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Stanley Geothermal Feasibility Study

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Stanley Geothermal Feasibility Study ( stanley-geothermal-feasibility-study )

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current location of the Stanley Hot Springs (Figure 2). Geologic structures, specifically faults, have been identified by previous investigators (i.e. Chapman, 1986; Krahmer, 1995) and by the work done in this study with the gravity survey near this location. One reason why thermal water reaches the surface at this location could be because of the intersection of 2 different faults (Figure 2), which would undoubtedly increase the fracture density and therefore increase permeability within this zone. Higher thermal gradients measured in wells and in the 2 meter survey indicate this is a good area for a test well. From the study of the geothermal system near Stanley, two main trends in faults have been identified that control the geothermal fluid flows, those trending NE-SW related to the Trans-Challis Fault System and those trending NW-SE related to regional extension of the Basin and Range geologic province. The chemical qualities of the geothermal water at the surface and calculated potential reservoir temperatures based on hydrochemistry have been determined. Reservoir temperatures for the system of interest range from 60°-83° C. The decrease in temperature moving SW from Sunbeam Hot Springs to the Stanley Hot Springs is due to the increased mixing of meteoric waters (Table 2). The gravity survey indicates that there is a fault oriented N-S that is locally controlling fluid movement in the area of the Stanley Hot Springs. A conceptual structural model was created by Kathleen Autenreith from Idaho State University based on data that was collected from background literature research and data collected from this investigation. This model takes two faults identified by Krahmer (1995) and projects them into the ground using Vulcan3D modeling software. The result of this modeling is shown in Figure 3. In order to increase the probability of success of any new test wells drilled, it would be reasonable to target areas affected by the intersection of major faults where higher fracture density and permeability would be expected. Figure 2 shows a trend line (blue) that represents the vertical projection to the surface of the predicted below ground fault plane intersection. By calculating the plunge of a line that defines the intersection of the two planes, the depth of that intersection can be estimated for any point along the trend line. The trend line is based on the faults identified by Fisher et al (1992) and this study. An average dip of 55° was calculated from Krahmer (1995) to determine the trend and plunge of 357° and 45°. The dips of faults in this area range from 45°-60° (Krahmer 1995). The shallower depth of 61 meters is essentially the same depth as wells previously drilled in the area and were found to have only moderate temperature due to mixing with shallow groundwater. It is estimated a depth greater than 152 meters would be needed to minimize the ground water mixing and cooling of the resource. Based on gradients in the area, depths of 389-750 meters may be required to obtain adequate temperatures for potential power production. As mentioned in the above, calculated reservoir temperatures based on geothermometers are in the range of 60°-83°C near the Stanley Bathing Pool and as high as 140°C at Sunbeam Hot Springs indicating a potential increase in reservoir temperatures to the north end east along the fault system. Temperatures over 80°C could be used for low temperature binary power production with the effluent from the power plant used for direct heat uses prior to re-injection. Chena Hot Springs in Alaska is successfully using water at 74°C for power production (Lund, 2006). Geothermal fluids at temperatures 7

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