The layered model of the Copahue geothermal reservoir, Argentina
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An exhaustive review of the available data related to the reservoir of the volcano-hosted Copahue geothermal system is presented. Reservoir interpretation to date suggests a vapor-dominated nature. However, the review provided reveals the limitations of this model, regarding the transition from shallow argillic to deep propylitic alteration zones, gas geothermometers calibrated to near-neutral pH environment, production tests, and low recharge of the feed zone, among the other features. We propose that a layered model with a shallow vapor zone above a fluid pressurized reservoir better accounts for the known features of the geothermal reservoir. Temperature profiles define the 800-m-thick upper thermal boundary that includes the impermeable clay cap. An argillic alteration layer (smectite + chlorite + illite + kaolinite) with low electric resistivity response, consistent with the presence of smectite, composes the clay cap. A shallow steam cap develops immediately below the impermeable layer. This vapor zone has 200–215 °C, low seismic activity, and high electrical resistivity, and is highlighted by the isothermal segment of the well logs. The bottom part of the reservoir is subjected to controversy because of the lack of direct measurements. The deep liquid-dominated reservoir has a temperature of ~ 280 °C, develops below 1500 m depth under near-neutral pH condition, and probably has a pervasive propylitic alteration, and wairakite + laumontite + chlorite + epidote + prehnite + actinolite is the likely mineral assemblage. Pressure collapse might trigger the development of the shallow steam cap during deflation–inflation volcanic cycles or Pleistocene-to-recent tectonic deformation. This work points out the main weak points of the previous conceptual model, providing an alternative one based on the first comprehensive compilation of data of the Copahue reservoir. Further research, including a deep exploration drilling stage, is required to establish the physicochemical reservoir state precisely and to validate the proposed layered model.
KeywordsCopahue geothermal field Geothermal reservoir Exploration Vapor-dominated Liquid-dominated
The definition of a conceptual model is essential during the feasibility stage of a geothermal project, given that it drives both surficial and underground exploration, constraining the inferences about the reservoir nature. Geothermal reservoirs are commonly classified as liquid- or vapor-dominated, based on the mobile phase. A reservoir steam fraction of 1 defines a vapor-dominated system, whereas a steam fraction from 1 to 0 defines a two-phase, liquid-dominated system. Each reservoir-type develops at different tectonic settings and shows different surficial manifestations, deep geological structures, and permeability conditions. These features, in turn, define the geometry of the system (e.g., Jolie et al. 2015; Moeck 2014, Stelling et al. 2016). Vapor-dominated systems display greater geothermal potential and have significant engineering benefits over liquid-dominated ones. They require about a third of the mass flow rate to achieve the same power output of a power plant, accessing a two-phase reservoir at the same conditions of temperature and pressure (Zarrouk and Moon 2014; Dipippo 2016). Therefore, the reservoir conceptual model has to be carefully analyzed to avoid incorrect planning of the deep-drilling stage, inaccurate assessment of the resource, and to perform better risk and financial models to prevent a delay or cancelation of the project.
The Copahue volcano is part of the Southern Volcanic Zone. It is located at a latitude of 37.8°S at the Argentina–Chile border, a region with a complex tectonic setting (Zapata et al. 1999; Ramos and Folguera 2005; Cembrano and Lara 2009; Pérez-Flores et al. 2016). The volcano has shown intense activity for the last 250 years (Delpino and Bermúdez 1993, 2002; Naranjo and Polanco 2004; Petrinovic et al. 2014; Caselli et al. 2015; Folguera et al. 2016). Its northeastern flank hosts several fumaroles that define the Copahue geothermal field. This area was the target of the most advanced Argentinean geothermal project to date (Pesce 1989; JICA 1992; Fig. 1b, c). After the start of production, the discharge of dry steam suggested that the system was vapor-dominated (Nakanishi et al. 1995). Numerous works have assumed the vapor-dominated nature for the reservoir at the Copahue geothermal system (e.g., Nakanishi et al. 1995; Chiodini et al. 2015; Lundgren et al. 2017). However, a complete review of available data is needed to assess this hypothesis adequately.
This study aims to analyze the available data of the Copahue geothermal reservoir, testing the current conceptual model nature. To reach these goals, we performed an analysis of the geologic and tectonic setting, pressure and temperature profiles, geothermal manifestations and hydrothermal alteration, and fluid geochemistry, together with an evaluation of the production history of Copahue project. Finally, we propose a 1D layered conceptual model of the volcano-hosted geothermal reservoir.
The pressure-depth profiles
A typical feature of the vapor-dominated systems is the low pressure of the reservoir respective to the surrounding because of the lower weight of the vapor column in comparison with the hydrostatic column (White et al. 1971). On the other hand, liquid-dominated reservoirs have the typical pressure profile with an almost hydrostatic gradient. Thus, a general overview of the pressure vs. depth paths is useful for comparison between Copahue and the rest of the vapor-dominated reservoirs.
It is interesting to note that all the volcano-hosted vapor-dominated reservoirs show the same three-segment pattern in the pressure vs. depth curve. The shallow segment has a high-pressure gradient in response to a hydrostatic column. The intermediate segment shows a slow pressure gradient indicating two-phase or single vapor-phase conditions. The bottom segment has a hydrostatic pattern that highlights the presence of the deeper liquid-dominated reservoir.
It is interesting to highlight that the very low-pressure gradient found along the shallow section of Copahue wells is a rare feature. Several numerical simulations performed by Pratama and Saptadji (2016) based on a two-phase liquid-dominated geothermal reservoir with a steam cap underlying brine reservoir model permits a sound interpretation. Such models reveal that pressure in boiling zones increases slightly until the main deep reservoir level, where the gradient turns to hydrostatic conditions, like a conventional liquid-dominated reservoir. In addition, the pressure profile differs from the center to the edge of the models. These differences should be taken into account to interpret the pressure profiles at the Copahue reservoir correctly.
Copahue wells show a dramatic pressure gradient increase from 900 m downward, adopting an almost hydrostatic behavior (Fig. 3). There are several explanations for this response, including a feed zone, condensation of steam, and accumulation in a dead leg or an artifact by the configuration of the casing and perforated liner. Another explanation might be the existence of a water level near the well bottom. In any case, if this trend is confirmed, the pressure profile would agree with a shallow vapor zone underlying a deeper two-phase reservoir.
The rare occurrence of vapor-dominated reservoirs contrasts with the frequent presence of steam caps or vapor zones above liquid-dominated reservoirs (Raharjo et al. 2016). Moreover, the formation of the steam caps is common in volcano-hosted liquid-domain reservoirs. Good examples of these local vapor zones at volcano-hosted systems are found at Ahuachapan in El Salvador (Monterrosa and López 2010), Monte Aso in Japan (Shibuya et al. 2000; Terada and Sudo 2012), or Tolhuaca in the compressive volcanic arc of Chile (Melosh et al. 2012; Iriarte 2013), among others. All these cases are probably related to deep feed zones that subject the reservoir to a local increase of permeability and heat flux. In exceptional cases, such as of the Te Mihi at the Wairakei geothermal system, the production forces a pressure drop and led to the formation of a significantly productive vapor zone from a liquid-dominated reservoir (Thain and Carey 2009). In addition, the development of vapor zones could be overlaid by shallow steam-heated waters, so a sealed upper boundary may not be essential (Ingebritsen and Sorey 1988; Hochstein and Sudarman 2000). This setting is consistent with the isotopic signature of the fumaroles at the western margin of the Copahue reservoir given the interaction inferred between deep geothermal fluids and the shallow steam-heated water table (Chiodini et al. 2015; Roulleau et al. 2016).
Surface geothermal manifestations: the high-sulfidation system
The development of a vapor-dominated reservoir is commonly related to a pressure drop over a deep liquid-dominated reservoir and responds to a couple of input–output constraints. The first one is that the recharge must be slow enough to boil. Otherwise, the vapor zone would be flooded with liquid (Raharjo 2012). The second one is the existence of surface leaks that allow the steam cap growth with time (White et al. 1971). If not, the system would pressurize, slowing or stopping evaporation from the underlying boiling brine. Hydrothermally altered soils, fumaroles, and hot springs are evidences of these fluid leaks. Therefore, they can be used to infer the physicochemical conditions at depth.
Mas et al. (1996) studied the altered soils at local depressions originated by strong pervasive alteration of the country rock. There are composed of alunite–kaolinite bearing assemblage with subordinated cristobalite, quartz, and cryptocrystalline jarosite, depending on the alteration degree (Fig. 4; Mas et al. 1996). This type of hydrothermal alteration currently develops at vents of active volcanoes where magmatic gases as SO2 and HCl occur at high concentrations (White and Hedenquist 1995). Therefore, aluminous-rich hydrothermal alteration assemblage related to the Copahue surficial manifestations is also of high-sulfidation type. Numerous works have demonstrated the existing relationship between sulfidation degree of epithermal systems and geothermal reservoirs (e.g., Henley and Ellis 1983; Henley et al. 1986; Hedenquist et al. 1992; Corbett and Leach 1993). While liquid-dominated reservoirs are related to low sulfidation assemblage, vapor-dominated ones are related to high-sulfidation assemblage. Unfortunately, the surface hydrothermal manifestations are not conclusive given that liquid-dominated reservoirs can develop high-sulfidation alteration, including alunite–kaolinite bearing soils, when related to shallow steam zones (e.g., González-Partida et al. 2005).
Several geothermal systems at a wide range of tectonic settings have a shallow steam-heated boiling aquifer overlying a pressurized liquid reservoir (e.g., Palinpinon at Philippines, Los Azufres at Mexico or Olkaria at Kenia; Grant and Bixley 2011), and the volcanic-hosted reservoir is not the exception (Tiwi at Philippines or Matsukawa at Japan; Gambill and Beraquit 1993; Hanano and Matsuo 1990). These steam-heated acid sulfate springs usually develop the advanced argillic assemblages composed by opal + alunite + kaolinite + pyrite (Pirajno 2009), as the alteration showed by the soils of Copahue (Fig. 4). Therefore, hydrothermal alteration above a vapor-dominated geothermal reservoir is similar to that found in local shallow, steam-heated zones above a boiling liquid-dominated reservoir (Boden 2016).
A thorough analysis of the alteration mineralogy shown in Fig. 5 reveals a complex hydrothermal alteration history. The coexistence of chloride with smectite, chloride–smectite, and Ca–zeolites may be explained by the over imposition of more than one hydrothermal alteration event. The lack of textural characteristics of the mineralogical assemblage obscures the thermal-alteration path. Unfortunately, no textural analysis is available, so it is impossible to clarify the thermal-alteration path. However, hand specimen studies, petrography, and the X-ray diffraction observations allowed. Mas et al. (1995) to define three partially overlapped Ca–zeolites zonations, consistent with changes in the thermal structure of the reservoir.
There is an approximate correspondence between the area of the geothermal field, the surficial heat flux, and the type of geothermal system. In the Larderello geothermal system, for example, the heat flow is about ~ 0.5 MWkm−2 over more than 70 km2 (Bellani et al. 2004, Della Vedova et al. 2008). On the other hand, values from 4 MWkm−2 until 12 MWkm−2 over more than 15 km2 are needed to explain the current state of the vapor-dominated systems of Kamojang and Darajat (Raharjo 2012, Raharjo et al. 2016). Allis (2000) analyzed the thermal regime over both intrusion-hosted and volcano-hosted vapor-dominated systems. He concluded that while the former is characterized by 1 MWkm−2 heat flow, the latter shows typical values around 10 MWkm−2 but with smaller reservoir areas (~ 10 km2). These features partially contrast with the proposed heat flow for Copahue. A surface heat flow of 0.3 MWkm−2 over an area of 20 km2 was calculated based on gradient well measures reported by Mas et al. (2000). Although these values reflect a relatively large heat source, they are still lower than previously described for entirely volcano-hosted vapor-dominated systems.
Redox condition of the geothermal reservoir by fluid geochemistry
It is known that fumaroles and fluids from wells play an essential role in the study of the physicochemical conditions of deep reservoirs. That is because of the equilibrium reaction velocities involved in the fluids’ host-rock system (Nicholson 1993; Arnórsson 2000). In contrast to high-velocity reactions, low-velocity reactions imply a lower chance of chemical re-equilibration at shallower levels during the upwelling of the geothermal fluids. Therefore, it is possible to infer different processes and physicochemical characteristics at a wide range of depth levels by studying the developed chemical systems with their respective reactions velocities.
Agusto et al. (2013) have previously studied the deep processes using the CO2–CH4 bearing system, which is less susceptible to re-equilibrate at shallow depths (Giggenbach 1991). These authors found that overheated fluids at Copahue dominate the vapor-single phase when they are analyzed regarding the DP buffer system (Fig. 7c). This overheated state suggests that the system is not in equilibrium and that more reducing conditions are needed to explain the chemical data. However, Fig. 7d reveals that the Copahue geothermal fluids tend towards equilibrium in the liquid phase field at a temperature range of 250–290 °C (Agusto et al. 2013), regarding neutral or slight reductive conditions with the FeO–FeO1.5 pair as the dominant redox buffer system. The estimated temperature range is consistent with the direct measures available (see Fig. 3) and corresponds to a near-neutral pH liquid-dominated reservoir.
The existence of slight reducing to neutral conditions in the reservoir is in agreement with the alteration mineralogy identified at the bottom wells (Fig. 5). Besides, a zonation of stilbite, laumontite, and wairakite was identified, and the existence of Ca-bearing zeolites supports both slightly alkaline conditions and the fact that XCO2 is low enough to stabilize Ca–Al silicates (Mas et al. 1995). This mineral alteration assemblage differs from the vapor-dominated or steam-heated alteration above a boiling liquid-dominated reservoir because of the highly acid alteration assemblage of the host rock (Boden 2016).
Well-production data and the vapor zone
The deep-drilling exploration stage at Copahue was carried out during several on and off stages between 1976 and 1991, and leads to perform production tests over a total of three exploratory wells. The static column of steam with only vapor-phase discharge is the main characteristic of the vapor-dominated reservoirs. After the exploratory wells at Copahue were opened, the main discharge was dry steam, and the results led to Nakanishi et al. (1995) to propose the vapor-dominated nature of this geothermal system. Although the unpublished feasibility report performed by JICA (1992) is consistent with this assumption, an additional information should be considered.
The isotopic composition of the fluids during the production test was tracked at both wells to understand the fluid source and its relation with the host rock. Panarello (2002) identified the depletion of δ18O and inferred that the shallow feed zone has a low permeability connection with the deeper liquid-dominated reservoir, suggesting that there is no lateral recharge. Both the fluid discharge and the isotopic evolution indicate the existence of an isolated shallow steam cap, at least located around the vicinity of the drilled wells (i.e., Las Mellizas Lake). A third exploration well was subjected to a short production test for only 16 days. Despite no discharge depletion having been identified, JICA (1992) pointed out that the steam discharge was not a consequence of extensive flow testing and suggested the possibility that similar behavior should be expected if the tests continued over time. The data reviewed so far indicate a) the existence of a nonproductive shallow steam cap, and b) that the main reservoir could not have been reached by the wells.
The layered model of the Copahue geothermal reservoir
As shown in Fig. 10, the conductive temperature vs. depth profile develops an upper thermal boundary, which corresponds with the Las Mellizas Formation. A constitutive part of this layer is the clay cap, composed of smectite + chlorite + illite + kaolinite alteration mineral assemblage. The clay cap is characterized by both a resistivity structure of ~ 10 Ω.m and a very low magnitude and density of the seismic events (JICA 1992; Lazo et al. 2015; Lundgren et al. 2017), and is part of the stilbite zeolite zone of Mas et al. (1995). The existence of this low permeability layer correlates with the identified acid argillic alteration zone. Temperature profiles indicate that the bottom of the thermal boundary is placed at 800 m depth, highlighting the efficiency of the well-developed clay cap (Fig. 10). Despite the relevance of the magnetotelluric surveys to define the clay cap extension and thickness (Gunderson et al. 2000; Cumming and Mackie 2007; Heise et al. 2008), the available data from Mamani et al. (2000) and Borzotta et al. (2018) were ruled out because of the low quality of the signal and the inadequate distance between the measured stations.
Immediately below the clay cap, there is a shallow steam cap that is identified in the well log by the isothermal segment (Sierra et al. 1992; Nakanishi et al. 1995). This vapor zone is hosted in the bottom of Las Mellizas Formation, showing poor seismic activity and low electric conductivity response (~ 120 Ω.m), in agreement with the lack of smectite (see the temperature profile and both the geoelectric and mineral alteration column in Fig. 10). Gas geothermometers based on the high-velocity re-equilibration system indicate a temperature of 200–215 °C for this shallow vapor reservoir, consistent with direct borehole measurements (JICA 1992; Agusto et al. 2013; Chiodini et al. 2015). The production data reported by Sierra et al. (1992) and isotopic abundances analysis performed by Panarello (2002) are in good agreement with an isolated and nonproductive zone, at least around the volume influenced by the wells. In addition, the presence of kaolinite at the top of this shallow steam cap suggests that it was formed by the interaction between the boiling zone and the host rock. A feasible explanation for the development of this shallow steam cap might be that a high permeability zone would have promoted a depressurization of the thermal fluids. Production data suggest that the feed zone reached by the exploration wells is the top of the shallow steam cap (Panarello 2002).
The physicochemical condition of a deep reservoir below the steam cap is the main discussion point. Despite some slight contradictions between the report of JICA (1992), Sierra et al. (1992), and Panarello (2002), our fluid chemical analysis approach (“Redox condition of the geothermal reservoir by fluid geochemistry” section) suggests the presence of a two-phase reservoir at depth. Recalibration of the CO2–CH4-bearing system at neutral-to-alkali reservoir conditions showed that the fluids are not equilibrated at vapor-saturated conditions (Agusto et al. 2013). It is possible, therefore, that a liquid phase might dominate the geothermal reservoir at Copahue. The boiling and steam separation model that explains the Xe increase and the constant R/Ra at the fumaroles (Roulleau et al. 2016) reinforces that hypothesis. The exploratory wells reached the base of the clay cap and likely hit near the top of this reservoir, located at 1100–1200 m depth (Fig. 10). Although biased measurements should not be ruled out, rapid pressure gradient rise at the bottom of the profiles might be responding to a hydrostatic column, thus suggesting a two-phase, transitional zone fed by the deeper reservoir. This zone correlates with an increase in the recorded seismic activity related to fluid pore pressure rise, and with the presence of wairakite, laumontite, and epidote as main alteration minerals (see seismic volcano-tectonic activity and mineral alteration assemblage columns in Fig. 10).
We propose that a liquid-dominated system composes the lower part of this system, probably below 1500 m depth. The more reliable gas geothermometer (log(XCH4/CH2O) vs. log(XCO2/XH2O); Agusto et al. 2013) indicates a temperature of 270–280 °C and near-neutral pH conditions. Homogenization temperatures of fluid inclusions found in quartz from cutting samples (Mas et al. 1993) are consistent with the gas geothermometers. A pervasive propylitic alteration affects the Cola de Zorro-Hualcupén Formation that host the reservoir. The likely mineral assemblage is wairakite + laumontite + chlorite + epidote + prehnite + actinolite. Coexistence of wairakite and actinolite suggests good permeability and temperature up to 280 °C. This mineral assemblage is partially recognized in the COP-3 well (see Fig. 5).
Since no direct measurements were taken, the thickness of the liquid-dominated reservoir will remain under debate; however, seismic activity registered at the volcano-hydrothermal system provides some clues. The first hypocenter distribution of the volcano-tectonic earthquakes at Copahue was presented by Lazo et al. (2015), based on the collected database from OVDAS. A curious aspect of the data is a seismic gap at 3 km depth that could be constraining the bottom of the reservoir. The main problem is the large vertical error bars (0.6 km) of the hypocenter locations. Velez et al. (2011), in turn, proposed a carapace zone (i.e., a strong permeability reduction below a shear-ductile zone) at 2 km depth as the bottom of the deep reservoir. Nevertheless, Lundgren et al. (2017) question the carapace boundary and, based on an enhanced seismic catalog, showed that the seismic gap does not exist. Conversely, the authors identified a decrease of the seismic activity below 4 km depth, interpreted as the fragile–ductile transition zone controlled by the magmatic heat source.
The mechanism for the development of the volcano-hosted vapor-dominated reservoir is still not fully understood. Since the first model proposed by White et al. (1971), several numerical models have demonstrated that this kind of system evolves from liquid-dominated reservoirs by a drop in the pressure; other complex constraints, like permeability boundaries to heat source and input–output balance, could also be influential (Faust and Mercer 1979; Preuss 1985; Ingebritsen and Sorey 1988; Norton and Hulen 2001; Raharjo et al. 2016). For instance, Allis and Shook (1999) showed that tectonic activity at The Geysers was capable of forming vapor-dominated reservoirs from liquid-pressurized conditions by a uniaxial extension below 1 km depth. In the case of Copahue, a multi-episodic magmatic injection and its effect on fracture-related permeability might contribute to the steam cap development. InSAR satellite data allowed to identify inflation–deflation cycles related to the volcanic activity at Copahue (Velez et al. 2011, 2016; Lundgren et al. 2017). It is expected that the connectivity of the fracture network will be enhanced in the host rock after each magmatic-related deformation cycle, hence, favoring the permeability and decreasing the local pressure.
The fluid chemistry at vents of the Copahue volcano also reflects the link between deformation processes and permeability enhancement because of a straighter fluid path from the deep source to the surface (Agusto et al. 2012a, b, 2018; Tassi et al. 2017). Morphostructural and volcanic landscape evolution provide further explanations. Moore et al. (2008) speculated based on petrologic evidence that catastrophic pressure reduction related to volcanic flank failure may have triggered the vapor zone at the Telaga Bodas geothermal system. In the case of Copahue, its northeastern flank is structurally controlled showing an NE-trending collapse with the associated eruptive deposits. The lack of precise radiometric dating of those deposits prevents dating this deformation episode, but the collapse of the northeastern flank of the volcano as the trigger for the current geothermal field development should not be ruled out. Additional studies are required to understand the relationship between the volcanic activity and the structurally controlled high permeability zone. This relationship is crucial to assess the evolution of the layered reservoir of the Copahue geothermal system. Further thermomechanical and petrophysical models linked to the fluid geochemical database could assess the effects of the Copahue volcano activity with transient changes at the layered geothermal reservoir.
The present work aimed to examine the available data of the Copahue geothermal field to understand the critical aspects of its reservoir and obtain a reliable conceptual model. Different sources of information, like high-sulfidation hydrothermal zones, lack of silica sinters and chloride hot springs, a first vapor-single-phase discharge at the exploration wells and results of chemical analysis, lead to several authors to interpret a vapor-dominated reservoir for Copahue geothermal system (Sierra et al. 1992; JICA 1992; Nakanishi et al. 1995; Chiodini et al. 2015). However, this outcome is contrary to the other lines of evidence, like the transition from shallow argillic to deep propylitic alteration zones, gas geothermometers calibrated to near-neutral pH environment, pressure profiles, and dry vapor declination until the feed zone becomes exhausted and low recharge of the feed zone, among others. Nevertheless, described features are consistent with a configuration where a shallow vapor zone caps a deep reservoir driven by a pressurized fluid.
The upper thermal boundary of the reservoir extends until 800 m depth, including the impermeable clay cap; the available temperature profiles clearly define it.
The clay cap is characterized by argillic alteration of the andesitic lavas of Las Mellizas Formation, in good agreement with the stilbite zone of Mas et al. (1995). Its low electric resistivity is consistent with the presence of smectite. It is mandatory to perform a magnetotelluric survey to define the extension of this layer.
We suggest the existence of a shallow steam cap immediately below the clay cap, based on the isolated and nonproductive behavior of this reservoir. This vapor zone has 200–215 °C, low seismic activity, and high electrical resistivity, and is highlighted by the isothermal profiles at the well logs (JICA 1992; Agusto et al. 2013).
The lower part of the reservoir is subject to controversy because of the lack of direct measurements.
A transition between the steam cap and a liquid-dominated reservoir might lead to a two-phase reservoir, although its development also depends on the permeability of the host rock, among other constraints.
We propose a deep liquid-dominated reservoir develops below 1500 m depth, with a temperature of ~ 280 °C and near-neutral pH condition. This reservoir develops at the Cola de Zorro-Hualcupén Formation, has a pervasive propylitic alteration, and the wairakite + laumontite + chlorite + epidote + prehnite + actinolite is the likely mineral assemblage (JICA 1992). Although geochemical and production data support the assumption of a deep brine level below the upper steam cap, there is no reliable evidence (e.g., direct data) of its existence at the moment.
The shallow steam zone development is likely consequence of a drastic decrease in pressure. This pressure drop could respond to a permeability enhancement during deflation–inflation cycles, and/or to Pleistocene-to-present tectonic deformation that leads to the collapse of the northeastern flank of the volcano.
Transient changes of the reservoir layering would be expected given, its direct interaction between the volcanic dynamics, and the hydrothermal–geothermal system.
This work contributes to the existing knowledge of the geothermal resource at Copahue by providing a revision and integrating the available information in a single conceptual model of the reservoir. Although the existence of a deep liquid-dominated reservoir is consistent with the available data, more work involving new deep wells is needed to constrain its physicochemical conditions better.
HB was the major contributor in analyzing and writing the manuscript. DY improved several geothermal interpretations and the manuscript. MA analyzed the chemical data. All authors read and approved the final manuscript.
The authors declare that they have no competing interests.
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