Steady state geothermal model of the crust and the problem of the boundary conditions: application to a rift system, the southern Rhinegraben

Royer, Jean‐Jacques; Danis, Michel

doi:10.1016/0040-1951(88)90062-5

Cited by 26 publications

(16 citation statements)

References 29 publications

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“…In a global compilation Klemperer found the depth to the tops of reflective zones to be generally correlated with heat flow and a nearly constant temperature of 300-400°C was estimated (see also Wever et al 1987;Meissner & Kusznir 1987;Royer & Danis 1988). Similarly Adam has found a correlation between the top of high conductivity lower crustal layers and heat flow with a similar estimated temperature limit (see also Shankland & Ander 1983;Haak & Hutton 1986).…”

Section: Upper Boundary-lower Temperature Limitmentioning

confidence: 90%

Water in the lower continental crust: modelling magnetotelluric and seismic reflection results

Hyndman

Shearer

1989

Geophysical Journal International

331

216

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S U M M A R YMagnetotelluric and multichannel seismic reflection measurements indicate that the Phanerozoic lower continental crust is commonly electrically conductive and reflective, in contrast to a more resistive and transparent middle to upper crust. A few per cent free saline water can provide an explanation for both results along with the apparent requirement that neither the conductive nor the reflective properties are retained when lower crustal rocks are brought to the upper crust. Common 10 km thick and 20-30 Qm resistivity layers can be explained with 0.5-3 per cent pore water, if there are equilibrium pore geometries and the salinity is close to that of sea-water as suggested by lower crust fluid inclusions. Seismic velocities and impedances must be affected if such porosity exists. Seismic reflectors with reflection coefficients of 5-10 per cent can be explained by layers or lamellae with porosity contrasts of 1-4 per cent and reasonable effective pore aspect ratios of 0.1-0.03. A minimum temperature of 350°C is estimated from a correlation between heat flow and depth to the top of conductive and reflective layers. The upward limit in the crust may occur at an impermeable boundary formed by hydration reactions at the top of greenschist facies conditions or by precipitation of silica. It also may be associated with the minimum temperature for ductile behaviour and equilibrium grain boundary pore configurations. The maximum temperature is about 700 "C according to the evidence indicating that there is no free water in granulite facies conditions. Areas that have been subject to such high temperature conditions without the subsequent addition of water, i.e. the lower crust of shields, are generally non-reflective and electrically resistive.

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Section: Upper Boundary-lower Temperature Limitmentioning

confidence: 90%

Water in the lower continental crust: modelling magnetotelluric and seismic reflection results

Hyndman

Shearer

1989

Geophysical Journal International

331

216

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“…Tem per a tures mea sured in the Soultz bore holes [Schellschmidt and Clauser, 1996] indi cate a high gra di ent in the first kilo metre (over 100 o C/km), de creas ing from 1000 m to 2000 m (around 30 o C/km), and be com ing very low be low 2000 m (un der 20 o C/km). This evo lu tion could be ex plained by a com bi nation of sev eral ef fects, in clud ing (i) a ther mal in su la tion ef fect due to the slightly lower con duct ing sed i ments [Schwarz and Henk, 2005], (ii) a large-scale fluid cir cu lation in the per me able zones of the gran ite roof, which brings hot flu ids be neath the sed i men tary cover [Sanjuan et al, 2006], (iii) a sig nif i cant heat ing ef fect due to the an omalously high ra dio ac tive con tent of the gran ite [Royer and Danis, 1988] and (iv) a thin ning of the crust due to the Oligocene rift ing [Brun et al, 1992]. As ex pected, our temper a ture maps show a local ised high pos i tive anom aly in the north ern part of the French Rhine graben at 1000 m depth ( fig.…”

Section: The Rhine Gra Benmentioning

confidence: 99%

Subsurface temperature maps in French sedimentary basins: new data compilation and interpolation

Bonté

Guillou-Frottier

Garibaldi

et al. 2010

Bulletin De La Société Géologique De France

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International audienceAssessment of the underground geothermal potential requires the knowledge of deep temperatures (1-5 km). Here, we present new temperature maps obtained from oil boreholes in the French sedimentary basins. Because of their origin, the data need to be corrected, and their local character necessitates spatial interpolation. Previous maps were obtained in the 1970s using empirical corrections and manual interpolation. In this study, we update the number of measurements by using values collected during the last thirty years, correct the temperatures for transient perturbations and carry out statistical analyses before modelling the 3D distribution of temperatures. This dataset provides 977 temperatures corrected for transient perturbations in 593 boreholes located in the French sedimentary basins. An average temperature gradient of 30.6°C/km is obtained for a representative surface temperature of 10°C. When surface temperature is not accounted for, deep measurements are best fitted with a temperature gradient of 25.7°C/km. We perform a geostatistical analysis on a residual temperature dataset (using a drift of 25.7°C/km) to constrain the 3D interpolation kriging procedure with horizontal and vertical models of variograms. The interpolated residual temperatures are added to the country-scale averaged drift in order to get a three dimensional thermal structure of the French sedimentary basins. The 3D thermal block enables us to extract isothermal surfaces and 2D sections (iso-depth maps and iso-longitude cross-sections). A number of anomalies with a limited depth and spatial extension have been identified, from shallow in the Rhine graben and Aquitanian basin, to deep in the Provence basin. Some of these anomalies (Paris basin, Alsace, south of the Provence basin) may be partly related to thick insulating sediments, while for some others (southwestern Aquitanian basin, part of the Provence basin) large-scale fluid circulation may explain superimposed cold and warm anomalies

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“…A 2D thermal structure was estimated along five DSS profiles across major tectonic provinces of Central and Eastern Europe by Cermak (1989). Royer and Danis (1988) have delineated the 2D thermal structure in the region from the Black Forest in Rhinergraben to the southern Vosges. The temperature-depth distribution was calculated along the Taratashskiy profile that crosses the Ural Mountain (Safanda et al, 1992) and along another profile in the central Fennoscandian shield that extends from Archaean granitegreenstone terrain in the NE to the Proterozoic domain in the SW (Kukkonen, 1998).…”

Section: Introductionmentioning

confidence: 99%

A tentative 2D thermal model of central India across the Narmada-Son Lineament (NSL)

Rai

Thiagarajan

2006

Journal of Asian Earth Sciences

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Steady state geothermal model of the crust and the problem of the boundary conditions: application to a rift system, the southern Rhinegraben

Cited by 26 publications

References 29 publications

Water in the lower continental crust: modelling magnetotelluric and seismic reflection results

Water in the lower continental crust: modelling magnetotelluric and seismic reflection results

Subsurface temperature maps in French sedimentary basins: new data compilation and interpolation

A tentative 2D thermal model of central India across the Narmada-Son Lineament (NSL)

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