zones, either in extensional or 12 contractional regimes, knowledge about the fault sealing behaviour is of 13 great importance to a wide spectrum of disciplines in geosciences, for 14 instance, structural geology, geochemistry, petroleum geology, etc. 15Geologists have extensively study the sealing properties of a fault zone over 16 the last decades, ranging from fault zone architecture, fault seal types, fault 17 seal processes, fault rock classification, research methods and controlling 18 factors.

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Section: Cataclasis 317mentioning

confidence: 99%

A review of fault sealing behaviour and its evaluation in siliciclastic rocks

Pei

Paton

Knipe³

et al. 2015

Earth-Science Reviews

110

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“…The deformation mechanisms likely to be active at different conditions within a fault zone, which may lead to seismic or aseismic deformation, are outlined, and the geological and physical parameters likely to control their prevalence discussed. The mechanisms by which rocks were deformed can be inferred from their textures (Knipe 1989); these relationships for the typical fault rocks encountered in exhumed fault zones are reviewed in this introduction. A conceptual fault-zone model building on previous review works (e.g.…”

mentioning

confidence: 99%

Geology of the earthquake source: an introduction

Fagereng

Toy

2011

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Earthquakes arise from frictional 'stick-slip' instabilities as elastic strain is released by shear failure, almost always on a pre-existing fault. How the faulted rock responds to applied shear stress depends on its composition, environmental conditions (such as temperature and pressure), fluid presence and strain rate. These geological and physical variables determine the shear strength and frictional stability of a fault, and the dominant mineral deformation mechanism. To differing degrees, these effects ultimately control the partitioning between seismic and aseismic deformation, and are recorded by fault-rock textures. The scale-invariance of earthquake slip allows for extrapolation of geological and geophysical observations of earthquake-related deformation. Here we emphasize that the seismological character of a fault is highly dependent on fault geology, and that the high frequency of earthquakes observed by geophysical monitoring demands consideration of seismic slip as a major mechanism of finite fault displacement in the geological record.

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“…The general importance of phase boundaries as preferred sites of dissolution during dissolution-precipitation creep is evident from many natural rocks (e.g. Groshong, 1988;Knipe, 1989;Tada and Siever, 1989;Schwarz andStöck-hert, 1996, 2002;Trepmann and Stöckhert, 2009;Trepmann et al, 2010;Wassmann et al, 2011). In polyphase rocks undergoing dissolution-precipitation creep, monomineralic inclusions can deform by crystal-plastic processes as observed for folded quartz veins indicating dislocation creep within metagreywacke deformed by dissolution-precipitation creep (Trepmann and Stöckhert, 2009).…”

Section: Deformation Processes and Conditions Recorded By The Mylonitmentioning

confidence: 99%

The microstructural record of porphyroclasts and matrix of partly serpentinized peridotite mylonites – from brittle and crystal-plastic deformation to dissolution–precipitation creep

Bial

Trepmann

2013

Solid Earth

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Abstract. We present microfabrics in high-pressure, metamorphic, partly serpentinized peridotite mylonites from the Voltri Massif, in which porphyroclasts and matrix record independent deformation events. The microfabrics are analysed using polarization microscopy and electron microscopy (SEM/EBSD, EMP). The mylonites contain diopside and olivine porphyroclasts originating from the mantle protolith embedded in a fine-grained matrix consisting mainly of antigorite and minor olivine and pyroxene. The porphyroclasts record brittle and crystal-plastic deformation of the peridotite at upper-mantle conditions and differential stresses of a few hundred MPa. After the peridotites became serpentinized, deformation occurred mainly by dissolutionprecipitation creep resulting in a pronounced foliation of the antigorite matrix, crenulation cleavages and newly precipitated olivine and pyroxene from the pore fluid at sites of dilation, i.e. in strain shadows next to porphyroclasts and folded fine-grained antigorite layers. Antigorite reveals a pronounced associated shape preferred orientation (SPO) and crystallographic preferred orientation (CPO) with the basal (001) cleavage plane oriented in the foliation plane. In monomineralic antigorite aggregates at sites of stress concentration around porphyroclasts, a characteristically reduced grain size and deflecting CPO as well as sutured grain boundaries indicate also some contribution of crystal-plastic deformation and grain-boundary migration of antigorite. In contrast, the absence of any intragranular deformation features in newly precipitated olivine in strain shadows reveals that stresses were not sufficiently high to allow for significant dislocation creep of olivine at conditions at which antigorite is stable. The porphyroclast microstructures are not associated with the microstructures of the mylonitic matrix, but are inherited from an independent earlier deformation. The porphyroclasts record a high-stress deformation of the peridotite with dislocation creep of olivine in the upper mantle probably related to rifting processes, whereas the serpentinite matrix records dominantly dissolution-precipitation creep and low stresses during subduction and exhumation.

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Deformation mechanisms — recognition from natural tectonites

Cited by 308 publications

References 115 publications

A review of fault sealing behaviour and its evaluation in siliciclastic rocks

A review of fault sealing behaviour and its evaluation in siliciclastic rocks

Geology of the earthquake source: an introduction

The microstructural record of porphyroclasts and matrix of partly serpentinized peridotite mylonites – from brittle and crystal-plastic deformation to dissolution–precipitation creep

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