Creep, compaction and the weak rheology of major faults

Sleep, Norman H.; Blanpied, Michael L.

doi:10.1038/359687a0

Cited by 409 publications

(271 citation statements)

References 38 publications

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“…In a final set of models, we modify this initial condition to evaluate the effects of lateral fluid flow driven away from a highly pressurized fault zone, as might be expected from transient pressurization during slip [e.g., Andrews, 2002;Hirose and Bystricky, 2007] or from interseismic localization of pressure within the fault [e.g., Rice, 1992;Sleep and Blanpied, 1992;Fulton and Saffer, 2009b]. In these simulations, pore pressures within the fault zone and country rock are lithostatic and hydrostatic, respectively.…”

Section: Modeling Results: Thermal Effects Of Transient Fluid Flowmentioning

confidence: 99%

Does hydrologic circulation mask frictional heat on faults after large earthquakes?

et al. 2010

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[1] Knowledge of frictional resistance along faults is important for understanding the mechanics of earthquakes and faulting. The clearest in situ measure of fault friction potentially comes from temperature measurements in boreholes crossing fault zones within a few years of rupture. However, large temperature signals from frictional heating on faults have not been observed. Unambiguously interpreting the coseismic frictional resistance from small thermal perturbations observed in borehole temperature profiles requires assessing the impact of other potentially confounding thermal processes. We address several issues associated with quantifying the temperature signal of frictional heating including transient fluid flow associated with the earthquake, thermal disturbance caused by borehole drilling, and heterogeneous thermal physical rock properties. Transient fluid flow is investigated using a two-dimensional coupled fluid flow and heat transport model to evaluate the temperature field following an earthquake. Simulations for a range of realistic permeability, frictional heating, and pore pressure scenarios show that high permeabilities (>10 −14 m 2 ) are necessary for significant advection within the several years after an earthquake and suggest that transient fluid flow is unlikely to mask frictional heat anomalies. We illustrate how disturbances from circulating fluids during drilling diffuse quickly leaving a robust signature of frictional heating. Finally, we discuss the utility of repeated borehole temperature profiles for discriminating between different interpretations of thermal perturbations. Our results suggest that temperature anomalies from even low friction should be detectable at depths >1 km 1 to 2 years after a large earthquake and that interpretations of low friction from existing data are likely robust.Citation: Fulton, P. M., R. N. Harris, D. M. Saffer, and E. E. Brodsky (2010), Does hydrologic circulation mask frictional heat on faults after large earthquakes?,

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Section: Modeling Results: Thermal Effects Of Transient Fluid Flowmentioning

confidence: 99%

Does hydrologic circulation mask frictional heat on faults after large earthquakes?

et al. 2010

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“…Recent models of fault evolution propose a cyclic nature of earthquake faulting processes where faults act as seals during seismic quiescence and as conduit during earthquakes (e.g. Sibson, 1992;Rice, 1992;Sleep and Blanpied, 1992;Caine et al, 1996;Miller et al, 1996;Miller, 2002). The basic assumption is that pore pressure increases within the fault zone during tectonic loading and decreases during faulting.…”

Section: Discussionmentioning

confidence: 99%

“…Therefore, characterization of the internal structure of exhumed fault zones is important for understanding their mechanical, hydraulic and seismic behaviour (Conti et al, 2001;Faulkner et al, 2003;Wibberley and Shimamoto, 2003). In particular, the analysis of deformation mechanisms and healing processes (cementation and compaction) provide information about temporal and spatial changes in the strength of faults (Sleep and Blanpied, 1992;Schulz and Evans, 1998;Janssen et al, 1998;Muchez and Sintubin, 1998;Lin et al, 2001;Sausse et al, 2001). …”

Section: Fault Architecture and Fault Zone Charactermentioning

confidence: 99%

Different styles of faulting deformation along the Dead Sea Transform and possible consequences for the recurrence of major earthquakes

Janssen¹,

Hoffmann‐Rothe²,

Bohnhoff³

et al. 2007

Journal of Geodynamics

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We compare fault-related deformation of three segments of the major transform plate boundary between Africa and the Arabian plate, the Dead Sea Transform (DST), namely: the Arava/Araba fault (Jordan/Israel), the Serghaya fault and the Ghab fault (both Syria). These segments show both similarities and marked differences in faulting deformation and fluid-rock interactions. In the case of the Arava fault, fault damage occurs across a zone up to 300 m wide. A fault core/gouge zone is not exhibited.Along the Serghaya fault, the typical fault zone architecture with a main gouge zone and a damage zone of up to 100 m thickness is exposed. Effects of faulting in the Ghab segment are shown by subsidiary faults and the formation of fault breccias. As in the Arava fault segment, a fault core is not exposed. were active along Serghaya fault and Ghab fault, where fault rock cementation led to * Corresponding author. Fax: +49-331-288-1328, E-mail address: jans@gfz-potsdam.de 2 porosity reduction and lower permeability. Such low permeability could create domains of higher pore fluid pressure, which reduce the effective shear stress required for slip on the fault. These differences in fluid-rock interactions may have played an important role with respect to the occurrence of earthquakes. We suggest that the recurrence interval on a fault segment that recovers after an earthquake without fluid assisted healing (e.g. Arava fault) should be longer than on segments with strong fluidassisted healing (cementation; e.g. Serghaya fault, Ghab fault), given that the regional stress field is the same.

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“…IPS is also recognized as one of the main factors controlling the geological evolution of porosity and permeability, and hence capacity and productivity, of (potential) hydrocarbon reservoirs (Pittman, 1979;Hutcheon‚ 1983;Carrozzi and Von Bergen‚ 1987), as well as a possible mechanism controlling fault creep, fault gouge compaction and fault strength recovery (Rutter and Mainprice, 1978;Angevine et al, 1982;Lehner and Bataille, 1984;Sleep and Blanpied, 1992;Sleep, 1995). In addition, Urai et al (1986) and Spiers et al (1989Spiers et al ( , 1990 have shown that IPS can be an important deformation mechanism in halite rock at low strain rates, which has important implications for the design of waste repositories in rock salt formations, and for understanding salt tectonics.…”

Section: Introductionmentioning

confidence: 99%

Intergranular Pressure Solution in Nacl: Grain-To-Grain Contact Experiments under the Optical Microscope

Spiers

Schutjens

1999

Oil & Gas Science and Technology - Rev. IFP

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Résumé -Dissolution sous contrainte dans NaCl : expériences de contact grain à grain sous microscope optique -La dissolution sous contrainte (IPS -Intergranular Pressure Solution) représente un mécanisme de lithification, de compaction et de déformation à l'échelle géologique pour une large gamme de roches. Les études expérimentales d'IPS réalisées sur des agrégats de quartz n'ont pas été couronnées de succès en raison d'un taux faible d'IPS, et les expériences IPS réalisées en utilisant une halite saturée comme analogue de roche Hickman et Evans, 1991) ont laissé des incertitudes quant au détail des mécanismes IPS et à la structure/saturation au contact du grain dans ce matériau. La présente étude fait état de quatre expériences de dissolution de contact réalisées sous microscope optique afin d'étudier le mécanisme et la cinétique de l'IPS pour des contacts simples halite/halite et halite/verre, chargés en eau salée (température ambiante). Des forces normales de contact dans la gamme de 1,0 à 2,6 N ont été appliquées en présence d'eau salée saturée en NaCl, induisant des pressions de 0,8 à 7,4 MPa. Des pertes de masse et des convergences -fonction du temps -ont été observées pour tous les contacts. Dans tous les cas, le fait de charger le contact (ou d'augmenter la charge sur le contact) a conduit à la formation immédiate d'une morphologie de contact rugueuse, composée d'un motif d'îles et de canaux, contrôlé par des caractéristiques cristallographiques, à l'échelle de quelques microns. Cette microstructure non équilibrée a évolué dans le temps vers une face de contact optiquement plate. Le processus de convergence/lissage doit donc avoir compris une diffusion de masse en dehors du contact et une expulsion de la saumure par l'intermédiaire d'une phase d'eau salée connectée, à l'intérieur du contact. Le fait qu'une structure rugueuse à petite échelle ait persisté dans des contacts ayant évolué vers un aspect optiquement plat n'est pas établi, bien que les observations au microscope à balayage élec-tronique faites après l'essai le suggèrent. Si ce phénomène était confirmé, son amplitude serait inférieure à 500 nm. Les mesures des taux de dissolution ont permis une comparaison avec un modèle pour l'IPS. Les analyses suggèrent que la diffusion en solution, à travers le contact, contrôlait certainement le taux. La structure du contact et la diffusivité varient alors avec la force de contact et la convergence. Les résul-tats sont largement en adéquation avec ceux des expériences précédentes sur la compaction, réalisées en utilisant de la poudre d'halite saturée. Les divergences avec les résultats d'autres chercheurs, issus d'expériences de dissolution sur des contacts simples, peuvent être expliquées en termes de différence de configuration d'expérience et de concurrence entre les forces motrices.Mots-clés : dissolution sous pression, contact de grain, diffusion, dissolution de l'halite. Science and Technology -Rev. IFP, Vol. 54 (1999) Oil & Gas

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Creep, compaction and the weak rheology of major faults

Cited by 409 publications

References 38 publications

Does hydrologic circulation mask frictional heat on faults after large earthquakes?

Does hydrologic circulation mask frictional heat on faults after large earthquakes?

Different styles of faulting deformation along the Dead Sea Transform and possible consequences for the recurrence of major earthquakes

Intergranular Pressure Solution in Nacl: Grain-To-Grain Contact Experiments under the Optical Microscope

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