Temperature dependence of thermal transport properties of crystalline rocks — a general law

The crustal section beneath amphibolite Niedźwiedź Massif (Fore-Sudetic Block in NE Bohemian Massif), modelled on the basis of geological and seismic data, is dominated by gneisses with subordinate granites (upper and middle crust) and melagabbros (lower crust). The geotherm was calculated based on the chemical analyses of the heat-producing elements in the rocks forming the crust and the measurements of their density and heat conductivity. The results were verified by heat flow calculations based on temperature measurements from 1,600 m deep well in the Niedźwiedź Massif and by temperaturedepth estimates in mantle xenoliths coming from the nearby ca. 4.5 My basanite plug in Lutynia. The paleoclimate-corrected heat flow in the Niedźwiedź Massif is 69.5 mW m -2 , and the mantle heat flow is 28 mW m -2 . The mantle beneath the Massif was located marginally relative to the areas of intense Cenozoic thermal rejuvenation connected with alkaline volcanism. This results in geotherm which is representative for lithosphere parts located at the margins of zones of continental alkaline volcanism and at its waning stages. The lithosphereasthenosphere boundary (LAB) beneath Niedźwiedź is located between 90 and 100 km depth and supposedly the rheological change at LAB is not related to the appearance of melt.

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“…We believe that the above formula describes well T-p dependence of k in the crust (see also Seipold 1998). …”

Section: An Advanced Thermal Modelmentioning

confidence: 52%

“…Most of the results (e.g. Clauser and Huenges 1995;Seipold 1998;Tommasi et al 2001;Abdulagatov et al 2006;Katsur 2007;Whittington et al 2009) indicate that thermal conductivity and thermal diffusivity stabilize for the p-T range of upper lithospheric mantle (i.e. for: 1-4 GPa, and 700-1,500°C).…”

Section: An Advanced Thermal Modelmentioning

confidence: 99%

Lithosphere thermal structure at the eastern margin of the Bohemian Massif: a case petrological and geophysical study of the Niedźwiedź amphibolite massif (SW Poland)

Puziewicz

Czechowski

Krysiński

et al. 2011

Int J Earth Sci (Geol Rundsch)

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“…Thermal conductivities for granitoids vary between 2.5 and 3.5 W/(m°K) (Seipold, 1998). Thus, present-day geothermal gradients of 32±8°C/km can be estimated for the upper crust (Adriasola et al, 2006); if a higher geothermal gradient was prevalent during the Neogene arc magmatism it would signify even less exhumation.…”

Section: Resultsmentioning

confidence: 99%

Fission track thermochronology of Neogene plutons in the Principal Andean Cordillera of central Chile (33-35°S): Implications for tectonic evolution and porphyry Cu-Mo mineralization

Maksaev

Munizaga

Zentilli

et al. 2009

AndGeo

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AbStRACt. Apatite fission track data for Miocene plutons of the western slope of the Principal Andean Cordillera in central Chile (33-35°S) define a distinct episode of enhanced crustal cooling through the temperature range of the apatite partial annealing zone (~125-60°C) from about 6 to 3 Ma. This cooling episode is compatible with accelerated exhumation of the plutons at the time of Pliocene compressive tectonism, and mass wasting on the western slope of the Principal Andean Cordillera in central Chile. The timing coincides with the southward migration of the subducting Juan Fernández Ridge and the development of progressive subduction flattening northward of 33°S. It also corresponds to the time of active magmatic-hydrothermal processes and rapid unroofing of the world class Río Blanco-Los Bronces and El Teniente porphyry Cu-Mo deposits. Zircon fission track ages coincide with previous 40 Ar/ 39 Ar dates of the intrusions, and with some of the apatite fission track ages, being coherent with igneous-linked, rapid cooling following magmatic intrusion. The thermochronologic data are consistent with a maximum of about 8 km for Neogene exhumation of the plutons.

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“…Other parameters used in the calculations are similar to those used by Grott and Breuer (2008a) and we prescribe an initial upper mantle temperature of 1800 K, an initial core temperature of 2100 K, a crustal thermal conductivity of 3 W m −1 K −1 (Clauser and Huenges, 1995;Seipold, 1998), a mantle thermal conductivity of 4 W m −1 K −1 and a crustal thickness of 50 km (Zuber et al, 2000;Neumann et al, 2004;Wieczorek and Zuber, 2004).…”

Section: Parametersmentioning

confidence: 99%

Implications of large elastic thicknesses for the composition and current thermal state of Mars

Grott

Breuer

2009

Icarus

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To cite this version:M. Grott, D. Breuer. Implications of large elastic thicknesses for the composition and current thermal state of Mars. Icarus, Elsevier, 2009, 201 (2) This is a PDF file of an unedited manuscript that has been accepted for publication. As a service to our customers we are providing this early version of the manuscript. The manuscript will undergo copyediting, typesetting, and review of the resulting proof before it is published in its final form. Please note that during the production process errors may be discovered which could affect the content, and all legal disclaimers that apply to the journal pertain. A C C E P T E D M A N U S C R I P T ACCEPTED MANUSCRIPT A C C E P T E D M A N U S C R I P T ACCEPTED MANUSCRIPT AbstractThe Martian elastic lithosphere thickness T e has recently been constrained by modeling the geodynamical response to loading at the Martian polar caps and T e was found to exceed 300 km at the north pole today. Geological evidence suggests that Mars has been volcanically active in the recent past and we have reinvestigated the Martian thermal evolution, identifying models which are consistent with T e > 300 km and the observed recent magmatic activity. We find that although models satisfying both constraints can be constructed, special assumptions regarding the concentration and distribution of radioactive elements, the style of mantle convection and/or the mantle's volatile content need to be made. If a dry mantle rheology is assumed, strong plumes caused by, e.g., a strongly pressure dependent mantle viscosity or endothermic phase transitions near the core-mantle boundary are required to allow for decompression melting in the heads of mantle plumes. For a wet mantle, large mantle water contents of the order of 1000 ppm are required to allow for partial mantle melting. Also, for a moderate crustal enrichment of heat producing, elements the planet's bulk composition needs to be 25% and 50% sub-chondritic for dry and wet mantle rheologies, respectively. Even then, models resulting in a globally averaged elastic thicknesses of T e > 300 km are difficult to reconcile with most elastic thickness estimates available for the Hesperian and Amazonian periods. It therefore seems likely that large elastic thicknesses in excess of 300 km are not representative for the bulk of the planet and that T e possibly shows a large degree of spatial heterogeneity.

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Temperature dependence of thermal transport properties of crystalline rocks — a general law

Cited by 141 publications

References 12 publications

Lithosphere thermal structure at the eastern margin of the Bohemian Massif: a case petrological and geophysical study of the Niedźwiedź amphibolite massif (SW Poland)

Lithosphere thermal structure at the eastern margin of the Bohemian Massif: a case petrological and geophysical study of the Niedźwiedź amphibolite massif (SW Poland)

Fission track thermochronology of Neogene plutons in the Principal Andean Cordillera of central Chile (33-35°S): Implications for tectonic evolution and porphyry Cu-Mo mineralization

Implications of large elastic thicknesses for the composition and current thermal state of Mars

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