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stay constant at depth. The arrows show the main flow regimes based on temperature and pressure data. In the less optimistic scenario, the wells would show smaller gradients at depth which result in a smaller resource size at a deeper level. A reasonable depth for the target temperature would be 3000 ft at the site of TG-8 and TG-9. Lastly, the worst case scenario could occur by only considering thermal data and excluding the geochemical data. According to this model the 250 °F isotherm would be far below exploitable depths and would not have any interaction with the circulating fluids. These source models assume the gradients in the eastern wells are representative of the deep thermal regime but it is also possible that the deep high temperature source might be totally screened by the presence of shallow cold waters. This could increase the size of the resource toward east. CONCLUSIONS Stable isotope analysis shows that thermal waters in CHS are in meteoric in origin. The 18O and 14C analysis of the spring waters indicates that the circulation time of the meteoric water is less than 3000 yr. The depth of circulation must be about 11,000 ft in order to get temperatures of 250 °F based on a background temperature gradient of 2 °F/100 ft. High background heat flow, deep circulation of thermal waters along the fractures, relatively recent age of the circulating waters, complexity of the fracture patterns, and the distribution of complex pressure regimes makes Chena geothermal system a typical fault/fracture driven geothermal system. This is true in spite of the fact that the system is only 3000 ft long and 300 ft wide. One of the unique applications in this prospect was taking advantage of multi-stage drilling. Although it was not intentionally applied for scientific purposes in Chena, the procedure turned out to be an advantage by greatly increasing the understanding of the flow regimes. So far the drilling activities have been successfully accomplished by delineating production and injection zones and a 0.25 MW power plant has been successfully operated. One of the ultimate goals in development of a production unit is to establish a system that does not allow intrusion of the cold groundwater into the energy conversion cycle. Well communication testing showed that the western end is in close connection with the deep circulating thermal waters (Holdman et al., 2007). The western area is characterized by high permeability and pressure which allows rapid recharge of the hot fluid to the system below depths of 400 ft. The eastern end wells have low deep pressures which is good for injection of the waste water in order to establish a sustainable power source. The high artesian flow rates of the western wells (500 gpm) indicate that the system has a large potential at greater depths and temperatures. Considering the geochemical evidence for temperatures of over 250 °F, further drilling in this area could result in higher temperatures. Thus, even though the system appears relatively small in its surface manifestations, it is quite capable of producing significant geothermal energy if properly managed. REFERENCES Biggar, N. (1973), “A Geological and Geophysical Study of Chena Hot Springs, Alaska”. M.S. Thesis, University of Alaska, Fairbanks, Alaska. Brasz, J. B., and Holdman, G. P. (2005), “Power production from a moderate temperature geothermal resource”, Resources Council Transactions, 29, 729-733 Erickson, D. C., Kyung, I. and Holdman, G. “Geothermal powered absorption chiller for Alaska Ice Hotel”, Geothermal Resources Council Transactions, 29, 57-59 Kolker, A., Newberry, R., Layer, P. Larsen, J. and Stepp, P (2007), “Geologic Setting of the Chena Hot Springs Geothermal System Alaska”, Proceedings of the Thirty-second workshop on geothermal reservoir engineering (this issue) Pritchard, R., (2005), “DIGHEM Survey for Chena Hot Springs Resort, Alaska, Big Delta Quadrangle D-4, D-5 , Circle Quadrangle A-4 and A-5”, Fugro Report #05070. Reed, E. V. and Liu, D. (2006), “Interpretive Report, Natural Source NSAMT and Controlled Source CSAMT Geophysical Surveys, Chena Hot Springs, GRED III Program, Chena Hot Springs, Fairbanks, Alaska”, Report to Chena Hot Springs Resort, 33 pp. plus maps and sections. Waring, G. A. (1917), “Mineral Springs of Alaska” USGS Water Supply Paper 418, 114 Wescott, E., & Turner, D., Eds. (1981), “A Geological and Geophysical Study of the Chena Hot Springs Geothermal Area, Alaska” University of Alaska Geophysical Institute; Report to D.O.E. Wilson, F. H., Dover, J. H., Bradley, D. C., Weber, F. R., Bindtzen, T. K., and Haeussler, P. J., ( 1998), “Geologic Map of Central (Interior) Alaska”, U. S. Geol. Surv. Open-file Rept. 98- 133. Wisian, K. W., Blackwell,D, D and Richards, M.,(2001), “Correlation of heat loss and total energy production for geothermal systems”, Geothermal Resources Council Transactions, 25, 332-335 Yoshikawa, K., (2006), “Chena hot springs resort hydrological investigations”, Unpublished report prepared for Chena Hot Springs Resort, 32 p. Geothermal P . (2005),PDF Image | THERMAL CHARACTERISTICS OF THE CHENA HOT SPRINGS
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