Grain-size-sensitive seismic wave attenuation in polycrystalline olivine

By I. Jackson, J. Gerald, U. Faul, B. H. Tan. 2002

408 citations recorded by the source corpus.

View Paper: https://www.semanticscholar.org/paper/b831e5536f3e46cd8488197d896cc29d291f55a8

How researchers see this paper

The researchers whose trusted networks rank it highest, strongest advocate first. Every researcher gets a different order.

In Geophysics

Citations in the corpus

Integrated geophysical‐petrological modeling of the lithosphere and sublithospheric upper mantle: Methodology and applications (2008, background): “…and Vso(T,P) are the unrelaxed high frequency wave velocities at a given temperature and pressure, and Q 1s ¼ A Tod 1 exp E þ VP RT a ð11Þ with A = 750 s amma, a = 0.26, E = 424 kJ mol 1, V = 1.2 1.4 10 5m3 mol 1, and R the universal gas constant [Jackson et al., 2002; Faul and Jackson, 2005].”
The thermal structure of the lithosphere from shear wave velocities (2006, methodology): “[16] used their melt-free experiments to estimate a value of E of 390–400 kJ mol, which is in good agreement with the value from geophysical observations.”
Joint inversion of seismic and gravity data for lunar composition and thermal state (2007, result): “…given by v (P, T, ω) = v (P, T, ω → ∞) [ 1 − 1 2Q cot ( απ 2 )] (14) indicating that dispersion in this limit depends on pressure, temperature and frequency through their effect on the attenuation Q. Typical values of α are around 0.2–0.3, consistent with experimental results (Jackson et al. 2002).”
Shear wave attenuation and dispersion in melt-bearing olivine polycrystals: 1. Specimen fabrication (2004, methodology): “The Andrade-pseudoperiod approach being advocated here has the advantage over the previously used power law dependence of Q 1 on pseudoperiod [Jackson et al., 2002] of coping with the progressive transition from essentially anelastic to viscous behavior encountered at sufficiently high T, small grai”
Polycrystal anelasticity at near‐solidus temperatures (2016, background): “Therefore, it is important to understand rock anelasticity for a quantitative interpretation of seismic velocity and attenuation structures [e.g., Karato, 1993; Jackson et al., 2002; Priestley and McKenzie, 2013; Abers et al., 2014].”
Influence of phase transformations on lateral heterogeneity and dynamics in Earth's mantle (2007, background): “…TðzÞ 1 TRðzÞ ð6Þ where Q00(z) is the radial part of the seismological quality model QR19 (Romanowicz, 1995), T is the temperature, TR is the temperature along the 1600 K adiabat, and values of the activation energy E⁎=424 kJ mol−1 K−1 and frequency exponent, α=0.26, are from Jackson et al. (2002).”
3‐D multiobservable probabilistic inversion for the compositional and thermal structure of the lithosphere and upper mantle. I: a priori petrological information and geophysical observables (2013, background): “Anelasticity in mantle rocks, and the associated attenuation of seismic waves, become important at temperatures >900ıC [e.g., Jackson et al., 2002; Jackson and Faul, 2010] .”
Mineralogy and elasticity of the oceanic upper mantle: Origin of the low‐velocity zone (2005, background): “While the effect of temperature and frequency on the attenuation have been measured experimentally [Jackson et al., 2002], the effect of pressure, partial melt, and water are unquantified in the seismic band, although speculative models have been proposed for the latter [Karato and Jung, B03204…”
On the origin of the asthenosphere (2012, background): “The best-documentedmechanismof anelastic relaxation is grain-boundary sliding accommodated by diffusionalmass transport (Cooper, 2002; Jackson, 2009; Jackson et al., 2002).”
Rheology of the Earth's mantle: A historical review (2010, methodology): “Experimental studies to characterize anelasticity were obtained and applied to explain the structure of the low-velocity and high-attenuation zone (Faul and Jackson, 2005; Jackson et al., 1992, 2002).”
Implications of grain size evolution on the seismic structure of the oceanic upper mantle (2008, methodology): “47 Laboratory data show that in addition to the well-known temperature-dependence of shear-wave 48 speed (VS) and attenuation (Q) (Minster & Anderson, 1981), VS and Q are also sensitive to grain 49 size (Tan et al., 2001; Cooper, 2002; Jackson et al., 2002).”