P. Schmoldt, PhD - MTNet - DIAS

7. Geology of the Iberian Peninsula
Fig. 7.26.: Filtered heat flow map of the Iberian Peninsula; from Fernandez et al. [1998]. Squares, dots, and triangles denote the
location of sea floor heat-flow measurements, measurements in oil wells, and measurements in water or mining exploration wells,
respectively. The approximate location of the PICASSO Phase I profile is indicated by the red line. The bathymetry is indicated every
200 m.
lower tLAB, a region of enhanced thermal conductivity, or increased radiogenic activity
beneath these southern regions.
Tejero and Ruiz [2002] created 1D thermal models for the Tajo Basin based on surface
heat flow data by Fernandez et al. [1998] and using seismic data of Banda et al. [1981];
Surinach and Vegas [1998]; ILIHA DSS Group [1993]; Gallart et al. [1995]; Pulgar et al.
[1996] for constraints of the lithosphere layer thickness. The authors use heat flow values
of 65 and 70 mW/m 2 for southern and northern Tajo Basin regions, respectively; as well as
a lithosphere consisting of five layers (sediments, upper crust, middle crust, lower crust,
uppermost mantle) with a Moho temperature of 650°C , tLAB temperature of 1350°C ,
and a tLAB depth of 110 km. Details about the layer properties used for the calculation of
the thermal model are summarised in Table 7.4. The tLAB depth derived by Tejero and
Ruiz [2002] is in agreement with results by Artemieva [2006] inferring depths between
100 km and 125 km for the tLAB beneath central Spain using a 1300°C isotherm and
statistical analysis to determine the global lithosphere model TC1; therein, data coverage
was low for the central Spain region though.
From their results, Tejero and Ruiz [2002] derive the geotherms for the Tajo Basin
shown in Figure 7.27, inferring that in this region the Moho does not represent a strong
mechanical discontinuity and that the upper and middle crust are competent layers, with
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