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Cardoso, Hamza and Alfaro the continental area. Experimental heat flow data are currently available for slightly more than 50% of the grid elements. The gridded data has been useful in the past in deriving heat flow maps of the South American continent (Hamza and Muñoz, 1996; Hamza et al, 2005). For purposes of the present work estimated values derived from spherical harmonic expansion of the global heat flow field (Cardoso, 2006; Hamza et al, 2008) were used for those grid elements for which experimental data are not available. The map of Figure (1) illustrates the distribution of experimental and estimated values. Figure 1: Discretized representation (2ox2o grids) of geothermal data distribution for South America. The colored grids indicate areas with experimental data. Heat flow values for the remaining cells were calculated using spherical harmonic coefficients derived from global heat flow map (Cardoso, 2006; Hamza et al, 2008). Figure 2: New heat flow map of South America based on updated data base and estimated values based on spherical harmonic expansion to degree 36 of the global heat flow (Hamza et al, 2008). This data base has recently been updated with temperature gradient and heat flow values for several new localities. Most of the new data are from the sedimentary basins of Catatumba, Cusiana, Cupiaga, Eastern Cordillera, Llanos, Magdalena and Putumayo, situated in the Andean region of Colombia (Alfaro, Personal communication), coastal areas of eastern Brazil (in the states of Ceará, Rio Grande do Norte, Bahia and Espirito Santo) and the São Francisco craton in central Brazil. The new heat flow map of South America derived from the updated data base is presented in Figure (2). 3. CRUST AL MODEL USED IN RESOURCE ASSESSMENT In addition to the temperature and heat flow data sets use has also been made, in the present work, of complementary information on thickness, density and seismic velocity of the crustal layers. For this purpose use has been made of global crustal data compilations by Mooney et al, (1998) and by Bassin et al (2000). The compilation of Bassin et al (2000) provides mean values for 20 x 20 grid elements. In these data sets the crust is assumed to be composed of five sequential layers, classified as: soft sediments, hard sediments, upper crust, middle crust and lower crust. A schematic representation of the crustal model adopted for resource estimates is illustrated in Figure (3). Figure 3: Schematic representation of the crustal model adopted for resource estimates. It often happens that all three top layers (soft sediments, hard sediments and upper crust) may not be present at depths less than 10km in all crustal segments. In fact three possible types of crustal types can be envisaged: Type 1- composed of just the sedimentary layers (soft and/or hard), but without upper crust; Type 2- devoid of any sedimentary cover, hence only upper crust may be present; Type 3- where both sediment layers and upper crust are present. In this last case, three subcategories may exist: Type 3a: soft sediment and upper crust; Type 3b: hard sediment and upper crust Type 3c: soft and hard sediments as well as upper crust. Following Muffler and Cataldi (1978) we have limited the resource base calculations to the maximum depth limit of 10 km. Since the minimum thickness of the layer classified as upper crust is 10 km it is not necessary to take into consideration resources associated with the middle and lower crustal layers. In some resource assessment studies depth limit for accessible resource base is set as 3 km. In 2PDF Image | Geothermal Resource Base for South America: A Continental Perspective
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