Grainsize-sensitive viscoelastic relaxation in olivine: Towards a robust laboratory-based model for seismological application

Jackson, Ian; Faul, U.

doi:10.1016/j.pepi.2010.09.005

Cited by 316 publications

(613 citation statements)

References 26 publications

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“…The anelastic properties of the mantle are based 123 on experiments on Fo90 olivine conducted by Jackson and Faul (2010). To account for the fact that 124…”

Section: Mantle 121mentioning

confidence: 99%

Seismological implications of a lithospheric low seismic velocity zone in Mars

Zheng

Nimmo

Lay

2015

Physics of the Earth and Planetary Interiors

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“…The anelastic properties of the mantle are based 123 on experiments on Fo90 olivine conducted by Jackson and Faul (2010). To account for the fact that 124…”

Section: Mantle 121mentioning

confidence: 99%

Seismological implications of a lithospheric low seismic velocity zone in Mars

Zheng

Nimmo

Lay

2015

Physics of the Earth and Planetary Interiors

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“…Note that the sensitivity spreads out in depth with longer periods. Global map outlining the locations of the major cratons and platforms used to segregate the surface wave dataset using the GTR1 regionalization scheme of Jordan (1981). Dark blue outlines 5ºx5º cratons and cyan/light blue outlines the Phanerozoic platforms.…”

Section: List Ofmentioning

confidence: 99%

“…Note that with a smaller surface heat flow, the lithosphere thickness increases. Xenolith data: black "x" -South Africa; black circle -Slave craton; black diamond -Tanzania; black "+" -Colorado Plateau; black square -Siberia; Example shear velocity profiles generated using the parameterization of Jackson and Faul (2010). The profiles were generated from a single geotherm profile, which was calculated using the variable set Low ( (Table 7).…”

Section: List Ofmentioning

confidence: 99%

“…While the majority of the cratons formed during the Archean, Proterozoic cratons are believed to have been formed on the perimeters of existing cratons (Lee et al, 2010)]. These Proterzoic cratons are called "platforms" since the craton is not exposed at the surface but instead resides below a thick continental sedimentary package (Jordan, 1981). No recent cratons or platforms have formed since the Proterozoic (Lee et al, 2010) implying that the thermal and/or tectonic conditions that allowed cratons to form in the past do not exist today.…”

Section: Cratonsmentioning

confidence: 99%

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Constraints on shear velocity in the cratonic upper mantle from Rayleigh wave phase velocity

Hirsch

Dalton

Ritsema

2015

Geochem Geophys Geosyst

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The standard model of the thermal and chemical structure of cratons has been scrutinized in recent years as additional data have been collected. Recent seismological and petrological studies indicate that the notion of cratonic lithosphere as a thick thermal boundary layer with a very depleted and dehydrated composition may be overly simplified and does not explain all aspects of the seismological and petrological observations. We designed a simple forward-modeling experiment to identify a suite of one-dimensional shear-velocity profiles that are representative of the cratonic upper mantle. The mean and standard deviation of phase velocities for Rayleigh waves that travel paths primarily over cratons were calculated from a global data set in the period range 40 to 300 seconds. One-dimensional Earth models were calculated using two approaches, and the predicted Rayleigh wave phase velocity for each model was compared to the observed range to identify models that provide a satisfactory fit to the observations. With the first approach, shear velocity was predicted from cratonic geotherms that were calculated for a range of surface heat-flow and crustal-thickness values. With the second approach, profiles of shear velocity were generated using random perturbations to 1-D global Earth model STW105. In total 26250 geothermv generated and 80,000 randomly generated 1-D Earth models were generated for comparison to the observations. The results show that cratonic shear velocity is higher than STW105 to depths greater than 200 km. The majority of randomly generated models contain increasing velocity with depth to 250-300 km while the majority of geotherm-generated models contain a low velocity layer in the depth range 100-150 km.vi

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“…These variations are calculated from the Jackson and Faul [2010] extended Burgers representation of olivine anelasticity. This model is thought to account for grain boundary sliding and has good laboratory control but requires extrapolating pressure and grain size effects.…”

Section: Density and Temperature Modelingmentioning

confidence: 99%

A rootless rockies—Support and lithospheric structure of the Colorado Rocky Mountains inferred from CREST and TA seismic data

Hansen

Dueker

Stachnik

et al. 2013

Geochem Geophys Geosyst

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[1] Support for the Colorado high topography is resolved using seismic data from the Colorado Rocky Mountain (CRM) Experiment and Seismic Transects. The average crustal thickness, derived from P wave receiver function imaging, is 48 km. However, a negative correlation between Moho depth and elevation is observed, which negates Airy-Heiskanen isostasy. Shallow Moho (<45 km depth) is found beneath some of the highest elevations, and therefore, the CRM are rootless. Deep Moho (45-51 km) regions indicate structure inherited from the Proterozoic assembly of the continent. Shear wave velocities from surface wave tomography are mapped to density employing empirical velocity-to-density relations in the crust and mantle temperature modeling. Predicted elastic plate flexure and gravity fields derived from the density model agree with observed long-wavelength topography and Bouguer gravity. Therefore, lowdensity crust and mantle are sufficient to support much of the CRM topography. Centers of Oligocene volcanism, e.g., the San Juan Mountains, display reduced crustal thicknesses and lowest average crustal velocities, suggesting that magmatic modification strongly influenced modern lithospheric structure and topography. Mantle velocities span 4.02-4.64 km/s at 73-123 km depth, and peak lateral temperature variations of 600 C are inferred. S wave receiver function imaging suggests that the lithosphereasthenosphere boundary is 100-150 km deep beneath the Colorado Plateau, and 150-200 km deep beneath the High Plains. A region of negative arrivals beneath the CRM above 100 km depth correlates with low mantle velocities and is interpreted as thermally modified/metasomatized lithosphere resulting from Cenozoic volcanism.

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Grainsize-sensitive viscoelastic relaxation in olivine: Towards a robust laboratory-based model for seismological application

Cited by 316 publications

References 26 publications

Seismological implications of a lithospheric low seismic velocity zone in Mars

Seismological implications of a lithospheric low seismic velocity zone in Mars

Constraints on shear velocity in the cratonic upper mantle from Rayleigh wave phase velocity

A rootless rockies—Support and lithospheric structure of the Colorado Rocky Mountains inferred from CREST and TA seismic data

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