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THERMAL CHARACTERISTICS OF THE CHENA HOT SPRINGS

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THERMAL CHARACTERISTICS OF THE CHENA HOT SPRINGS ( thermal-characteristics-ofchena-hot-springs )

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reasonable estimate range for the power generation at Chena might be from 1 to 10 MW. The highest output is probably only reachable if the higher temperatures indicated by the geochemical thermometers occur over most of the anomaly region and at economic depths, probably less than 3000 ft. Ions, isotopes and mixing models Deep water samples from the wells show a similar chemical characteristic hot spring waters. The most saline and therefore the most primitive waters are found in the vicinity of TG-8 and TG-9, where highest temperatures were found. The high salinity wells are highly clustered in the western part of the anomaly from Well 4 to TG-9. The low salinity wells are located east of Well 4. The low salinities in the eastern wells are likely due to mixing with the surface water. Interestingly, although the deep well TG-7 is the hottest in the eastern part (T ~ 153 °F), water samples from depth of 450-500 ft show very low salinity which might indicate a great amount of mixing occurs in this area even at great depths. This could imply larger temperatures in the deeper parts than what is observed by temperature logs. Although the highest temperature found so far is 176 °F, both Na-K-Ca and SiO2 geothermometers suggest temperatures of 260±10 °F. Samples from both eastern and western wells show the same high geochemical temperatures. Previous studies of hot spring waters estimated temperatures around 266 °F based on the same methodology. Therefore, the geochemical studies clearly indicate higher temperatures somewhere in the CHS geothermal system. In order to understand the possible source of deep waters and timing of the circulation, a stable isotope study based on 18O was carried out at SMU. Small δ18O shifts from the meteoric line (0.5 mil) shows that the deep water is meteoric in origin and has a relatively recent recharge history. 14C analysis shows the age to be less than 3000 yr (Yoshikawa, 2006). Static well pressures The well pressures show varying characteristics with increasing depth (Holdman et al., 2007). Shallow pressures in wells up to 200 ft deep (at a constant elevation of 1120 ft) change gradually from 52.5 psi in Well 1 to 31 psi in TG-3 which follows the general topography (decreasing to the west). In the west, the pressures are slightly higher compared to the hydraulic head associated with the deep geothermal system. In deep wells TG-8 and TG-9, the static increase of pressures with depth is well above the corresponding hydrostatic head. A pressure map below 300 ft shows increase opposite to the shallow regime and the topography that is toward the east. In the southeast part, deep well TG-7 has a pressure which is 17 psi less than TG-8. This clearly indicates that the recharge of the shallow geothermal system is in the west. This is in agreement with the temperature logs which indicate eastward flow of deep fluids by overturns. THE COMBINED CONCEPTUAL MODEL Both temperature and pressure data indicates that the deep thermal waters enter the shallow system at depths below 600 ft at a distance of 300 ft west of the main hot springs (TG-8 and TG-9 sites). Upon entry to shallow levels, the thermal waters migrate toward the east where the pressure due to the deep geothermal systems declines. The thermal waters find ways to the surface at the current location of the hot springs where rocks are highly permeable. Part of the water continues to flow toward the north-east along the shallow fractures. Geochemical analysis of the waters shows that a substantial amount of mixing between groundwater and geothermal water occurs here. This makes the deep resource estimation in the eastern end even more difficult. In the west, at TG-11, the projected depth for 250 °F is about 1500 ft assuming conductive T-D behavior. Here, if the gradients are lower at greater depths the source temperatures could be deeper. Figure 7 Conceptual model for temperatures in CHS The wells in the main cluster are likely reflecting a shallow convective flow pattern. Therefore a single deep thermal model of the area would not be possible. This is especially the case in the east where lateral flow of geothermal water screens deep thermal regime. A good approach is to give bracket for the possible scenarios. Figure 7 shows a 2D representation of the best possible scenario based on results of subsurface temperatures from the existing wells. According to this, the gradients in the wells

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