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24 Chapter 2 Geothermal ResourceBase Assessment the ongoing assessment of hydrothermal geothermal resources being conducted by the USGS. However, some larger basement EGS resource areas that might, in some sense, be considered marginal to hydrothermal systems – such as The Geysers/Clear Lake area in California and the High Cascades Range in Oregon – are included in this discussion (see Section 2.3.5). The data set used to produce the Geothermal Map of North America, published by the American Association of Petroleum Geologists (AAPG) (Blackwell and Richards, 2004a), is the basic thermal data set used in developing the resource assessment. The conterminous U.S. portion of the map is shown in Figure 2.1. In order to expand coverage from the earlier GSADNAG map (Blackwell and Steele, 1992; Blackwell et al., 1991) and early versions of this type of resource evaluation (Blackwell et al., 1993; Blackwell et al., 1994), extensive industryoriented thermal data sets were used, as well as published heat flow data from research groups. To that end, a western heatflow data set was developed, based on thermal gradient exploration data collected by the geothermal industry during the 1970s and 1980s (Blackwell and Richards, 2004c; Kehle, 1970; Kehle et al., 1970). The basic information in this data set consists of temperaturedepth/gradient information. However, thermal conductivity and heat flow were also determined for as many of the sites as possible, based on thermal conductivity estimates from geologic logs (where available), and geologic maps for other sites where there were no well logs. About 4,000 points were used in the preparation of the map (of the 6,000 sites in the database). The focused nature of the drilling is shown by the clumps of data on Figure 2.2, especially in western Nevada and southwestern Utah. A second industry data set consisting of about 20,000 point bottomhole temperature (BHT) measurements, compiled in the early 1970s and published in digital form (AAPG CDROM, 1994), was also utilized. The AAPG BHT data set was augmented in Nevada by BHT data digitized from hydrocarbon exploration well logs in the files of the Nevada Bureau of Mines and Geology. Use of the BHT data required extensive analysis of the error associated with the determination of in situ equilibrium temperatures from these nonequilibrium data. That process is described briefly in Section 2.2.2 and, in more detail, by Blackwell and Richards (2004b, c). The heat flow varies from less than 20 mW/m2 in areas of low heat flow to more than 150 mW/m2 in areas of high heat flow. The causes of the variations and the distribution of heat flow in the conterminous United States are discussed in detail by Roy et al. (1968, 1972), Sass et al. (1971), Lachenbruch and Sass (1977), Reiter et al. (1986), Morgan and Gosnold (1989), Blackwell et al. (1991), and others. The value of surface heat flow is the building block for the temperatureatdepth calculation (see Figure 2.3). Individual sites have thermal conductivity (rock columns) that varies with depth and, thus, the average thermal gradient depends on the depth interval studied – whereas, heat flow does not. In this study, contours of measured heat flow are combined with regionally specific, depthaveraged thermal conductivity models to more accurately represent the largerscale thermal regime (i.e., average gradients and temperatures as a function of depth).PDF Image | Geothermal Resource Base Assessment
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