On the transient behavior of frictional melt during seismic slip

Nielsen, S. B.; Mosca, Pietro; Giberti, Gustavo C.; Toro, Giulio Di; Hirose, Takehiro; Shimamoto, Toshihiko

doi:10.1029/2009jb007020

Cited by 60 publications

(85 citation statements)

References 60 publications

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“…The thickness of the layer w where temperature rises may be between 0.1 and 10 cm based on field observations [John et al, 2009]. Thick black lines show the expected temperature of fusion for dry peridotite and H 2 O-bearing peridotite [Nielsen et al, 2010;Till et al, 2012] assuming host rock temperature of 600°C. Based on our results, for a 3 cm thick layer, frictional melting may readily occur for M5+ earthquakes with slips of 75 cm and 35 cm for dry and wet peridotite, respectively.…”

Section: Discussionmentioning

confidence: 99%

“…where Q represents energy that is converted to heat, A is the rupture area, m the mass of peridotite to be melted, ρ the density, w the fault thickness, and C the heat capacity that we assume is 1 J/g°C [Andersen and Austrheim, 2006;Nielsen et al, 2010]. Note that in equations (3a) and (3b) only the fracture energy G is used to estimate the temperature rise (frictional heat is calculated by assuming E H = 0).…”

Section: Energy Budget and Temperature Rise For Intermediate-depth Eamentioning

confidence: 99%

“…Given the low thermal diffusivity of rocks (~1.5 mm 2 /s), thicknesses are not expected to be much larger for second-long rupture durations observed here. A temperature of 1400-1800°C is required to melt peridotite and gabbroic rocks [Nielsen et al, 2010;Del Gaudio et al, 2009], thus depending on the temperature of the slab a ΔT of between 600-1000°C is needed for melting to occur. Our data (see Figure 4) suggests that for a 1 cm thick layer, frictional melting may occur for 0.4 m of slip, corresponding to M w 4.7.…”

Section: Energy Budget and Temperature Rise For Intermediate-depth Eamentioning

confidence: 99%

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Seismic evidence for thermal runaway during intermediate‐depth earthquake rupture

Prieto

Florez

Barrett

et al. 2013

Geophysical Research Letters

109

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[1] Intermediate-depth earthquakes occur at depths where temperatures and pressures exceed those at which brittle failure is expected. There are two leading candidates for the physical mechanism behind these earthquakes: dehydration embrittlement and self-localizing thermal shear runaway. A complete energy budget for a range of earthquake sizes can help constrain whether either of these mechanisms might play a role in intermediate-depth earthquake rupture. The combination of high stress drop and low radiation efficiency that we observe for M w 4-5 earthquakes in the Bucaramanga Nest implies a temperature increase of 600-1000°C for a centimeter-scale layer during earthquake failure. This suggests that substantial shear heating, and possibly partial melting, occurs during intermediate-depth earthquake failure. Our observations support thermal shear runaway as the mechanism for intermediate-depth earthquakes, which would help explain differences in their behavior compared to shallow earthquakes. Citation: Prieto, G. A., M. Florez, S. A. Barrett, and G. C. Beroza (2013), Seismic evidence for thermal runaway during intermediate-depth earthquake rupture, Geophys. Res. Lett., 40,[6064][6065][6066][6067][6068]

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Section: Discussionmentioning

confidence: 99%

Section: Energy Budget and Temperature Rise For Intermediate-depth Eamentioning

confidence: 99%

Section: Energy Budget and Temperature Rise For Intermediate-depth Eamentioning

confidence: 99%

See 1 more Smart Citation

Seismic evidence for thermal runaway during intermediate‐depth earthquake rupture

Prieto

Florez

Barrett

et al. 2013

Geophysical Research Letters

109

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“…Such knowledge has been established only recently, because the technical implementation of high-velocity, seismic-like conditions in laboratory experiments was achieved no earlier than the 1980s with the pioneering work of Shimamoto & Tsutsumi [55] and became widespread in the last decade (see [8,33,[56][57][58][59][60][61][62][63][64][65][66][67][68][69][70][71][72] among others). It is notable that such high-velocity weakening has been documented even on rocks which show rate-strengthening in traditional, slow frictional tests.…”

Section: Challenging Observations (A) Dissipation: Is It Only Friction?mentioning

confidence: 99%

From slow to fast faulting: recent challenges in earthquake fault mechanics

Nielsen

2017

Phil. Trans. R. Soc. A.

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Faults—thin zones of highly localized shear deformation in the Earth—accommodate strain on a momentous range of dimensions (millimetres to hundreds of kilometres for major plate boundaries) and of time intervals (from fractions of seconds during earthquake slip, to years of slow, aseismic slip and millions of years of intermittent activity). Traditionally, brittle faults have been distinguished from shear zones which deform by crystal plasticity (e.g. mylonites). However such brittle/plastic distinction becomes blurred when considering (i) deep earthquakes that happen under conditions of pressure and temperature where minerals are clearly in the plastic deformation regime (a clue for seismologists over several decades) and (ii) the extreme dynamic stress drop occurring during seismic slip acceleration on faults, requiring efficient weakening mechanisms. High strain rates (more than 10 4 s −1 ) are accommodated within paper-thin layers (principal slip zone), where co-seismic frictional heating triggers non-brittle weakening mechanisms. In addition, (iii) pervasive off-fault damage is observed, introducing energy sinks which are not accounted for by traditional frictional models. These observations challenge our traditional understanding of friction (rate-and-state laws), anelastic deformation (creep and flow of crystalline materials) and the scientific consensus on fault operation. This article is part of the themed issue ‘Faulting, friction and weakening: from slow to fast motion’.

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“…For sufficiently large combinations of slip speeds and effective normal stress, thermal power generated during solid-on-solid slip overwhelms the ability of thermal conduction to carry the frictional heat away from the slip interface and macroscopic melting may occur (Di Toro et al, 2006Hirose and Shimamoto, 2005;Liou et al, 2004;Nielsen et al, 2010;Niemeijer et al, 2011;Okada et al, 2001;Okada et al, 2002;Spray, 2005;Tsutsumi and Shimamoto, 1997). Since molten layers have a low viscosity, they may lead to hydrodynamic lubrication of faults reducing dynamic friction.…”

Section: Introductionmentioning

confidence: 99%

Laboratory observations of transient frictional slip in rock–analog materials at co-seismic slip rates and rapid changes in normal stress

Yuan

Prakash

2012

Tectonophysics

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Keywords:Rock-analog materials Co-seismic slip rates Rate weakening and strengthening Flash heating Rapid change in normal stress Plate-impact pressure-shear friction experiments Knowledge of frictional (shear) resistance and its dependency on slip distance, slip velocity, normal stress, and surface roughness is fundamental information for understanding earthquake physics and the energy released during such events. In view of this, in the present study, plate-impact pressure-shear friction experiments are conducted to investigate the frictional resistance in a rock analog material, i.e. soda-lime glass, under interfacial conditions of relevance to fault rupture. The results of the experiments indicate that a wide range of frictional slip conditions exist at the slip interface ranging from initial no-slip and followed by slip weakening, slip strengthening (healing), and seizure all during a single slip event. The slip-weakening phase is understood to be most likely due to thermal-induced flash heating and incipient melting at asperity junctions, while the slip strengthening (slip-healing) phase is understood to be a result of coalescence and solidification of local melt patches on the slip interface. In addition, plate impact pressure-shear normal-stress change (drop) experiments are employed to probe the response of the slip interface due to sudden alterations in normal stress. In particular, the location (timing) of the stress drop is varied so as to investigate the behavior of the slip interface in its slip-weakening, slip-strengthening (healing) phase, or the seized phase, in response to sudden drop in normal stress. These experimental results provide a rich set of data to better understand the range of possible friction slip states that can be achieved and/or critically examine existing dynamic friction models for fault slip behavior.

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On the transient behavior of frictional melt during seismic slip

Cited by 60 publications

References 60 publications

Seismic evidence for thermal runaway during intermediate‐depth earthquake rupture

Seismic evidence for thermal runaway during intermediate‐depth earthquake rupture

From slow to fast faulting: recent challenges in earthquake fault mechanics

Laboratory observations of transient frictional slip in rock–analog materials at co-seismic slip rates and rapid changes in normal stress

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