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214 Chapter 2 Geothermal ResourceBase Assessment et al., 1968). In contrast, in parts of the nearby Adirondack Mountains, the heat flow is only 30 mW/m , 2.3 EGS Resource Maps and ResourceBase Estimates – Lower 48 States 2.3.1 Heat (thermal energy) content 2 because the upper crustal rocks have very small radioelement content. In the analysis of temperatures to 10 km, the heat flow from below the layer of radioactive elements providing a heat source in the continental crust must be known, because the depthscale of the radiogenic contribution is similar to the depth of calculation. For the majority of the area covered by the analysis, two different “mantle” heat flow values were used: 60 mW/m2 for the high heatflow regions in the west and 30 mW/m2 for most of the rest of the map area. The region of high mantle heat flow is shown as the dotted area inside the heavy black line in Figure 2.6. The high mantle heat flow is a result of the plate tectonic activity (subduction) that has occurred along the west coast of North America during the past 100 million years, and the hot spot activity along the Yellowstone/Snake River Plain track (Blackwell, 1989). Part of the Cascade Range in the Pacific Northwest (active volcanic arc) and part of the Snake River Plain (hot spot track) were assigned mantle heat flow values of 80 mW/m2, because they are associated directly with geologically young volcanism. Finally, part of the Great Valley/Sierra Nevada Mountains areas were given a mantle heat flow of 20 mW/m2 compatible with the outer arc tectonic setting in those areas (see Morgan and Gosnold, 1989; Blackwell et al., 1991). Transitions in heat flow between these different areas are generally sharp on the scale of the map, but are hard to recognize in some locations, because of the variable heat flow due to the upper crustal effects. Nonetheless, as deeper depths are considered, this regional factor becomes dominant. The results of the analysis described in the previous section are presented as temperatureatdepth maps and as thermal energy (or “heat”) in place. The temperatures were calculated from the depths of 3 to 10 km at every km. The mean values at 0.5 km intervals were used in the recoverable resource analysis in subsequent chapters. Maps of the temperature at 3.5 km, 4.5 km, 5.5 km, 6.5 km, 7.5 km, and 10 km are shown in Figure 2.7. Heatinplace was calculated and is listed in Table A.2.1 for 1 km x 1 km x 1 km blocks centered at depths of 3.5, 4.5, 5.5, 6.5, 7.5, 8.5, and 9.5 km using the assumptions and equations shown in Figure 2.3. The values listed in Table A.2.1, and shown in the histogram in Figure 2.8, represent the geothermal resource base and not the power that can be generated. For demonstration purposes, the values are shown in terms of stored thermal energy, namely, exajoules (EJ = 1018 J). The only area excluded from the calculation is Yellowstone National Park (8,980 km2). It represents a large area of high temperature, and so its exclusion affects the resource base calculation of areas at high temperature at shallow depths. The histogram in Figure 2.8 shows that there is a tremendous resource base of approximately 13 million EJ, between the depths of 3.5 to 7.5 km in the temperature range of 150°C to 250°C. Even if only 2% of the resource were to be developed, the thermal energy recovered would be 260,000 EJ. This amount is roughly 2,600 times the annual consumption of primary energy in the United States in 2006. To understand the magnitude of the thermal energy or heat content of the rock, it is useful to consider the following “thought experiment.” Imagine a 14 km long x 14 km wide x 1 km thick slice of rock below the ground surface, which is at an initial temperature of 250°C. Reasonable average values are 2,550PDF Image | Geothermal Resource Base Assessment
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