Solute fluxes and geothermal potential of Tacaná volcano-hydrothermal system, Mexico–Guatemala

Collard, Nathalie; Taran, Yuri; Peiffer, Loïc; Campion, Robin; Paz, Mariana Patricia Jácome

doi:10.1016/j.jvolgeores.2014.10.012

Cited by 10 publications

(11 citation statements)

References 21 publications

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“…a relatively high flux), the total volume of the various thermal aquifers feeding the springs in the study area is in the order of ~5x10 7 -10 8 m 3 (or ~5x10 10 -10 11 L). This aquifer volume is consistent with low porosity volcanic deposits of 5% et al 1992;Taran and Peiffer 2009), an order of magnitude higher than for Tacaná volcano (Collard et al 2014(Collard et al , 2020, but an order of magnitude lower than for the extremely high energy output of Domuyo volcano (Chiodini et al 2014).…”

Section: Water Mass Budget For Thermal Springssupporting

confidence: 68%

“…Qr*Cr = Qs*Cs 2where Qr and Qs are the discharges of rivers and thermal springs, respectively (in L/s); and Cr and Cs are the Cl or SO4 concentrations of rivers and thermal spring waters, respectively (in mg/L). This approach is based on the Cl-inventory method (Ingebritsen et al 2001;Taran and Peiffer 2009;Chiodini et al 2014;Collard et al 2014;Rouwet et al 2014a). Sulphate is used here, instead of the more conservative Cl, because the generally low concentrations of Cl could introduce a high error in the flux estimates.…”

Section: Water Mass Budget For Thermal Springsmentioning

confidence: 99%

“…The residence time given by Rowe et al (1995) and Sanford et al (1995) 5) (Collard et al 2014(Collard et al , 2020; and references therein). Unsurprisingly, the San Cayetano spring exhibits an energy output of 83.9 ± 16.8 MW, corresponding to 76.4% of the total energy output of nearly 110 ± 22 MW for the entire Irazú-Turrialba spring system (Table 5).…”

Section: Mineral Solubility and Geothermometrymentioning

confidence: 99%

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Response of a Hydrothermal System to Escalating Phreatic Unrest the Case of Turrialba and Irazú in Costa Rica (2007-2012)

Rouwet¹,

Mora‐Amador

Ramı́rez³

et al. 2021

Preprint

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This study presents the first hydrogeochemical model of the hydrothermal systems of Turrialba and Irazú volcanoes in central Costa Rica, manifested as thermal springs, summit crater lakes, and fumarolic degassing at both volcanoes. Our period of observations (2007-2012) coincides with the pre- and early syn-phreatic eruption stages of Turrialba volcano that resumed volcanic unrest since 2004, after almost 140 years of quiescence. Peculiarly, the generally stable Irazú crater lake dropped its level during this reawakening of Turrialba. The isotopic composition of discharged fluids reveals the Caribbean meteoric origin; a contribution of “andesitic water” for Turrialba fumaroles up to ~50% is suggested. Four groups of thermal springs drain the northern flanks of Turrialba and Irazú volcanoes into two main rivers. Río Sucio (i.e. “dirty river”) is a major rock remover on the North flank of Irazú, mainly fed by the San Cayetano spring group. Instead, one group of thermal springs discharges towards the south of Irazú. All thermal spring waters are of SO4-type (i.e. steam heated waters), although none of the springs has a common hydrothermal end-member. A water mass budget for thermal springs results in an estimated total output flux of 187 ± 37 L/s, with 100 ± 20 L/s accounted for by the San Cayetano springs. Thermal energy release is estimated at 110 ± 22 MW (83.9 ± 16.8 MW by San Cayetano), whereas the total rock mass removal rate by chemical leaching is ~3,000 m3/y (~2,400 m3/y by San Cayetano-Río Sucio). Despite Irazú being the currently less active volcano, it is a highly efficient rock remover, which, on the long term can have effects on the stability of the volcanic edifice with potentially hazardous consequences (e.g. flank collapse, phreatic eruptions). Moreover, the vapor output flux from the Turrialba fumaroles after the onset of phreatic eruptions on 5 January 2010 showed an increase of at least ~260 L/s above pre-eruptive background fumarolic vapor fluxes. This extra vapor loss implies that the drying of the summit hydrothermal system of Turrialba could tap deeper than previously thought, and could explain the coincidental disappearance of Irazú’s crater lake in April 2010.

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Section: Water Mass Budget For Thermal Springssupporting

confidence: 68%

Section: Water Mass Budget For Thermal Springsmentioning

confidence: 99%

Section: Mineral Solubility and Geothermometrymentioning

confidence: 99%

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Response of a Hydrothermal System to Escalating Phreatic Unrest the Case of Turrialba and Irazú in Costa Rica (2007-2012)

Rouwet¹,

Mora‐Amador

Ramı́rez³

et al. 2021

Preprint

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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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