Combining seismically derived temperature with heat flow and bathymetry to constrain the thermal structure of oceanic lithosphere

Goutorbe, Bruno

doi:10.1016/j.epsl.2010.04.013

Cited by 26 publications

(47 citation statements)

References 68 publications

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“…This observation confirms with an up‐to‐date global dataset a result suggested by most previous surface wave studies of lithospheric cooling [e.g., Forsyth , 1977; Zhang and Tanimoto , 1991; Zhang and Lay , 1999; Maggi et al , 2006a]. However, for ages larger than 100 Myrs, some flattening of the isotherms may be seen as predicted by models where a constant heat flux is provided at depth [ Doin and Fleitout , 1996; Goutorbe , 2010]. …”

Section: Tomographic Inversionmentioning

confidence: 99%

A global shear velocity model of the upper mantle from fundamental and higher Rayleigh mode measurements

2012

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[1] We present DR2012, a global SV-wave tomographic model of the upper mantle. We use an extension of the automated waveform inversion approach of Debayle (1999) which improves our mapping of the transition zone with extraction of fundamental and higher-mode information. The new approach is fully automated and has been successfully used to match approximately 375,000 Rayleigh waveforms. For each seismogram, we obtain a path average shear velocity and quality factor model, and a set of fundamental and higher-mode dispersion and attenuation curves. We incorporate the resulting set of path average shear velocity models into a tomographic inversion. In the uppermost 200 km of the mantle, SV wave heterogeneities correlate with surface tectonics. The high velocity signature of cratons is slightly shallower (≈200 km) than in other seismic models. Thicker continental roots are not required by our data, but can be produced by imposing a priori a smoother model in the vertical direction. Regions deeper than 200 km show no velocity contrasts larger than AE1% at large scale, except for high velocity slabs within the transition zone. Comparisons with other seismic models show that current surface wave datasets allow to build consistent models up to degrees 40 in the upper 200 km of the mantle. The agreement is poorer in the transition zone and confined to low harmonic degrees (≤10).Citation: Debayle, E., and Y. Ricard (2012), A global shear velocity model of the upper mantle from fundamental and higher Rayleigh mode measurements,

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Section: Tomographic Inversionmentioning

confidence: 99%

A global shear velocity model of the upper mantle from fundamental and higher Rayleigh mode measurements

2012

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“…Since the 1980s, many researchers have paid increasing attention to the thermal structure of the lithosphere, which made it a new growth point of geodynamics (e.g. Čermák and Bodri 1986;Chen 1988;Pasquale, 1990;Baumann and Rybach 1991;Wang 1996;Rudnick et al 1998;Zang et al 2002;Cooper et al 2004;Gong et al 2005;Liu et al 2005a;Green 2006;Mall and Sharma 2009;Goutorbe 2010). Based on the heat conduction principle, the composition of surface heat flow (including crustal and mantle heat flow), the thermal structure of the lithosphere, and the temperature at depth can be calculated.…”

Section: Methodsmentioning

confidence: 99%

Meso–Cenozoic thermal regime in the Bohai Bay Basin, eastern North China Craton

Qiu

Wei

Zuo

et al. 2015

International Geology Review

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This article discusses the Meso-Cenozoic thermal history, thermal lithospheric thinning, and thermal structure of the lithosphere of the Bohai Bay Basin, North China. The present-day thermal regime of the basin features an average heat flow of 64.5 ± 8.1 mW m -2 , a lithospheric thickness of 76-102 km, and a 'hot mantle but cold crust'-type lithospheric thermal structure. The Meso-Cenozoic thermal history experienced two heat flow peaks in the late Early Cretaceous and in the middle to late Palaeogene, with heat flow values of 82-86 mW m -2 and 81-88 mW m -2 , respectively. Corresponding to these peaks, the thermal lithosphere experienced two thinning stages during the Cretaceous and Palaeogene, reaching a minimum thickness of 43-61 km. The lithospheric thermal structure transformed from the 'hot crust but cold mantle' type in the Triassic-Jurassic to the 'cold crust but hot mantle' type in the Cretaceous-Cenozoic, according to the ratio of mantle to surface heat flow (q m /q s ). The research on the thermal history and lithospheric thermal structure of sedimentary basins can effectively reveal the thermal regime at depth in the sedimentary basins and provide significance for the study of the basin dynamics during the Meso-Cenozoic.

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“…Equation (36) has been used in models of oceanic lithosphere subsidence, for example, equation (1) of Colin and Fleitout [67]. Their intent was to simply represent the increase in the vigor of convection as the rheological boundary layer thickens.…”

Section: The Transient Heat Flow Equation (17) Then Becomes In Normalmentioning

confidence: 99%

“…Its existence or nonexistence of an asymptote has been widely argued since the works of Davis and Lister [5] and Parsons and Sclater [7]; Stein and Stein [27] and Zhong et al [31] review the discussions and provide additional references. Goutorbe [36] presented a combined inversion of bathymetric, seismic, and heat flow data which support a CHABLIS plate model. My conclusions are closest to those of Korenaga and Korenaga [35].…”

Section: Classes Of Data On Seafloor Subsidencementioning

confidence: 99%

Small-scale convection beneath oceans and continents

Sleep

2011

Chin. Sci. Bull.

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Small-scale convection supplies heat flow of ~17 mW m 2 to the base of stable continents where xenolith studies resolve the geotherm. However, effects of small-scale convection are difficult to resolve in ocean basins. On first pass, most seafloor appears to subside to an asymptote compatible with ~40 mW m 2 convective heat flow. These common regions are tracked by hotspots so uplift associated with ponded mantle material is an attractive alternative. Unaffected seafloor in the North and South Atlantic continues to subside with the square root of age as expected from pure conduction. The theory of stagnant-lid convection provides good scaling relationships for heat flow. For linear viscosity, heat flow is proportional to the underlying "half-space" viscosity to the 1/3 power and the temperature to change viscosity by a factor of e to the 4/3 power. The formalism is easily modified to represent convection beneath a lid of highly viscous and buoyant cratonal lithosphere and to represent transient convection beneath thickening oceanic lithosphere. Asthenospheric mantle with linear, strongly temperature-dependent, and weakly depth-dependent viscosity is compatible with both oceanic and continental data. More complicated rheology may allow vigorous small-scale convection under most but not all old ocean basins. Still viable hypotheses require poorly understood global features, including lateral variations of asthenospheric temperature. Seismological studies have the potential to resolve the lithosphere-asthenosphere boundary, including local variations of its depth associated with small-scale convection.lithosphere, asthenosphere, ocean depth-age, small-scale convection, craton, mantle plume Citation:Sleep N H. Small-scale convection beneath oceans and continents.

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Combining seismically derived temperature with heat flow and bathymetry to constrain the thermal structure of oceanic lithosphere

Cited by 26 publications

References 68 publications

A global shear velocity model of the upper mantle from fundamental and higher Rayleigh mode measurements

A global shear velocity model of the upper mantle from fundamental and higher Rayleigh mode measurements

Meso–Cenozoic thermal regime in the Bohai Bay Basin, eastern North China Craton

Small-scale convection beneath oceans and continents

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