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the present work this limit has been adopted in calculating the total resource base. The maps of Figures (4a), (4b) and (4c) illustrate spatial distributions of the thicknesses of these layers in South America. Note that the thickness of soft sediments (see Figure 4a) is in excess of 1.5km in the northern parts of Colombia and Venezuela. It is in the range of 0.5 to 1.5km in most parts of the Pre Cordilleran and Paleozoic basins. Soft sediments are present as a thin layer with thickness less than 500m in large parts of the Precambrian cratonic areas and in the Andean ranges. Figure 4a: Map of thickness of soft sedimentary layers, derived from crustal data of Bassin et al (2000).. The hard sedimentary layers have thicknesses reaching up to 8km. Regions with thickness greater than 2km seem to be situated along an arc shaped belt extending from Venezuela to south Brazil. It is practically absent in Precambrian cratonic areas (see Figure 4b). Figure 4b: Map of thickness of hard sediment layers, derived from crustal data of Bassin et al (2000). On the other hand, thickness variations of upper crustal layer present a quite different pattern. As can be seen from Figure (4c) thicknesses of this layer reach up to values of 24km in the central Andean region. Thickness values are in the range of 12 to 20km in the central parts of the continent. Both the northern and southern extremes are characterized by relatively thin upper crust (thicknesses less than 12 km). Figure 4c: Thickness of upper crust in South America derived from the data set of Bassin et al (2000). 4. CRUSTAL TEMPERATURES Vertical distributions of temperatures in the crustal layers were calculated for each of the 20 x 20 cells. A simple one dimensional heat conduction model, that incorporates the effects of depth-dependent variations in thermal conductivity and radiogenic heat production, was used for this purpose. The relation for temperature (Ti) as a function of depth (zi) for the ith grid element is: q−AD AD2 T(z)=T + 0i 0i i z+ 0i i [1−e−Zi/Di ](1) 0i ki ki where T0i is the surface temperature, q0i the surface heat flux, A0i radiogenic heat productivity and ki the thermal conductivity of the ith element. The values of A0i is derived from empirical relations (Cermak et al, 1990) relating crustal seismic velocities with radiogenic heat productivity. The thermal conductivity values of the sedimentary layers were derived from the heat flow data base. The spatial distributions of basal temperatures of the soft and hard sediment layers and upper crust, calculated using equation (1), are presented in Figures (5a), (5b) and (5c) respectively. Note that temperatures in excess of 800C at the base of soft sediments (see Figure 5a) occur only in northern Venezuela, altiplano region and northern Chile. In most of the remaining regions it falls in the range of 40 to 600C. In the case of hard sediments (see Figure 5b) the basal temperatures in excess of 800C occur in several localities lying along an arc shaped belt extending from northern Venezuela to central Brazil, passing through southeast Ecuador and Altiplano region of Bolivia. Temperatures of less than 800C are found along the eastern parts of the continent. Cardoso, Hamza and Alfaro 3PDF Image | Geothermal Resource Base for South America: A Continental Perspective
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