Time-variation of hydrothermal discharge at selected sites in the western United States: implications for monitoring

Ingebritsen, Steven E.; Galloway, Devin L.; Colvard, Elizabeth M.; Sorey, M.L.; Mariner, R.H.

doi:10.1016/s0377-0273(01)00207-4

Cited by 78 publications

(54 citation statements)

References 52 publications

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“…Boles et al (2015) calculate a permeability of ∼10 −17 m 2 associated with deep upflow of mantle helium along a paleosubduction zone in the Los Angeles Basin. Both of these are several orders of magnitude higher than bulk permeability of intact crystalline rock (∼10 −23 m 2 ; Ingebritsen et al, 2001). Wisian and Blackwell (2004) estimate permeability in shallow geothermal systems must reach ∼10 −15 -10 −16 m 2 for natural fluid circulation to occur.…”

Section: Discussionmentioning

confidence: 93%

Regional crustal-scale structures as conduits for deep geothermal upflow

Siler

Kennedy

2016

Geothermics

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a b s t r a c tGeothermal fluids produced from two of the largest production geothermal fields in the Great Basin have helium isotope ratios that are anomalously high relative to basin-wide trends. These data indicate that the geothermal systems, Dixie Valley, Nevada and McGinness Hills, Nevada have an anomalously high fraction of mantle derived fluid. These connections to deeply derived fluid and heat may supplement crustal heat production and be responsible, in part, for the anomalously high production capacity, relative to other Great Basin geothermal fields, that Dixie Valley and McGinness Hills support. Deep-seated crustal structures across the Great Basin and around the world are known to be associated with structural reactivation, can have relatively high permeability, and can act as fluid flow conduits. These deep seated structures across the Great Basin control upflow of deeply derived heat and fluids into the shallow geothermal systems at Dixie Valley and McGinness Hills, contributing to their productivity.

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Section: Discussionmentioning

confidence: 93%

Regional crustal-scale structures as conduits for deep geothermal upflow

Siler

Kennedy

2016

Geothermics

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“…The "Cl-inventory" uses Cl as the conservative tracer. As mentioned earlier, this is true for less acidic magmatic-hydrothermal systems (Ingebritsen et al 2001;Taran and Peiffer 2009;Chiodini et al 2014;Collard et al 2014). Measuring the Cl-release from rivers draining thermal springs, and knowing the Cl-content and Cl/solute ratios in thermal spring waters, the rock mass removal rate can be estimated by:…”

Section: Rock Leaching Upon Weatheringmentioning

confidence: 95%

“…heat output) from springs can be estimated, by multiplying the enthalpy of discharged spring waters, often based on geothermometric temperatures of the deep system, with the spring discharge rates. Such estimates were obtained for the active magmatic-hydrothermal systems of El Chichón and Tacaná (both in Chiapas, Mexico;Taran and Peiffer 2009;Collard et al 2014), and Domuyo (Argentina; Chiodini et al 2014), and originally of the Cascades Volcanic Range by Ingebritsen et al (2001). Understanding the state of unrest on the long term of a specific volcano is needed to rule out if the volcano would be a feasible target for geothermal exploitation, or not.…”

Section: Rock Leaching Upon Weatheringmentioning

confidence: 99%

Fluid Geochemistry and Volcanic Unrest: Dissolving the Haze in Time and Space

Rouwet

Hidalgo

Joseph

et al. 2017

Advances in Volcanology

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The heat and gas released by a degassing magma affects the overlying predominantly meteoric aquifers to form magmatic-hydrothermal systems inside the solid body of a volcano. This chapter reviews how fluid geochemical signals help to track the evolution throughout the various stages of volcanic unrest. A direct view into a degassing magma is possible at open-conduit degassing volcanoes. Nevertheless, in most cases gas is trapped (i.e. scrubbed) by abundant water, leading to the loss of the pure signal the magma ideally provides. Deciphering how magmatic gas rises through, reacts, and re-equilibrates with the liquids in the magmatic-hydrothermal system in time and space is the only way to trace back to the pure signal. The most indicative magmatic gas species (CO 2 , SO 2 -H 2 S, HCl and HF) are released as a function of their solubility in magma. The less soluble gas species are released early from a magma at higher pressure conditions (CO 2 ) (deeper), whereas the more soluble species are released later, at lower pressures (SO 2 , HCl and HF) (shallower depth). When these gases hit the water during their rise towards the surface, they will be more or less scrubbed. Depending on the chemical equilibria inside the magmatic-hydrothermal system (e.g. SO 2 -H 2 S conversion, acidity), the gas that eventually reaches the surface will carry the history of its rise from bottom to top. Tracking volcanic unrest implies a time frame; the kinetics of magma degassing throughout the liquid cocktail inside the volcano impose the maximum resolution the volcano provides and hence the monitoring time window to be adopted for each volcano. Gas-dominated systems are "faster" and require a higher monitoring frequency, water-dominated systems are slower and require a lower monitoring frequency. ResumenEl calor y gas liberados por la desgasificación del magma afecta los acuíferos de origen predominantemente meteórico para formar sistemas magmático-hidrotermales dentro el cuerpo sólido del volcán. Este capítulo revisa como la geoquímica de fluidos puede ayudar a trazar la evolución a través de las varias etapas de "unrest" volcánico. Una visión directa dentro de un magma en desgasificación es solo posible para volcanes de conducto abierto. Sin embargo, en la mayoría de las situaciones el gas queda atrapado (i.e. "scrubbing") en el agua, que conduce a la pérdida de la señal pura que el magma idealmente puede proporcionar. Descifrar como el magma sube a través de los líquidos, y reacciona y re-equilibra con ellos dentro el sistema magmático-hidrotermal, en un marco de tiempo y espacio, es la única manera para rastrear el origen de la señal del magma. La desgasificación de magma se da por cuatro procesos: (1) durante la subida de magma, (2) por la descompresión debido al eliminar una porción del edificio volcánico, (3) debido a la convección interna dentro la cámara magmática, o (4) después de "ebullición secundaria" siguiendo el enfriamiento y consecuente cristalización. Las especies gaseosas magmáti-cas más indicativas (CO 2 , ...

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“…These variations in hydraulic regime in a volcano can be detected through self potential, microgravity, resistivity or VLF surveys (Finizola et al 2003;Révil et al 2004;Zlotnicki et al 2006;Gottsmann et al 2007;Fournier et al 2009;Villasante-Marcos et al 2014). Water level gauging in wells or flow rate measurements from (thermal) springs at volcano flanks is the most direct way, although few examples of frequent monitoring exist (Ingebritsen et al 2001;Hurwitz et al 2002;Taran and Peiffer 2009), which inevitably leads to the need for numerical modeling procedures to increase theoretical insights (Hurwitz et al 2003;Todesco and Berrino 2005). …”

Section: Effusive Eruptive Unrestmentioning

confidence: 99%

Recognizing and tracking volcanic hazards related to non-magmatic unrest: a review

et al. 2014

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Eruption forecasting is a major goal in volcanology. Logically, but unfortunately, forecasting hazards related to non-magmatic unrest is too often overshadowed by eruption forecasting, although many volcanoes often pass through states of non-eruptive and non-magmatic unrest for various and prolonged periods of time. Volcanic hazards related to non-magmatic unrest can be highly violent and/or destructive (e.g., phreatic eruptions, secondary lahars), can lead into magmatic and eventually eruptive unrest, and can be more difficult to forecast than magmatic unrest, for various reasons. The duration of a state of non-magmatic unrest and the cause, type and locus of hazardous events can be highly variable. Moreover, non-magmatic hazards can be related to factors external to the volcano (e.g., climate, earthquake). So far, monitoring networks are often limited to the usual seismic-ground deformation-gas network, whereas recognizing indicators for non-magmatic unrest requires additional approaches. In this study we summarize non-magmatic unrest processes and potential indicators for related hazards. We propose an event-tree to classify non-magmatic unrest, which aims to cover all major hazardous outcomes. This structure could become useful for future probabilistic non-magmatic hazard assessments, and might reveal clues for future monitoring strategies.

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Time-variation of hydrothermal discharge at selected sites in the western United States: implications for monitoring

Cited by 78 publications

References 52 publications

Regional crustal-scale structures as conduits for deep geothermal upflow

Regional crustal-scale structures as conduits for deep geothermal upflow

Fluid Geochemistry and Volcanic Unrest: Dissolving the Haze in Time and Space

Recognizing and tracking volcanic hazards related to non-magmatic unrest: a review

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