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temperature dependent. For the Na-K-Ca-Mg geothermometer, these relationships are based on several different mineral equilibria, and these different reactions result in a discontinuous function for this geothermometer. The most commonly used cation geothermometer is the Na-K-Ca-Mg formulations of Fournier and Truesdell (1973) and Fournier and Potter (1979). The Na- K-Ca-Mg geothermometer has two formulations, one for lower (<100oC) temperature waters and one for higher (>100oC) temperature waters. This geothermometer was used extensively in the previous USGS geothermal resource assessment (Brook and others, 1979). However, in the western United States (Brook and others, 1979), these two different formulations result in a major discontinuity and an underreporting in the number of systems in the range between 100oC and 130oC (fig. 4). There should be a larger number of lower temperature geothermal systems, with a systematic decrease in the number of systems as aquifer temperatures increase (see for example, Reed, 1983, fig. 16). Although control from calibration well samples is limited, it appears that the K- Mg geothermometer provides estimated temperatures reasonably close to temperatures measured in drilled geothermal systems within the 90oC to 130oC range. The potassium- magnesium geothermometer relates temperature to the logarithm of the ratio of potassium concentration squared to magnesium concentration, c(K)2/c(Mg) (Giggenbach, 1988). Temperatures were calculated for the geothermal systems (with reported Mg concentrations) in the western United States (Brook and others, 1979), using the K-Mg geothermometer (fig. 5), and these K-Mg geothermometer temperatures exhibit a continuous decrease in the number of geothermal systems as higher temperatures are evaluated, regardless of the type of water chemistry. Because the potassium to magnesium ratio is consistently representative of the subsurface temperature, the K-Mg geothermometer is generally the preferred cation geothermometer in this assessment. The Na-K-Ca geothermometer is preferred in Cl-rich waters and used where Mg data are unavailable. The magnesium ion concentration is below the detection limit in many analyses of geothermal waters, and the K-Mg geothermometer cannot be calculated for these waters. Reservoir Volume The difficulty of developing accurate estimates for the volumes of unexploited geothermal reservoirs varies depending on the geologic setting and the availability of data from exploration and development drilling. Many geothermal reservoirs are dominated by fracture porosity, which can be characterized by high permeabilities but relatively low fluid volumes. In addition, fracture permeability is sensitive to relatively rapid (in geologic time) temporal variations in the state of stress and fluid chemistry, and this can lead to heterogeneous permeability distributions within the fracture-dominated reservoirs (for example, Melosh and others, 2008). Estimates of reservoir volumes in the new assessment are derived from production histories, drilling results, chemical tracer tests, and exploratory geological and geophysical investigations. 8PDF Image | Assessment of Identified Geothermal Resources
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