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Prospecting for a Blind Geothermal System Utilizing Geologic and Geophysical Data, Seven Troughs Range, Northwestern Nevada

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Prospecting for a Blind Geothermal System Utilizing Geologic and Geophysical Data, Seven Troughs Range, Northwestern Nevada GRC Transactions, Vol. 38, 2014 Prospecting for a Blind Geothermal System Utilizing Geologic and Geophysical Data, Seven Troughs Range, Northwestern Nevada Corina Forson1, James E. Faulds1, and Phil Wannamaker2 1Nevada Bureau of Mines and Geology, University of Nevada, Reno NV 2Energy and Geoscience Institute, University of Utah, Salt Lake City UT Keywords resources. Researchers estimate that only ~20% of the accessible Nevada, Basin and Range, structural controls, Seven Troughs geothermal resources in the Great Basin have been discovered, Range, blind geothermal system, exploration, geologic map- suggesting that opportunities abound for discovering blind or ping, Magnetotelluric, two-meter survey hidden geothermal systems (Brook et al., 1979; Richards and Blackwell, 2002). If prospecting for a truly blind geothermal system, it becomes Abstract important to distinguish between a blind, hidden, and conventional geothermal resource. All geothermal systems have three main The Seven Troughs Range in Pershing County, Nevada, has elements: heat source (magmatic or high geothermal gradient in been identified as an area with high potential for hosting a blind amagmatic settings), reservoir (to hold and sustain the hot water), geothermal system. A reconnaissance 2D magnetotelluric (MT) and fluid, which is the medium that transfers the heat. Conven- survey across the western U.S. has shown a possible correlation tional geothermal systems exhibit fluid surface manifestations, between broad low resistivity anomalies, extending from the up- such as fumaroles or hot springs. Hidden geothermal systems per to deep crust, and loci of high enthalpy geothermal systems. lack fluid features on the surface but contain more subtle features Where MT surveys have been conducted across the Basin and (or paleo manifestations), such as siliceous sinter, travertine, tufa Range, anomalous zones of high conductivity strongly correlate deposits, and/or hydrothermally altered rocks. Vegetation can also with known high temperature geothermal systems, such as Dixie serve as an indicator, as it can be concentrated in lineaments along Valley, Coso, and McGinness Hills; as well as anomalies in 3He R/ faults that leak fluids or be absent near faults leaking toxic gasses. Ra. Along the regional MT transect only a few areas of pronounced Blind geothermal systems are confined to the subsurface; lacking upwelling are not connected with any known geothermal systems any obvious fluid features and/or paleo-manifestations associated (e.g., Kumiva Valley region). These locations are hypothesized to with conventional or hidden systems. have high potential for hosting blind geothermal systems. Thus, Within both magmatic and amagmatic environments faults this project focuses on identifying favorable structural settings for and fractures within the brittle crust play an important role in geothermal activity in the Kumiva Valley area and more specifi- generating and maintaining permeability and transporting fluids cally the Seven Troughs Range, where the low resistivity anomaly to the surface. In amagmatic systems, and more specifically the reaches the near surface. Detailed geologic and structural analyses extensional setting of the Basin and Range, moderate to steeply were conducted to identify favorable structural settings for geo- dipping faults and fractures promote the transmission of meteoric thermal activity that are likely to host a blind geothermal system. fluids to depth (Blackwell, 1983). The depth of circulation re- An initial two-meter temperature survey was also conducted to quired to attain high temperatures depends on the permeability of further assess two favorable structural settings in the area. the rocks and the geothermal gradient. Areas with known recent faulting (i.e., Quaternary) are ideal for prospecting for geothermal Introduction systems, because the most substantial fluid migration in a fault system is likely during and after rupture events (Micklethwaite A majority of the operating geothermal power plants and and Cox, 2004). It comes as no surprise that a majority of the prospects have utilized the presence of surface manifestations known geothermal systems in the Great Basin region of the Basin (i.e., geysers, boiling mud pots, hot springs, sinter terraces etc.) to and Range province are spatially associated with faults, and many locate areas of high geothermal potential (e.g., Bradys geothermal are temporally associated with Quaternary faults. In the Great system; Faulds et al., 2010). However, many resources have little Basin many geothermal systems are found proximal to normal or no surface manifestations and are considered ‘hidden’ or ‘blind’ and oblique-slip faults, suggesting that such faults control or chan- 369 Forson, et al. nel hydrothermal fluids. Faults oriented orthogonal to the least in Pershing County, northwestern Nevada, and 2) to estimate the principal stress direction are most likely to host high temperature possible locations of blind geothermal resources in that area. geothermal systems (Faulds et al., 2004, 2006, 2011). Within the The field area is located ~50 km northwest of Lovelock, Nevada northwestern Great Basin, the regional extension direction trends (Figure 1). This specific field area was chosen based on the loca- west-northwest. Accordingly, normal faults striking north-north- tion of a regional magnetotelluric (MT) anomaly (Wannamaker east host most of the geothermal systems (Coolbaugh et al., 2005; et al., 2011; Figure 2A). In addition, an ongoing study funded by Faulds et al., 2005). However, many north-northeast-striking faults the Department of Energy aims to integrate MT data, soil gas flux in this region show no signs of geothermal activity. Therefore, it and geochemistry, and structural analysis to recognize heretofore is necessary to recognize common structural settings of known undiscovered blind geothermal resources. geothermal systems to aid in the discovery of blind systems with The reconnaissance 2-D MT survey has shown a possible cor- no surface manifestations. relation between low resistivity in the deep crust and magmatic Several fault patterns have been recognized as particularly underplating in areas with high rates of recent extension (e.g., favorable structural settings for geothermal activity (Curewitz and Dixie Valley region). The deep crustal, low resistivity anomalies Karson, 1997; Faulds et al., 2006, 2011), including: 1) overlapping are linked to tapering zones of lower resistivity in the upper crust, normal faults (step-overs) with hard linkage, 2) terminations of suggesting that deep crustal fluids can upwell to remarkably major normal faults (horse-tailing), 3) intersections of normal, shallow depths (Wannamaker et al., 2011). The presumed lower strike-slip, and/or oblique-slip faults, 4) accommodation zones crustal magmatic underplating may be spatially correlated to where belts of oppositely dipping normal faults intermesh, and 5) large crustal breaks that may accommodate the efficient transfer transtensional pull apart zones. These structural controls can be of high temperature fluids from deeper levels to the near surface. identified via topographical manifestations, such as 1) major steps Where reconnaissance MT surveys have been conducted across the in rage fronts, 2) interbasinal highs, 3) mountain ranges consisting Basin and Range, anomalous zones of high conductivity strongly of relatively low, discontinuous ridges, and 4) lateral terminations correlate with known high temperature geothermal systems, such of mountain ranges (Faulds et al., 2006, 2011). as Dixie Valley, Coso, and McGinness Hills (Wannamaker et al., 2011) (Figure 2B). Commonly, these systems exhibit significant Motivation and Purpose of This Study 3He R/Ra anomalies, a further indication of magmatic input (Ken- nedy and van Soest, 2007). Along the MT transect conducted by The purpose of this study is 1) to determine the structural set- Wannamaker et al. (2011), only a few areas of pronounced up- ting and geothermal potential of the central Seven Troughs Range welling associated with deep crustal, low resistivity anomalies are not connected with any known geothermal systems (e.g., Kumiva Valley region, Figure 2B&C). These locations are hypothesized to have high geothermal potential. Thus, this project focuses on identifying favorable structural settings for geothermal activity in the Kumiva Valley area and more specifically the Seven Troughs Range, where the low resistivity anomaly reaches the near surface (Figure 2C). The field area lies in the central Seven Troughs Range (Figures1and 3), where the Kumiva Valley MT anomaly is nearest to the surface (Wannamaker et al., 2011). This area may be analogous to Dixie Valley or McGinness Hills (Figure 2B), where en- hanced geothermal activity and possible deep crustal breaks correlate with areas of elevated conductivity. These low-resistivity upwelling zones likely mark areas in which geothermal fluids circulate from depth to the surface. However, there is no known geothermal system in the Seven Troughs Range. Nonetheless, the 2-D MT anomaly in this area (Figure 2C) and a preliminary analysis for favor- able structural settings suggest that this location has relatively high potential to host a blind geothermal system. The Kumiva Valley area is therefore a green- Figure 1. The great Basin physiographic province outlined in red. The Four geothermal/struc- field exploration area without current recognized tural domains are highlighted in green (from Faulds et al.,
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