Ge277-Experimental Rock Friction implication for seismic faulting Some other references: Byerlee, 1978; Dieterich, 1979; Ruina, 1983; Tse and Rice, 1986;

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Presentation transcript:

Ge277-Experimental Rock Friction implication for seismic faulting Some other references: Byerlee, 1978; Dieterich, 1979; Ruina, 1983; Tse and Rice, 1986; Blanpied et al, 1991; Chester, 1995; Lockner et Beeler, 1999; Cocco and Bizarri, 2002 Review articles by - Scholz (1998): ‘Earthquakes and Friction Laws’ - Chris Marone (1998): ‘ Laboratory derived friction laws and their application to seismic faulting

Earthquakes result from frictional instabilities (Brace and Byerlee, 1966) Whether friction is stable or unstable determines the mode of slip (seismic vs aseismic) The stability of frictional sliding is not a rheological property. It depends of key parameters including –Temperature –Amplitude of stress change – ‘Stiffness’ of the fault (length of the slipping patch) –Effective normal stress

Friction Experiments (Scholz, 1990)

Slip hardening Slip weakening

Friction coefficient is generally of the order of 0.6 for most rock types (Byerlee, 1978) The shear stress at Frictional yield depends linearly on normal stress

Friction behavior for a wide range of materials is shown for step changes in load point velocity (Dieterich & Kilgore 1994). Experimental data show that, whatever the material considered, friction depends on sliding rate and that changes in slip rates are followed by a transient adjustment.

Time dependence of static friction for loading with Vs/r = 1 and 10  /s. The data indicate that static friction and healing vary with loading rate and therefore that static friction is a system response. Lines represent best fit log-linear relations. (Marone, 1998)

DcDc Static friction depends on hold time and dynamic friction decreases with slip rate. These phenomena contribute to an (apparent) slip-weakening friction law.

Previous figure (a) Measurements of the relative variation in static friction with hold time for initially bare rock surfaces (solid symbols) and granular fault gouge (open symbols). The data have been offset to  s = 0.6 at 1 s and thus represent relative changes in static friction. (b) Friction data versus displacement, showing measurements of static friction and s in slide-hold-slide experiments. Hold times are given below. In this case the loading velocity before and after holding Vs/r was 3 m/s (data from Marone 1998). (c) The relative dynamic coefficient of friction is shown versus slip velocity for initially bare rock surfaces (solid symbols) and granular fault gouge (open symbols). The data have been offset to d = 0.6 at 1 m/s. (d) Data showing the transient and steady-state effect on friction (see Figure 2 for identification of friction parameters) of a change in loading velocity for a 3-mm-thick layer of quartz gouge sheared under nominally dry conditions at 25-MPa normal stress (data from J Johnson & C Marone). (Marone, 1998)

Premonitory slip before unstable sliding (Lockner and Beeler, 1999)

Premonitory slip before unstable sliding

Constant stress experiment (creep experiment). In creep experiments three stages are generally observed, primary, secondary and tertiary creep leading to failure. The sample ultimately fails by Static Fatigue following sub-critical crack growth. Rock strength is time dependent. (Lockner, 1998)