2014
DOI: 10.1186/bf03352197
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A note on latent heat release from disequilibrium phase transformations and deep seismogenesis

Abstract: Latent heat release by equilibrium mineralogical transformations in an adiabatically subducting slab reversibly perturbs temperatures and pressures so as to conserve entropy. However, latent heats of metastable transformations in such a slab yield irreversible isobaric temperature changes which increase entropy despite adiabatic constraints. As a result, latent heat release by metastable exothermic transformations can yield local superheating above the background adiabat, with the degree of potential superheat… Show more

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Cited by 16 publications
(14 citation statements)
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References 40 publications
(56 reference statements)
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“…The manifestation of the stress accumulation in terms of surface temperature and SLHF is prominent in the case of shallow focal depth earthquakes. The change in SLHF is likely to be attributed to a dis-equilibrium in the mineralogical phase transformation due to the accumulation of stress (Bina, 1998). This effect is less prominent in the case of shallow-focus earthquakes.…”
Section: Resultsmentioning
confidence: 98%
“…The manifestation of the stress accumulation in terms of surface temperature and SLHF is prominent in the case of shallow focal depth earthquakes. The change in SLHF is likely to be attributed to a dis-equilibrium in the mineralogical phase transformation due to the accumulation of stress (Bina, 1998). This effect is less prominent in the case of shallow-focus earthquakes.…”
Section: Resultsmentioning
confidence: 98%
“…Specifically, density differences driving for instance subduction do not need to be assigned but follow from chemical composition and temperature. Moreover, reversible material property changes at phase transitions can trigger events that may be of interest to the geodynamicists and seismologists [4].…”
Section: Introductionmentioning
confidence: 99%
“…Several large deep‐focus earthquakes in 1994 and 1996 have come as a test of models for the occurrence of deep earthquakes. These models include transformational faulting of olivine to spinel [ Green and Burnley , 1989; Kirby et al , 1992; Green and Houston , 1995; Green and Zhou , 1996]; clinoenstatite to ilmenite [ Akaogi et al , 1987; Hogrefe et al , 1994; Kirby et al , 1996]; serpentinite dehydration [ Meade and Jeanloz , 1991]; plastic instability and shear induced melting [ Griggs and Baker , 1969; McKenzie and Brune , 1972; Ogawa , 1987; Hobbs and Ord , 1988; Lomnitz‐Adler , 1990; Spray , 1993; Kikuchi and Kanamori , 1994; Kanamori et al , 1998; Bina , 1998a]; reactivation of preexisting fault planes [ Silver et al , 1995]; grain‐size reduction causing rheology changes [ Riedel and Karato , 1996, 1997; Karato et al , 2001]; and slab stresses due to an increase in mantle viscosity at 660 km [ Vassiliou et al , 1984; Goto et al , 1987; Vassiliou and Hager , 1988]. Observations show that the largest recent deep event, the 1994 Bolivia earthquake, occurred at the bottom of the subduction zone, that several large earthquakes (1994 Fiji and 1996 Flores Sea, Indonesia [e.g., Tibi et al , 1999]) may have ruptured outside the inner core of the slab as defined by previously located seismicity, and that deep seismicity occurs in areas which may be too warm for olivine to exist metastability.…”
Section: Introductionmentioning
confidence: 99%