Friction in faulted rock at high temperature and pressure

Stesky, Robert; Brace, W. F.; Riley, Dominic

doi:10.1016/0148-9062(74)90508-7

Cited by 60 publications

(78 citation statements)

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“…Subsequent studies have investigated the effects of humidity [Dieterich and Conrad, 1984;Frye and Marone, 2002], rock type, normal stress [Dieterich, 1972], shear stress [Karner and Marone, 2001], and loading rate [Kato et al, 1992] on frictional healing. The effect of temperature was also explored [Stesky et al, 1974;Blanpied, 1995;Karner et al, 1997;Nakatani, 2001], but with the exception of Nakatani [2001], experimental constraints on the temperature dependence of frictional healing are rather limited. Recent findings from high-speed frictional experiments suggest that dramatic variations in the coefficient of friction at slip rates greater than 0.1 m/s may be thermally activated [Tsutsumi and Shimamoto, 1997;Di Toro et al, 2011;Brown and Fialko, 2012].…”

Section: Introductionmentioning

confidence: 99%

Temperature dependence of frictional healing of Westerly granite: Experimental observations and numerical simulations

Mitchell

Fialko

Brown

2013

Geochem Geophys Geosyst

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[1] Temperature is believed to have an important control on frictional properties of rocks, yet the amount of experimental observations of time-dependent rock friction at high temperatures is rather limited. In this study, we investigated frictional healing of Westerly granite in a series of slide-hold-slide experiments using a direct shear apparatus at ambient temperatures between 20 C and 550 C. We observed that at room temperature coefficient of friction increases in proportion to the logarithm of hold time at a rate consistent with findings of previous studies. For a given hold time, the coefficient of friction linearly increases with temperature, but temperature has little effect on the rate of change in static friction with hold time. We used a numerical model to investigate whether time-dependent increases in real contact area between rough surfaces could account for the observed frictional healing. The model incorporates fractal geometry and temperature-dependent viscoelasoplastic rheology. We explored several candidate rheologies that have been proposed for steady state creep of rocks at high stresses and temperatures. None of the tested laws could provide an agreement between the observed and modeled healing behavior given material properties reported in the bulk creep experiments. An acceptable fit to the experimental data could be achieved with modified parameters. In particular, for the power-law rheology to provide a reasonable fit to the data, the stress exponent needs to be greater than 40. Alternative mechanisms include time-dependent gouge compaction and increases in bond strength between contacting asperities.

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Section: Introductionmentioning

confidence: 99%

Temperature dependence of frictional healing of Westerly granite: Experimental observations and numerical simulations

Mitchell

Fialko

Brown

2013

Geochem Geophys Geosyst

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“…For this reason, data for Westerly granite are selected here to evaluate quantitative effects of the normal stress and temperature on failure strength in the brittle-plastic transition regime. Of the published data for Westerly granite, the data by Griggs et al [1960], Stesky et al [1974] and Wong [1982a,b] alone are used for the present analysis, because these data include a complete set of the parameters: compressive failure strength S (S --ot -%, where c•t and c• 3 are the maximum and minimum principal stresses at failure, respectively, and compressive stress is taken as positive), confining pressure P (P --c•3), temperature T, failure angle 0, and strain rate •. The failure angle is defined here as the angle between the c•-axis and the macroscopic fracture surfaces or alternatively the macroscopic shear zone at a high temperature.…”

Section: Data Used For the Present Analysismentioning

confidence: 99%

“…With these observations in mind, the operative mechanism for the temperature effect g(T) for Westerly granite above 500øC may be ascribed to quartz plasticity (as well as biotite plasticity), since it has been reported that feldspar minerals do not deform plastically at the experimental conditions employed [e.g., Stesky et al, 1974;Stesky, 1978]. The micromechanism for quartz plasticity was not identified [e.g., Griggs et al, 1960;Stesky, 1978].…”

Section: Experimental Studies By Stesky Et Al [1974] and Steskymentioning

confidence: 99%

A shear failure strength law of rock in the brittle‐plastic transition regime

Ohnaka

1995

Geophysical Research Letters

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As a first step to establish the law governing shear failure of typical crustal materials in the brittle‐plastic transition regime under lithospheric conditions, and thereby to properly estimate a depth profile of lithospheric strength in quantitative terms, the effects of the normal stress σn across the fault surfaces and ambient temperature T on the shear failure strength of dry Westerly granite in the brittle to brittle‐plastic transition regimes are evaluated quantitatively, using experimental data published by earlier authors. The empirical law proposed can predict the shear failure strength at strain rates of 10−4‐10−5/S under any (σn, T) conditions in the brittle to brittle‐plastic transition regimes.

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“…The brittle fracture, which is one of the main deformation mechanisms in the lithosphere, is ignored in the previous study of the rheological structure of the lithosphere for a long time, only the frictional sliding and creep were taken into account. Experiments show that the stress causing the brittle fracture of an intact rock will be less than that causing frictional sliding on fractures at some temperatures, pressures and strain rates [1,2] . When the angle between the partial cutting (fractures) and the main compressive stress is greater than a given value, the rock will produce new brittle fractures, other than frictional sliding along the cutting [3] .…”

Section: Introductionmentioning

confidence: 99%

“…(1) has some disadvantages: (1) The temperature effect is deduced from a small number of data. (2) The effect of the strain rate is not taken into account. (3) It only provides the fracture parameter for E-mail: wrq1973@gmail.com granite and gabbro.…”

Section: Introductionmentioning

confidence: 99%

Effects of Temperature and Strain Rate on Fracture Strength of Rocks and Their Influence on Rheological Structure of the Lithosphere

Wei¹,

Zang²

2006

Chinese J. Geophys.

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Effects of temperature and strain rate on fracture strength of rocks are studied based on available experiment data, and a new empirical formula for the fracture strength of some typical rocks in the lithosphere is obtained. The effects of the confining pressure, size of rock samples, temperature and strain rate are taken into account in this formula so that it can further reveal the actual fracture states in the lithosphere. Application of the new empirical formula to the Ordos block shows that the conventional rheological model overestimates the rheological strength and misinterpret rheological deformation mechanisms in the lithosphere. The brittle regime in the rheological structure calculated from the new formula can be divided into two sub-regions in which frictional sliding or brittle fracture is dominant, respectively. The magnitude of the rheological strength is decreased and the area of the brittle regime is enlarged when more representative rocks and effect of the strain rate are taken into account.

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Friction in faulted rock at high temperature and pressure

Cited by 60 publications

References 0 publications

Temperature dependence of frictional healing of Westerly granite: Experimental observations and numerical simulations

Temperature dependence of frictional healing of Westerly granite: Experimental observations and numerical simulations

A shear failure strength law of rock in the brittle‐plastic transition regime

Effects of Temperature and Strain Rate on Fracture Strength of Rocks and Their Influence on Rheological Structure of the Lithosphere

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