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28 Chapter 2 Geothermal ResourceBase Assessment Although there are BHT data in some areas to depths of 6,000 m, the maximum depth used for the correction was 4,000 m, due to limited information on the drilling effect for deeper wells, and a lack of calibration wells at those depths. Generalized thermal conductivity models for specific geographic areas of the various sedimentary basins were used to compute the heat flow associated with the BHT gradients. The results were checked against conventional heatflow measurements in the same regions for general agreement. 2.2.2 Geothermal gradients Data from the Western Geothermal Database were also used to prepare the contour map. These are heatflow measurements derived from thermal gradient exploration wells drilled primarily for geothermal resources exploration in the western United States, generally during the late 1970s and 1980s. The majority of these wells are 150 m or less in depth. The raw data were processed to calculate heat flow where there was sufficient information. There are site/wellspecific thermal conductivity data for about 50% of the sites. In the Basin and Range, most of the sites are in the valley fill. Thermal conductivity was assumed for these wells based on lithology logs or, in the absence of even this data, on wellsite geology maps. The flow of the temperatureatdepth calculations is shown in Figure 2.3. There are discussions of each of the main parameters used in the following sections. The important parameters are the measured heat flow (this section), the thermal conductivity distribution (Section 2.2.3 and 2.2.4), the surface temperature (Section 2.2.5), and the distribution of heat due to radioactive elements in the crust (U, Th, K) (Section 2.2.6). In the calculations, Q0 is the measured heat flow, K is the thermal conductivity, Qm is the mantle or tectonic component of heat flow (Section 2.2.6), A is the radioactive heat generation, r is the scaled depth of the radioactivity effect (10 km in these calculations, see Section 2.2.6), X is the depth of the temperature calculation, the subscript s indicates the sediment section, and the subscript b indicates the basement section of the calculation. The mean thermal gradient in the sedimentary section can be found by dividing the heat flow by the thermal conductivity (see Figure 2.3). The variation in the mean gradient is from less than 15°C/km to more than 50°C/km on a regional basis. Within an individual well, the geothermal gradient can vary by up to a factor of 5 or more, depending on the lithology in a particular depth interval. However, the whole sedimentary section is averaged in the approach used here. Unlike thermal gradient maps produced from direct observations from individual wells (Kron and Stix, 1982; Nathenson and Guffanti, 1980; DeFord and Kehle, 1976), the gradients produced as described in this section and the subsequent temperatureatdepth calculations are not biased by the part of the sedimentary section in which the measurements were made. Thus, the geothermal gradient distribution used here is smoother and more regionally characteristic of the average geothermal gradient to depths below where direct measurements exist. This smoothing process produces a somewhat different temperatureatdepth result than would be obtained from extrapolation of existing gradient compilations that do not include thermal conductivity and heatflow analyses.PDF Image | Geothermal Resource Base Assessment
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