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Resumen:
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Intraplate main structural units of the Iberian Plate (Spanish Central System and Tertiary Basins) results from a mid-Tertiary compressive regime, caused by the convergence of African and European Plates. Crustal structure of this zone has been studied by means of spectral anal y sis of gravity maps. A gravity survey has been canied out anda Gravity map has been produced. Bidimensional spectral analysis of the data allows us to obtain the mean depth of the sources contributing to the total observed fie ld. From the plot of the natural logarithm versus the radial frequency, two major discontinuities are recorded. The deeper one, located to a mean depth of 28 ± 5 km, corresponds to the crust-mantle boundary, in good agreement with seismic data (Suriñach & Vegas, 1988), and the shallower has a mean depth of 7 ± 0.4 km, representing the upper crust-middle crust transition. In order to isolate the regional and residual sources, specific filters has been designed (Gupta & Ramani, 1980). Regional gravity map shows a relative low which expands in a NW-SE direction under the Spanish Central System and surrounding areas of Duero and Tajo Basins. Low and high anomalies distribution in residual gravity map reflects density changes in the upper crust. Two ESW trending strong gradients present in this map are related to the reverse faults which bound the northern and southern linúts of the Spanish Central System with the Basins. The inversion method applied (Parker, 1972) permits us to obtain the three-dimensional Moho discontinuity, whjchs consistent with the two-dirnensional models for the area (Tejero et al., 1996). The Moho geometry is characterised by a N 150° E trending wide through, transverse to the chain, reaching depths greater than 33 km. Thjs through is located in the middle part of the chain, running to the basins. To the northeastern and southwestern part, the Moho rise to 30 km deep, which is the average depth value of the Iberian Plate crust. This gravity analysis together with seismic data are used to constrain spatial variations in density and crustal structure, which combined with thermal data, allow us to designa vertical strength distribution for the crust. Its thermal structure is derived from surface heat flow observations assurning heat production and the1mal conductivity values for sediments, upper crust, lower crust and lithospheric mande. The strength profiles show that ductile-brittle transition occurs between 10 and 15 km. Deepest earthquakes reach depths not far from 15 km, which is in good agreement with these results.
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