- Open Access
Groundwater age and hydrothermalism of confined aquifers in the Argentine Pampean plain
© The Author(s) 2017
- Received: 10 August 2016
- Accepted: 7 June 2017
- Published: 13 June 2017
The Pampean plain of Cordoba province (Argentina) has hydrothermal manifestations linked to Cretaceous depocenters. However, they are in general neither well known nor carefully used, and, in numerous cases, they are unjustifiably wasted. The objective of this work is to show the most outstanding hydrogeological features and the geologic setting that control the low enthalpy hydrothermal deep systems and groundwater age in the Pampean plain of Cordoba province. To perform the study, conventional geological and hydrogeological methodologies were used. Isotopic (18O, 2H, 3H, 13C and 14C) and geochemical studies (Cl–SO4–HCO3 and Na–K–Mg ternary diagrams) were made to evaluate groundwater age and hydraulic and geochemical features of the aquifer system. The confined aquifer systems (CASs), located at 120–350 m depth, are multilayered and linked to fluvial Neogene paleosystems. The isotopic analysis for these hydrothermal systems shows that groundwater is not related to magmatic waters and it has a meteoric origin being recharged in the mountain and piedmont western areas (Comechingones Mountains). The 14C ages obtained for A1 and A2 CASs indicate waters recharged during Holocene cold periods, between the “Little Ice Age” and the ending of “Holocene Climatic Optimum,” and during the last glaciation, respectively. The groundwater temperatures in the discharge points are between 24 and 38 °C, which exceeds 4–12 °C the expected value for that depth, if normal gradients are considered. The analysis using geothermometers showed that the groundwater samples were located in the immature water field near the boundary of the partially equilibrated waters. The thermal anomaly is linked to the Cretaceous depocenters of General Levalle, especially associated to the low block of the Tigre Muerto regional fault. This geothermal anomaly shows agreement with the regional geotectonic setting and it should be the result of the continental crustal thinning and the geological regional faults that make easy groundwater circulation to several depths. The groundwater flowing from recharge areas, favored by the structure of dipping regional blocks, would be reached higher temperatures (the order of 79 °C) explaining the present oversaturation in SiO2, what implies maximum depths of up to 1500 m and the observed thermodynamic behavior of such mineralogical phases. This general framework is in agreement with the Cl–SO4–HCO3 ternary diagram which indicates steam-heated waters.
- Groundwater age
- Confined aquifer
- Cretaceous depocenters
In the twentieth century, high-temperature water resources have been used for the production of electricity, whereas medium and low temperature resources are used for domestic heating, from individual houses to whole communities, as well as for balneology, industrial, and agricultural purposes (Albu et al. 1997; Stober and Bucher 2013). The utilization of geothermal energy provides an opportunity to decrease the dependency on fossil sources of energy. The substitution of fossil-fired installations leads to a reduction of CO2 emission and decreases climatic warming. The task to assess a geothermal energy potential includes geological, hydrological, technological, infrastructural, economical, and ecological investigations. In this sense, the basic hydrogeological studies in a geological basin are essential due to knowledge requirements about the spatial distribution of aquifer layers and groundwater flow, age and geochemistry, to have data for a sustainable management of such an important resource. For this reason, all around the world scientists are investigating thermal waters (Albu et al. 1997; Stober and Bucher 2013; Vasilyev et al. 2016).
Numerous hydrothermal manifestations were identified in Argentina (Pesce 2008). In Cordoba province, according to Cabrera et al. (2012a, b), Chiodi et al. (2014), and Blarasin et al. (2014), the most important manifestations are located in the area of Sierras Chicas Mountains (near Villa Giardino and Capilla del Monte towns), in Traslasierra area (near El Quicho, Serrezuela, and Piedrita Blanca towns) and in the east plain of Cordoba province (San Basilio, General Soler, and La Carlota towns, among others). All of them are low enthalpy geothermal systems. In the large plain of the South of Cordoba province, these systems are associated to a Cretaceous depocenter. The geological framework is supported by several geological and geophysical data, especially those resulting from oil and mining explorations in Cordoba province, which enabled the researchers to obtain information about the geological characteristics up to 7000 m deep. It is worth highlighting the deep geological studies carried out during oil exploration in General Levalle area (Cordoba province) by the Argentine Geological and Mining Service (SEGEMAR) in agreement with the Australian Geological Service (Pieters and Skirrow 1997), Hunt Oil and YPF Company (Chebli et al. 1999; Webster et al. 2004; Reinante et al. 2014; Calegari et al. 2014; Sigismondi and Fantín 2014). Also, the results obtained by National Universities (Degiovanni et al. 2005; Rapela et al. 2007; Rapela and Baldo 2014) have been considered. In addition to the geological importance these thermal systems have, they represent great socio-economic potential resources that can be used either for tourism or some productive enterprises. However, they are in general neither well known nor carefully used, and in numerous cases, they are unjustifiably wasted (Cabrera et al. 2010; Blarasin et al. 2014). That is why conceptual hydrogeological models of these hydrothermal systems are needed, which can become the basis for their sustainable use.
Taking into account that the groundwater data will be useful for water managers that must carefully plan their use, the objective of the present work is to show the most outstanding hydrogeological features and the geological setting that controls the low enthalpy hydrothermal deep systems and groundwater age in the Argentinian Pampean plain.
The geological analysis was carried out at 1:100,000 scale on the basis of topographical charts from the National Geographic Institute (IGN) and satellite images (IGN and Google Earth). The deep geological framework interpretation (up to 7000 m deep) was carried out according to background regional studies in Córdoba province. Thus, the analyzed information corresponds to four deep wells which penetrated the sedimentary column and reached the bedrock: Ordoñez well (3402 m), Santiago Temple well (1100 m), Saira well (2700 m), and Camilo Aldao well (2300 m) (Rapela et al. 2007; Rapella and Baldo 2014).
Stratigraphic profile presented in the Río Cuarto Geological Worksheet (Degiovanni et al. 2005) was considered. The description of this profile was based in the results obtained by the Hunt Oil Company in Levalle area (Córdoba) where a deep well (5179 m) which did not reach the bedrock was drilled (Chebli et al. 1999; Webster et al. 2004; Reinante et al. 2014; Calegari et al. 2014; Sigismondi and Fantín 2014).
To improve the interpretation of the different aquifer levels, deep sediment profiles (up to 350 m) were assessed. The sediment samples obtained from drillings were treated and subjected to textural analysis. Then, stratigraphical correlations and paleoenvironmental regional interpretations were carried out. After that, hydraulic conductivity (K) values were estimated for the different sedimentary layers using empirical granulometric methods such as (a) Sheelheim equation, to estimate K with the average particle size (Schafmeister 2006); (b) Slichter equation, which base the calculus on 0.01–5 mm particle size (Pérez et al. 2014); and (c) Profile Sieve Percentage (PGP) (Pérez et al. 2014), which uses triangular diagrams based on the model proposed by the United States Department of Agriculture and considers both fine and coarse fractions. The results of these estimations were compared with K tables (Custodio and Llamas 1996) and background hydraulic tests data obtained by other authors in this region (Blarasin et al. 2014; Maldonado et al. 2016).
This hydrogeological study included geochemical and isotopic analysis of rainfall and of every hydrological system (surface water, such as streams and lagoons, and groundwater, i.e., unconfined and confined aquifers). Groundwater level depths were measured in the field by means of water level meters, using manometers in artesian wells. Water samples were taken following standard methods and water quality parameters such as electric conductivity (CE), pH, temperature, and dissolved oxygen (DO) were measured in situ. The selected samples belong to wells with short screen lengths (less than 10 m) so that they are considered adequate for the interpretation of groundwater behavior at different depths, preventing water mixtures from different aquifers.
Main dissolved ions (CO 3 −2 , HCO3 −, SO 4 −2 , Cl−, Na+, K+, Ca+2, Mg+2) were analyzed at the laboratory of the Geology Department at the National University of Río Cuarto, using standard methods (APHA, AWWA, and WPCF 2005). CO 3 −2 and HCO3 − through potentiometric titration with 0.01 N HCl using a Hanna pH-meter to indicate the end point. SO 4 −2 was measured by gravimetric method and Cl− by titration with a potassium chromate indicator and 0.01 N silver nitrate titrant solution to indicate the end point. Na+ and K+ were determined by the flame emission photometric method and Ca+2 and Mg+2 by titration with 0.02 N ethylenediamine tetra-acetic acid (ETAA) titrant solutions. The indicator for Ca+2 was NaOH and ammonium purpurate, and the indicators for Mg+2 were ammonia buffer solution and eriochrome. SiO2 and Li were analyzed by Perkin Elmer Sciex ELAN 9000 ICP/MS at the Activation Laboratory Ltda. (ActLab) in Canada. Samples were filtered with 45-micron filter and acidified prior analysis. Detection limit for Li was 1 µg/L and for Si 0.2 mg/L.
The stable isotopes (18O, 2H) and 3H were determined at the Institute of Geochronology and Isotopic Geology (INGEIS-CONICET-UBA), whereas 13C and 14C were carried out at the Environmental Isotopic Laboratory (uWEILAB) at the University of Waterloo in Canada. 18O and 2H analyses were performed by means of a “Off-axis integrated cavity Output Spectroscopy” (OICOS) (Lis et al. 2008) and DLT-100 liquid–water isotope analyzer from LGR inc. Results were expressed in the usual form i.e., δ (‰). Uncertainties are ±1‰ for δ2H and ±0.3‰ for δ18O, and reference standard is V-SMOW (Gonfiantini 1978).
In addition, selected wells were sampled for 3H and 14C determination, to obtain representative values of different aquifer systems. Samples were prepared following the laboratory instructions. Samples for 3H analysis were collected in 600-mL polyethylene bottles, while those for δ13C and 14C were collected in 150-ml polyethylene bottles. All the samples were shipped in ice coolers. The 3H was determined by liquid scintillation counting after electrolytic enrichment. The detection limit was of 0.8 ± 0.3 tritium units (TU). 14C and 13C samples were analyzed by an accelerator mass spectrometer (AMS). 14C results are expressed as percent of modern carbon (pmC) relative to the National Institute of Standards and Technology (NIST). 14C standard was SMR-4990C and normalized to δ13C −25‰. Reference standard for δ13C is V-PDB (Craig 1957), and the uncertainty is of ±0.2‰.
The analysis of radioactive isotopes for the different confined aquifers made it possible to estimate groundwater ages, which were later corrected by means of Tamers (1975) and Pearson-Gonfiantini (in Salem et al. 1980) methods. The first method considers a chemical correction of the initial activity (14A), and the second method involves chemical and isotope issues. The isotopic ages were checked with the hydraulic method estimation based on the groundwater flow velocity (using Darcy Law) and on the distance to the recharge perimountain area (Kazemi et al. 2006). To compare the estimated ages, other indirect methods were used such as stable isotopes values (δ2H and δ18O, Kazemi et al. 2006).
The chemical geothermometers have been used to estimate the subsurface temperatures of the geothermal fluids. The SiO2 (Fournier et al. 1974), Na/K and Na/K/Ca (Fournier and Truesdell 1973), Na/Li (Fouillac and Michard 1981), and Mg/Li (Kharaka and Mariner 1989) geothermometers were calculated. The saturation rates were determined with respect to the silica phase. The interpretation of these geothermometers led us to think in an initial assessment of the presence of a deep high temperature resource in a geothermal system, but it is necessary to consider the water–rock interaction condition. Thus, the Cl–SO4–HCO3 ternary diagram was used for the classification of the thermal fluids as a first step to describe a geothermal system. This diagram can help to define whether the geothermometers are applicable for the given water sample (Giggenbach 1991), as most solute geothermometers work only for neutral water or mature water that is characterized by high Cl− and low SO4 − (Sekento 2012). This diagram is helpful in providing an initial indication of mixing relationships or geographical groupings. Therefore, the Na–K–Mg ternary diagram (Giggenbach 1986) was used for the evaluation of equilibrium between the thermal waters and rocks at the studied depth and to determine the reliability of the used thermometers. The maximum depths reached by the hydrothermal fluids were estimated. Finally, the analysis of all the information led to the geochemical, isotopic, and geothermal regional model.
The Pampean plain in the south of Cordoba is part of a sedimentary basin whose varied topography is related to the presence of differentially tilted and sunken structural blocks. This basin shows a tectonic inversion from an extensional regime happened at the end of the Mezosoic to a compressive one in the Paleogene (Chebil et al. 1999). The plain covers part of the sedimentary basin called Chacoparanaense basin and minor depocenters such as the one in General Levalle. This depocenter, where the studied area is located, is linked to the regional cretaceous extension of the Gondwana supercontinent. In this sector, this regime was manifested as a process of active rifting related to the opening of the South Atlantic Ocean. The basin is bounded by extensional faults that are linked to an area of cortical weakness and limited by different ages and composition bedrock, as result of the suture between the Río de la Plata Craton and Pampia terrain (Calegari et al. 2014). It is part of the central Pampean rift system (Ramos 1999), filled with continental, alluvial, and lacustrine sedimentary successions (Webster et al. 2004). Calegari et al. (2014), based on seismic information, estimate that the sedimentary column could exceed 6000-m thick in the deeper sectors. The basin has a cortical attenuation which gives rise to a gravimetric anomaly linked to a crustal thinning and not the thick sedimentary column. Moreover, in the gravimetric profiles it is clearly observed that where it should be a gravimetric minimum due to the presence of a depocenter, there is actually a high (Calegari et al. 2014). Furthermore, chemical and isotopic analyses of rocks obtained in the mentioned deep boreholes from YPF Company (Ordoñez, Saira, Santiago Temple and Camilo Aldao) show the presence of granitic rocks enriched in lithophile elements of long ionic radio as Cs, Rb, Ba, Th, U, K, but depressed in elements such as Nb, Ta, Y, and Zr (Rapela et al. 2007; Rapela and Baldo 2014). Although this pattern is typical of basic rocks formed in arc environments (subduction zone), the larger development observed in the Ordoñez well suggests an arc origin and emplacement in continental crust.
Hydrolithology and hydrodynamics
Hydraulic features of the different aquifer systems
Hydraulic conductivity (K) (m/d)
Effective porosity (ep) (%)
Hydraulic gradients (%)
Groundwater velocity (m/d)
Up to 75–100
Confined aquifer systems
Hydrogeochemistry, isotope features, and groundwater age estimation
Chemical and stable isotopes results for confined aquifer systems
HCO3 − (mg/L)
SO 4 −2 (mg/L)
A1 CAS (n = 5)
1.5 ± 0.2
2.1 ± 0.2
1.6 ± 0.4
A2a CAS (n = 5)
1.5 ± 0.2
2.1 ± 0.2
2.5 ± 0.2
A2b CAS (n = 11)
1.8 ± 0.4
1.5 ± 0.4
1.8 ± 0.4
The isotopic similarity of A1 CAS with the unconfined aquifer would suggest hydraulic connection between systems. However, and taking into account that in the studied area all the wells are artesian, the hydraulic connection may have occurred nearby the piedmont where the hydraulic relationship is inverted. In contrast, the relationship may be local and the supply may go from A1 CAS aquifer to the unconfined one.
The similarity of isotopic composition between A1 and A2a CAS with the surface and groundwater of the piedmont areas of the Comechingones Mountains makes it possible to assume allochthonous recharge. Moreover, the existence of old waters in the studied area may be interpreted if the long distance to the recharge piedmont area (approximately 80 km) and the estimated groundwater velocity in the confined systems (about 0.07 m/d) are taking into consideration.
Notably, the freshest groundwater (944–1850 μS/cm) is the one found in the deepest system (A2b CAS). Also, it has more depleted isotopic values (δ18O ≈ −6.6‰; δ2H ≈ −43‰) than the overlying systems (Table 2; Fig. 6) which indicates a disconnection between them and also allochthonous recharge coming from the western area. That is to say, they have similar isotopic signatures to the rivers and streams located in the Comechingones Mountains and piedmont areas which are fed by depleted Atlantic rains, as was previously stated (Cabrera et al. 2010).
The hydraulic method suggests ages in the order of 3000 years (between 1500 and 7000 years) for the A1 CAS system and in the order of 4000 years (between 2000 and 9000 years) for deeper systems (A2a and A2b CASs).
The low activity of 3H in groundwater of confined systems (<2.5 UT) suggests that they are old waters recharged before the 1950s, that is to say, older than 60 years.
14C ages water confined aquifer systems
14C Age (BP)
Pearson-Gonfiantini (BP) ε = −8.46
Taking into account the geochemical features of these confined systems (2–3 mg/L of dissolved oxygen and huge amounts of dissolved sulfate) and in spite of being geothermal waters, evidences of the processes like methanogenesis, sulfate reduction, denitrification, or anaerobic oxidation of organic matter were not identified. Therefore, it is assumed that dead C from carbonate dissolution is the main cause of decreased 14C activity.
In this way, the corrected 14C values indicate an age between 2000 and 5000 BP for the A1 CAS and between 1000 and 23,000 BP for A2 CAS (Table 3). Younger ages estimated for groundwater in C13 well (A2a CAS) and C15 well (A2b CAS), even lower than those estimated with hydraulic methods, would be related to groundwater mixtures with the overlying systems, which confirms the interpretation from stable isotopes. However, it must be taken into account that this anomalous situation is also linked to the fact that some wells have been permanently opened for more than 50 years. Therefore, it is supposed that the oldest groundwater has already been drained (C15 well). The highest radiocarbon ages resulted higher than those obtained with the hydraulic method, probably because depth and confinement of A2 CAS may generate lower K values. Moreover, the hydraulic method only takes into account the advection process, whereas the age is affected by hydrodynamic dispersion then, the methods may produce similar results but never the same. It is important to highlight that to improve these interpretations more data of groundwater ages are needed.
Main temperature features of the confined aquifer systems
Upwelling temperature (°C)
Overheating with depth (°C)
Classification by temperature
Hypothermal to mesothermal
Hypothermal to mesothermal
The cationic geothermometers were used in order to compare results and to get an overview of the temperatures that the hydrothermal fluids could have reached. However, they were rejected because in the Na–K–Mg ternary diagram (Fig. 12b), although the samples are located near the boundaries of the partially equilibrated waters, they are in the immature waters field (Giggenbach 1986). Fournier and Truesdell (1973) indicate that these geothermometers, ion exchange reactions fluid-rock based, appear to give erratic results for waters from reservoirs at less than 200 °C due to different chemical reactions, i.e., precipitation of calcium as carbonate, Na–Ca exchange clays, among others.
The maximum temperatures that these fluids must have reached would suggest that groundwater flowed from recharge areas and reached greater depths and highest temperatures than those measured during well sampling (Fig. 7). This is also evidenced by the slight oversaturation in SiO2 (mainly chalcedony) that groundwater presents when it reaches lower temperatures in more shallow environments. In this way, the temperatures that should have reached these hydrothermal fluids in order to achieve their present composition lead us to estimate that these fluids must have descended between 486 m and 1562 m (average = 1018 m).
According to Blarasin et al. (2014) and Chiodi et al. (2014), the hydrothermalism in the area presents a strong geotectonic-structural conditioning, and it can be the result of the continental crustal thinning (Gimenez et al. 2011; Calegari et al. 2014). Thus, it may produce a geothermal anomaly and the regional geological faults (Kostadinoff and Reartes 1993) may be the most appropriate ways for groundwater circulation to several depths and the resulting heat transfer. Different hypotheses must be investigated in the future, for example, the presence of bedrock formed by granitic rocks (with U, Th, K, Llambias 2008; Rapella and Baldo 2014) that may produce high internal radiogenic heat over long time periods. Following Donaldson (1962), other probable hypothesis to be investigated is that the heat transference may be possible in these systems through sediments that underlie the aquifer and the distribution of heat in the aquifer system itself may become possible by free hydrothermal convection.
The geochemical and isotopic analyses show that the groundwater has meteoric origin being recharged in the mountain and piedmont western areas (Comechingones Mountains). The absence of 3H in most groundwater samples from the confined systems suggests that they are old waters not directly related to the present hydrological cycle. The 14C ages obtained for A1 and A2 CASs indicate waters recharged during Holocene cold periods, between the “Little Ice Age” and the ending of “Holocene Climatic Optimum,” and during the last glaciation, respectively.
The registered thermal anomaly defines a geothermal area with the highest values linked to the General Levalle Cretaceous depocenter, especially associated to the low block of the Tigre Muerto regional fault. This geothermal anomaly is consistent with the regional geotectonic setting and it is the result of the continental crustal thinning and the geological regional faults that make groundwater circulation easy at several depths. The groundwater flowing from recharge areas, favored by the dipping regional blocks, would have reached higher temperatures (in the order of 79 °C, according to the chalcedony geothermometer) explaining the present oversaturation in SiO2. This situation implies maximum depths up to 1500 m and the observed thermodynamic behavior for such mineralogical phases. This framework is in agreement with the Cl–SO4–HCO3 ternary diagram which indicates steam-heated waters. Moreover, the results obtained in the Na–K–Mg ternary diagram show that the cationic geothermometers were not useful because the samples were located in the immature water field near the boundary of the partially equilibrated waters.
In relation to the groundwater extraction rhythms, although the piezometric levels have been locally decreased, no significant changes have been observed in the past 20 years. Nonetheless, it is worth highlighting that the groundwater that is being used was recharged thousands of years ago, which should be taken seriously into account if a sustainable groundwater management is desired.
More studies are needed to improve the knowledge about these confined aquifers, then it is necessary to have more information about hydraulic aquifer parameters and piezometric level monitoring.
AC and MB carried out the field survey. AC processed the geological, hydrogeological, hydrochemical, isotopic, and geothermal data and has made the maps and profiles for the manuscript. MB furthermore participated in the interpretation of data and results and reviewed literature for the manuscript. LM carried out isotopical and groundwater age estimation. All authors read and approved the final manuscript.
The authors declare that they have no competing interests.
This paper was supported by FONCyT-MINCyT Cordoba PID 35/08, UNRC and partially by IAEA Research Contract ARG: 17385; CRP F33020.
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- Albu M, Banks D, Nash H. Mineral and thermal groundwater resources. London: Chapman & Hall; 1997.View ArticleGoogle Scholar
- APHA, AWWA, WPCF. American Public Health Association & Eaton, Andrew D & Water Environment Federation & American Water Works Association. Standard methods for the examination of water and wastewater, 21st. Washington, D.C.; 2005.Google Scholar
- Arnórsson S. Isotopic and chemical techniques in geothermal exploration, development and use. Sampling methods, data handling and interpretation. Vienna: International Atomic Energy Agency; 2000. p. 351.Google Scholar
- Blarasin M, Cabrera A, Matteoda E, editors. Aguas subterráneas de la provincia de Córdoba. UniRío. Universidad Nacional de Río Cuarto. Argentina; 2014.Google Scholar
- Cabrera A. Evolución hidrogeoquímica e isotópos ambientales del sistema acuífero asociado a los ambientes morfotectónicos de la falla regional Tigre Muerto. Córdoba. Tesis doctoral. UNRC. Inédita; 2009. p. 300Google Scholar
- Cabrera A, Blarasin M, Matteoda E. Análisis hidrodinámico, geoquímico e isotópico de base para la evaluación de sistemas hidrotermales de baja temperatura en la llanura cordobesa argentina. Revista Boletín Geológico y Minero de España. 2010;121(4):387–400.Google Scholar
- Cabrera A, Blarasin M, Maldonado L. Modelo hidrotermal de baja entalpía en acuíferos confinados utilizando geotermómetros. Córdoba. Argentina. En: Actas del XI Congreso Latinoamericano de Hidrogeología. Cartagena de Indias. Colombia. 20–24 Agosto 2012; 2012.Google Scholar
- Cabrera A, Blarasin M, Maldonado L. Influencia de morfoestructuras sobre la dinámica y calidad del agua subterránea de un sector de la llanura pampeana cordobesa. En: Resúmenes del V Congreso Argentino de Cuaternario y Geomorfología. Río Cuarto. Córdoba, Argentina. 2–4 Octubre 2012; 2012.Google Scholar
- Calegari R, Chebli G, Manoni R, Lázzari V (2014) Cuencas Cretácicas de la Región Central del Pais: General Levalle. En: Relatorio del XIX Congreso Geológico Argentino. Córdoba, 2. 2–6 Junio 2014; 2014. p. 913–37.Google Scholar
- Chebli G, Mozetic M, Rossello C, Bühler M. Cuencas Sedimentarias de la Llanura Chacopampeana. En Caminos R, editor. Geología Argentina, Servicio Geológico Minero, Instituto de Geología y Recursos Naturales, Anales, 29. Buenos Aires; 1999. p. 627–44.Google Scholar
- Chiodi A, Martino R, Báez W, Fórmica S, Fernández G. Recursos Geotérmicos de Córdoba. En: Relatorio del XIX Congreso Geológico Argentino. Córdoba, 2. 2–6 Junio 2014; 2014. p. 1179–87.Google Scholar
- Craig H. Isotopic standards for carbon and oxygen and correction factors for mass-spectrometric analysis of carbon dioxide. Geochim Cosmochim Acta. 1957;12:133–49.View ArticleGoogle Scholar
- Custodio E, Llamas M. Hidrología subterránea. 2nd ed. Barcelona: Omega; 1996. p. 1–2350.Google Scholar
- Degiovanni S, Villegas M, Blarasin M y Sagripanti G. Hoja Geológica 3363-III Río Cuarto. 1:250.000. Programa Nacional de Cartas Geológicas. Secretaría de Minería de la Nación (SEGEMAR). Boletín No 349. Argentina; 2005.Google Scholar
- Donaldson I. Temperature gradients in the upper layers of the Earth’s crust due to convective water flows. J Geophys Res. 1962;67:3449–59.View ArticleGoogle Scholar
- Fournier R, Truesdell A. An empirical Na-K-Ca geothermometer of natural water. Geochim Cosmochim. 1973;37:1255–75.View ArticleGoogle Scholar
- Fournier R, White D, Truesdell A. Geochemical indicators of subsurface temperature. Part I, basic assumptions. J Res US Geol Surv. 1974;23:259–62.Google Scholar
- Fouillac C, Michard G. Sodium/lithium ratio in water applied to geothermometry of geothermal reservoirs. Geothermics. 1981;10:55–70.View ArticleGoogle Scholar
- Giggenbach WF. Geothermal solute equilibria. Derivation of Na-K-Mg-Ca geoindicators. Geochim. Cosmochim. Acta. 1988;52(12):2749–65.View ArticleGoogle Scholar
- Giggenbach WF. Graphical techniques for the evaluated water/rock equilibration conditions by use of Na, K, Mg and Ca contents of discharge water. Proceedings of the 8th New Zealand Geothermal Workshop; 1986. p. 37–43.Google Scholar
- Giggenbach WF. Chemical techniques in geothermal exploration, In: D’Amore F, editor. Applications of geochemistry in geothermal reservoir development. UNITAR/UNDP publication, Rome; 1991. p. 119–45.Google Scholar
- Gimenez M, Dávila F, Astini R, Martínez P. Interpretación gravimétrica y estructura cortical en la cuenca de General Levalle, Provincia de Córdoba, Argentina. Revista Mexicana de Ciencias Geológicas. 2011;28(1):105–17.Google Scholar
- Gonfiantini R. Standards for stable isotope measurements in natural compounds. IAEA/WMO, 2002. G. Network for isotopes in precipitation. The GNIP database. Nature. 1978;271:534–6.View ArticleGoogle Scholar
- Kazemi G, Lehr J, Perrochet P. Groundwater age. New Jersey: Wiley; 2006.View ArticleGoogle Scholar
- Kharaka Y, Mariner R. Thermal history of sedimentary basins. Methods and case histories. New York: Springer-Verlag; 1989.Google Scholar
- Kostadinoff J, Reartes W. Medición e interpretaciones del flujo de calor terrestre en el Sur de la provincia de Buenos Aires. Revista de la Asociación Geológica Argentina. 1993;48(2):147–53.Google Scholar
- Lis G, Wassenaar L, Hendry M. High-precision laser spectroscopy D/H and 18O/16O measurements of microliter natural water samples. Anal Chem. 2008;80(1):287–93. doi:10.1021/ac701716q.View ArticleGoogle Scholar
- Llambias E. Geología de los cuerpos ígneos. Revista de la Asociación Geológica Argentina. Serie B. Didáctica y complementaria 29. Bs. As; 2008.Google Scholar
- Mark G, Foster D, Pollard P, Williams P, Tolman J, Darvall M, Blake K. Stable isotope evidence for magmatic fluid input during large-scale Na–Ca alteration in the Cloncurry Fe oxide Cu–Au district, NW Quensland, Australia. Terra Nova. 2004;16(2):45–89.View ArticleGoogle Scholar
- Maldonado L, Blarasin M, Cabrera A, Panarello H, Dapeña C. Assessing groundwater age in confined aquifers from the central Pampean plain of Córdoba, Argentina. Radiocarbon. 2016. doi:10.1017/RDC.2016.35.Google Scholar
- Pérez M, Tujchneider O, Paris M, D’Elia M. Estimación de la conductividad hidráulica a partir de datos granulométricos. Actas de XIX Congreso Geológico Argentino. Martino R, Lira R, Guereschi A, Baldo E, Franzese J, Krohling D, Manassero M, Ortega G, Pinotti L, editors. Córdoba, Argentina; 2014.Google Scholar
- Pesce A. Web SEGEMAR. 2008. http://www.segemar.gov.ar/geotermia/geoter.htm.
- Pieters P, Skirrow R. Informe geológico y metalogenético de las sierras de San Luis y Comechingones, provincia de San Luis y Córdoba. Servicio Geológico Minero Argentino. Proyecto de Cooperación Argentino-Australiano, Buenos Aires. Argentina; 1997. p. 129.Google Scholar
- Ramos V. Rasgos Estructurales del Territorio Argentino. RAGA-Revista de la Asociación Geológica Argentina. Instituto de Geología y Recursos Minerales. 1999;29(24):715–84.Google Scholar
- Rapela C, Pankhurst R, Casquet C, Fanning C, Baldo E, Gónzalez Casado J, Galindo C, Dahlquist J. The Río de la Plata craton and the assembly of SW Gondwana. Earth Sci Rev. 2007;83(1–2):49–82.View ArticleGoogle Scholar
- Rapela C, Baldo E. El cratón del Río de la Plata en la provincia de Córdoba. Relatorio del XIX Congreso Geológico Argentino. Córdoba, Argentina; 2014. p. 871–80.Google Scholar
- Reinante S, Olivieri G, Salinas A, Lovechio J, Basile Y. La cuenca Chacoparaná: estratigrafía y recursos de hidrocarborus. XIX Congreso Geológico Argentino. Córdoba, Argentina; 2014. p. 895–912.Google Scholar
- Salem O, Visser J, Dray M, Gonfiantini R. Groundwater flow patterns in the Western Lybiam Arab Jamahiriya evaluated from isotope data. In: Investigations with isotope techniques. international atomic energy agency. Vienna; 1980. p. 165–80.Google Scholar
- Schafmeister M. What grains can tell on Darcy velocity? International Symposium Aquifers Systems Management. Dijon, France, Communication DARCY-126, CD ROM edition; 2006.Google Scholar
- Sekento L R (2012) Geochemical and isotopic study of the Menengai geothermal field, Kenya. Report 31 in: Geothermal Training in Iceland 2012. UNU-GTP, Iceland, 769–92.Google Scholar
- Sigismondi M, Fantín F. Estructura cortical y características geodinámicas. XIX Congreso Geológico Argentino. Córdoba, Argentina; 2014. p. 939–61.Google Scholar
- Stober I, Bucher K. Geothermal energy. Berlin: Springer-Verlag; 2013.View ArticleGoogle Scholar
- Tamers M. Validity of radiocarbon dates on groundwater. Geophys Surv. 1975;2:217–39.View ArticleGoogle Scholar
- Tóth J. Gravitational systems of groundwater flow. Theory, evaluation, utilization. Cambridge: Cambridge University Press; 2009. p. 297.View ArticleGoogle Scholar
- Webster R, Chebli G, Fischer J. General Levalle basin, Argentina: a frontier Lower Cretaceous rift basin. Am Assoc Petrol Geol Bull. 2004;88:627–52.Google Scholar
- Vasilyev G, Peskov N, Gornov V, Kolesova M. The effectiveness of low-grade geothermal heat usage under the conditions of the Russian climate. Geothermics. 2016;62:93–102.View ArticleGoogle Scholar