- Research article
- Open Access
Modeling acid-gas generation from boiling chloride brines
© Zhang et al; licensee BioMed Central Ltd. 2009
- Received: 27 September 2008
- Accepted: 16 November 2009
- Published: 16 November 2009
This study investigates the generation of HCl and other acid gases from boiling calcium chloride dominated waters at atmospheric pressure, primarily using numerical modeling. The main focus of this investigation relates to the long-term geologic disposal of nuclear waste at Yucca Mountain, Nevada, where pore waters around waste-emplacement tunnels are expected to undergo boiling and evaporative concentration as a result of the heat released by spent nuclear fuel. Processes that are modeled include boiling of highly concentrated solutions, gas transport, and gas condensation accompanied by the dissociation of acid gases, causing low-pH condensate.
Simple calculations are first carried out to evaluate condensate pH as a function of HCl gas fugacity and condensed water fraction for a vapor equilibrated with saturated calcium chloride brine at 50-150°C and 1 bar. The distillation of a calcium-chloride-dominated brine is then simulated with a reactive transport model using a brine composition representative of partially evaporated calcium-rich pore waters at Yucca Mountain. Results show a significant increase in boiling temperature from evaporative concentration, as well as low pH in condensates, particularly for dynamic systems where partial condensation takes place, which result in enrichment of HCl in condensates. These results are in qualitative agreement with experimental data from other studies.
The combination of reactive transport with multicomponent brine chemistry to study evaporation, boiling, and the potential for acid gas generation at the proposed Yucca Mountain repository is seen as an improvement relative to previously applied simpler batch evaporation models. This approach allows the evaluation of thermal, hydrological, and chemical (THC) processes in a coupled manner, and modeling of settings much more relevant to actual field conditions than the distillation experiment considered. The actual and modeled distillation experiments do not represent expected conditions in an emplacement drift, but nevertheless illustrate the potential for acid-gas generation at moderate temperatures (<150°C).
- Concentration Factor
- Reactive Transport Model
- Acid Condensate
This study was conducted as part of investigations related to the long-term safety assessment of the proposed high-level nuclear waste repository at Yucca Mountain, Nevada. The heat released by the spent nuclear fuel is expected to induce boiling at near-atmospheric pressure of pore water (moisture) present in the unsaturated rock around waste-emplacement tunnels [1–5]. This boiling, as well as the deliquescence of naturally occurring salts in dust, could lead to the formation of residual brines [6, 7] at temperatures significantly above the boiling point of pure water , possibly accompanied by the release of acid gases such as HCl and formation of acid condensate [9, 10]. The potential enhancement of waste package corrosion by the release of HCl and other acid gases from such solutions and subsequent formation of acid condensate was the primary motivation for this study.
Gaseous HCl is often a primary cause of well-casing and pipe-system corrosion in geothermal systems [11–13]. For this reason, many studies have focused on gaseous HCl and acid condensates in geothermal areas. In most instances, the HCl source is volcanic in origin [14–17]. Fournier and Thompson  reported the generation of HCl gas through steam-driven hydrolysis of NaCl at 600°C and pressures up to 700 bar, and suggested that the hydrolysis of chloride brines could be at the origin of HCl gas in volcanic and sub-volcanic environments. Bischoff et al. , studying the generation of HCl gas in the CaCl2-H2O system at high temperature (380-500°C and pressure (up to about 800 bar), showed that this system generates significant amounts of HCl in the vapor phase by the hydrolysis of CaCl2. These authors concluded this mechanism is likely the source of HCl in steam at the Geysers geothermal system in Northern California.
Very few experiments have been conducted to evaluate the formation of HCl gas in natural systems at atmospheric pressure and (relatively) low temperatures. In the context of geologic disposal of nuclear waste, Pulvirenti et al.  distilled a synthetic concentrated CaCl2-type water representative of some of the calcium-rich pore waters at Yucca Mountain. These authors observed a number of acid gases released from the concentrated brine, including HCl, Cl2, NO, NO2, and HNO3. The vapor from their distillation experiments produced acid condensate (pH <1). Olsen et al.  conducted experiments similar to those of Pulvirenti et al. , and also obtained highly acid distillate and brine boiling temperatures exceeding 140°C. In this case, the authors suspected the acid gas produced may have consisted primarily of nitrosyl chloride (NOCl), which would be expected to release HCl upon contact with water . In both these cases, solutions were boiled in closed or partially closed systems that were unlike the conditions in a waste emplacement drift, but nevertheless indicated the generation of acid gases at temperatures significantly lower than is characteristic of geothermal systems.
Understanding the generation of acid gases and condensates is important for protecting metal structures from corrosion in geothermal production systems (and other engineered systems in the vicinity of boiling solutions). Modeling studies can provide insights into these processes and thus can be quite helpful. For example, Helgeson  and Glover  calculated the theoretical maximum HCl content of a vapor phase released from boiling a deep geothermal brine in an open system. Their results show that the maximum HCl content, as a function of temperature and steam fraction, can reach up to 200 mg/kg. Using a batch model, Andreussi et al.  calculated the chemical composition of the first drop of condensate that forms at dew-point temperature through expansion of superheated geothermal steam, with implications for corrosion and scaling in turbines. Their calculation considers the solution boiling-point elevation by referring the measured boiling point of NaCl solutions to an ionic strength that is the same as the solution being studied. More complex modeling studies on acid-gas generation and condensation from boiling chloride brines have not been conducted, at least not in the context of multiphase flow and multicomponent reactive transport, as done here. The objective of the present study is, therefore, to assess these processes as quantitatively as possible under conditions relevant to boiling systems at atmospheric pressures. This is achieved by first presenting simple bounding derivations of condensate pH as a function of vapor loss from a distiller (dynamic system) for a vapor initially at equilibrium with a saturated calcium chloride brine at 50-150°C and 1 bar. A more complex reactive transport model is then applied to simulate the distillation of a calcium-chloride-dominant brine at atmospheric pressure. Results show that acid distillates can be generated from relatively low-temperature gases (< 150°C), with pH values strongly dependent on the amount of water vapor condensing from the gas phase.
The reactive transport simulator TOUGHREACT [ and references therein] is used here, extended with a Pitzer activity-coefficient model based on the formulation of Harvie et al.  and thermodynamic data from Wolery et al.  (as implemented by Alai et al. ). For the Ca-Cl system, interactions parameters in this database were derived from  (Model 2 of these authors, without separate ion pairs CaCl+ and CaCl2(aq)) together with solubility data for CaCl2 hydrate salts from  and . These data reproduce reasonably well saturation concentrations from  for CaCl2:2H2O up to about 100°C , however somewhat underestimate saturations (by 15-20%) at ~150°C. A later revision of this thermodynamic database , not available prior to the start of this study, includes data derived from  (Model 3 of these authors, with separate ion pairs CaCl+ and CaCl2(aq)) that yield more accurate saturations at high temperatures. For HCl(g), reference thermodynamic data are taken from  and extrapolated to higher temperatures using SUPCRT92 . The implementation of the Pitzer model in TOUGHREACT is presented in Zhang et al. [33, 34], together with comparisons of calculated activity and osmotic coefficients with measured data from the literature [e.g., ].
TOUGHREACT computes reactive flow and transport for multicomponent and multiphase systems. In the present case, the multiphase system includes an aqueous phase containing dissolved salts, a gaseous phase (air, water vapor, trace gases), and various solid mineral phases. Therefore, a representative geochemical system is considered, including aqueous speciation, mineral (salts) precipitation and dissolution, and gas generation and dissolution/reaction in condensate. The coupled heating, boiling, vapor phase transport and condensation are modeled in the context of nonisothermal multiphase flow and reactive geochemical transport. The boiling point elevation caused by elevated concentrations of dissolved salts is captured in the model through the lowering of the water-vapor pressure resulting from the decrease in water activity with increasing ionic strength . The numerical model relies on an equation-of-state module that computes the physical properties and phase equilibrium behavior of water and saline solutions, coupled with multiphase flow and transport (advection and diffusion) in the phases involved (liquid or gas). As such, the numerical model simulates "real" evaporation and condensation as a function of temperature, pressure, and system composition, including vapor pressure lowering and PVT effects from condensation and feedback on fluid flow .
It should be noted that TOUGHREACT was designed to simulate multiphase flow in porous media (i.e., using Darcy's law), and therefore cannot accurately simulate flow in open conduits (i.e., flow represented with Navier-Stokes equation) such as would be required for the distillation simulation presented below. In this study, flow and transport processes in open conduits are approximated using a high-permeability porous-medium representation. In this respect, simulation results regarding gas flow are regarded as more qualitative than quantitative.
Preliminary calculations assuming pure CaCl2 solutions were carried out to investigate relationships between salt concentration, HCl gas fugacity (≅ partial pressure), and condensate pH at various temperatures. These calculations are based on analytical derivations that are applied using computed HCl gas fugacities and water activities. The objective is to illustrate, as simply as possible, the effect of partial condensation (vapor loss from a distiller) on condensate pH in a dynamic system. Note that more sophisticated numerical simulations of distillation are presented later, and do not rely on these preliminary analyses.
Computed chemical properties of saturated CaCl2:2H2O solutions at 50-150°C and ~1 bar.
P 0 sat
The distillation of a calcium-chloride-dominant brine was simulated based on an experiment reported by Pulvirenti et al. . These authors distilled at atmospheric pressure a synthetic brine of a composition intended to represent evaporated Yucca Mountain pore water. The actual brine composition was determined by Rosenberg et al.  after evaporating a synthetic solution representative of certain types of calcium-rich pore waters at Yucca Mountain and concentrating that solution by a factor of 1,243.
Initial brine salt recipe (Pulvirenti et al. ).
SiO2 xH2O (84%SiO2)
The atmosphere was represented using a large gridblock (essentially infinite volume) having constant temperature and pressure (25°C, 1 bar), and connected directly to the gridblock representing the condenser, set at the same conditions. Only the condenser gridblock was allowed contact with the atmosphere (the outlet of the condenser). Initial conditions in the gridblock representing the flask were set at the boiling point of pure water under atmospheric conditions (~100°C, 1 bar). Heat was applied directly to the gridblock representing the flask. No liquid-phase flow was allowed to take place from the flask to the condenser; thus, mass transport resulted only from vapor flow by advection and diffusion. Heat loss by vapor flow out of the system was accounted for. Note that "real" condensation was simulated, meaning that the model relies on a full equation of state coupled to heat flow and fluid flow to predict the amount of condensation taking place by cooling in the condenser. In the present case, most of the generated vapor was predicted to flow into the atmosphere gridblock, with a minor part condensing in the condenser, as discussed later. The distillate was allowed to flow out of the condenser gridblock into the atmosphere gridblock.
Initial chemical composition of the synthetic brine used in the numerical simulation, determined from the salt recipe in Table 2.
The time step size was chosen to capture the fast evaporation of the brine (relative to a constant heat input) in the final boiling stages. The simulation was run for a total boiling time of 3.1 days, a point at which the ionic strength of the brine in the flask reached 41 molal and numerical convergence was difficult to achieve. That simulation end point corresponds to a concentration factor of ~54,000 relative to initial pore water.
The simulated temperature of the brine rises with increasing concentration factor (Figure 4), directly reflecting the effect of vapor-pressure lowering by increasing salt concentrations. Two main breaks in the temperature and water activity trends (Figure 4) reflect the precipitation of halite at a concentration factor around 6,500 (water activity around 0.65) and calcium chloride at a concentration factor of around 21,000 (water activity around 0.2) (Figure 5).
The concentrations of aqueous components increase monotonically before precipitation occurs (Figure 5). After the precipitation of halite, the sodium concentration decreases, but chloride concentration continues to increase, although at a decreased rate. This occurs because the chloride concentration is higher than the sodium concentration in the initial solution (Table 2). Note that the sodium concentration does not remain constant after equilibration with halite because the concentrations of other species still increase with continued boiling, thus affecting activity coefficients and the ionic activity product of halite. The same processes apply to other components. Upon further boiling, the precipitation of calcium chloride removes calcium from the solution, causing the calcium concentration to decrease and chloride concentration to nearly stabilize. Note that sylvite precipitation is predicted to start at a concentration factor close to 9,500, causing an obvious decrease in potassium concentration but essentially producing unnoticeable changes in the temperature and chloride trends. However, at the onset of calcium chloride precipitation, the potassium concentration starts to increase because the precipitation of calcium chloride consumes a lot of choride, causing sylvite to precipitate at a decreased rate. Nitrate salts were not predicted to precipitate in this simulation, which was carried out until numerical convergence was no longer achieved (at concentration factor ~54,000).
The pH of the boiling brine is computed to decrease from an initial value of around 8, with noticeable breaks at pH 6.6 when halite starts to precipitate (concentration factor around 6,500) and pH around 3.7 when calcium chloride forms (concentration factor around 21,000) (Figures 5 and 6). The pH decrease is mostly driven by the evaporative concentration effect on H+, as well as the increase in the activity coefficient of H+ at higher ionic strengths, and (to a lesser extent) by the temperature effect on the dissociation of water and bicarbonate. The precipitation of halite and later calcium chloride (the two most dominant salts) are responsible for most of the reduction in the rate of ionic strength increase with evaporation (and thus most of the reduction in the rate of activity coefficient increase and water activity decrease). As a result, the precipitation of these salts coincides with breaks in the pH trend. Note that as a result of decreasing pH, and a more pronounced activity coefficient increase for sulfate (double-charged) than bicarbonate (single-charged), calcite dissolves in favor of calcium sulfate precipitation (e.g., SO4-2 + CaCO3(s) + H+ ==> CaSO4(s) + HCO3-) and eventually totally disappears at a concentration factor of about 7,200.
Three acid gases, HCl, HF, and HNO3, are exsolved from the boiling brine in the beaker. Their partial pressure trends as a function of concentration factor (Figure 6) show breaks corresponding to the changes in pH discussed above (Figure 6). These breaks are indirectly induced by halite and calcium chloride precipitation (Figure 5) which also correspond to the temperature breaks observed earlier (Figure 4). The trend of CO2 partial pressure is closely related to the decreasing pH in the beaker (Figure 6) and the resulting dissolution of calcite (Figure 5). Initially, the CO2 partial pressure drops slightly because more CO2 is lost by gas-phase transport than produced by calcite dissolution. However, as the pH decreases further and more calcite dissolves, the CO2 partial pressure starts rising. Eventually, when all calcite is consumed, the CO2 partial pressure drops sharply as the brine becomes depleted in total dissolved carbonate (the diffusion of atmospheric CO2 into the distillation apparatus is not sufficient to maintain atmospheric CO2 conditions directly above the beaker).
Condensation occurs in the condenser where the vapor is cooled to 25°C. The acid gases dissolve immediately into the condensate, causing its pH to drop (Figure 6). As discussed earlier, the pH of the condensate is controlled primarily by the fugacities of the acid gases (mostly HCl in this case, Figure 6) and the amount of vapor loss from the distiller. The more vapor loss (with preferential partitioning of HCl into the condensate), the smaller the amounts of condensed water and proportionally higher HCl enrichment in condensate, thus the lower the pH in the condensate (Figure 1). Note that in this simulation, the predicted condensate pH (Figure 6) represents computed values for "instantaneous" condensation (i.e., small amounts of distillate generated at prescribed intervals in time, without allowing continuous accumulation of the distillate). The condensate is allowed to accumulate for a simulated time period around 1.5 minutes. During this time, the amount of vapor flowing out of the condenser is computed to be around 96% of the H2O mass flowing into the condenser, yielding very low (negative) condensate pH values at elevated temperatures, in qualitative agreement with the preliminary analyses discussed earlier. When simulations are set up such that the distillate continuously accumulates in the condenser, with more complete condensation of the incoming vapor stream, predicted pH values in the condensate remain above 2.
Model results show low-pH condensates from acid-gas volatilization, as observed in the distillation experiments of Pulvirenti et al. . When it is distilled, the synthetic concentrated brine releases acid gases, in our case predicted to consist primarily of HCl and HF. Two key factors, however, affect the generation of acid condensate: (1) the concentration factor and (2) the amount of condensation taking place, which is a direct function of the amount of vapor loss from the distiller (partial condensation). In our simulations, the volatilization of acid gases in quantities significant to yield condensate pH values below 2 were predicted only at high concentration factors (above >20,000), and only in cases where significant vapor loss (partial condensation) occurred. Note that Alai et al.  report no evidence of acid gases in evaporation experiments up to concentration factors ~3,400 using a similar type of water. This is in agreement with our results, which show that at such a lower concentration factor, the predicted partial pressures of these gases are quite low (<10-12 bar for HF, <10-10 for HCl, and <10-11 for HNO3).
The two salts most significantly affecting predicted thermal evolution and chemical trends in the brine and vapor are halite and calcium chloride. These salts precipitate in our simulations at concentration factors of ~6,500 and ~21,000, respectively, producing noticeable breaks in the predicted trends of brine pH and temperature, gas partial pressures, and condensate pH (Figures 4, 5, and 6). These breaks occur because the rate of ionic strength increase with evaporation is sharply reduced once these minerals start to precipitate, in turn reducing the rate at which ion activity coefficients increase (and water activity decreases) with increasing evaporation. Upon continuous boiling, the most pronounced break in the trend of increasing temperatures occurs at ~153°C when the brine becomes saturated with respect to calcium chloride. It should be noted that, upon further evaporation, predicted temperatures climbed up to near 180°C, significantly higher than the maximum temperature (~144°C) in the distillation experiment . Because of large uncertainties in ion-interaction parameters for mixtures of multiple salts at elevated temperature, most notably those of the nitrate salts, model results above ~150°C (above concentration factors ~20,000) should be viewed with caution.
The model presented in this study incorporates physical and chemical processes affecting the boiling of saline solutions, including boiling point elevation, salt precipitation, and brine chemistry at elevated ionic strength and temperature. By implementing these processes into an existing reactive transport code, we were able to reproduce, at least semi-quantitatively, the volatilization of acid gases and generation of acid condensate observed in laboratory experiments such as those of Pulvirenti et al.  and Olsen et al. . The simulation of vapor flow by advection and diffusion was only approximate because open conduits were approximated by a porous medium with high permeability. Nevertheless, fundamental processes were captured, including evaporative concentration with vapor-pressure lowering, volatilization of HCl, HF, and HNO3, and transport followed by dissociation of these gases into vapor condensate.
The combination of reactive transport with multicomponent brine chemistry to study evaporation, boiling, and the potential for acid gas generation at the proposed Yucca Mountain repository is seen as an improvement relative to previously applied simpler batch evaporation models [6, 7]. This approach allows the evaluation of thermal, hydrological, and chemical (THC) processes in a coupled manner, and modeling of settings much more relevant to actual field conditions than the distillation experiment considered here. Further modeling work by the authors  has integrated the type of brine distillation model presented here into full THC simulations of the near-field within and around waste emplacement tunnels. These simulations show that deleterious effects of acid gases from boiling pore waters at Yucca Mountain are not anticipated because very small amounts of acid gases are generated, that are quickly buffered by the comparatively large rock mass surrounding emplacement tunnels.
The authors would like to thank three anonymous reviewers for their careful and helpful reviews. We also thank John Apps for a very useful internal review of this paper, and Daniel Hawkes for editorial support. This manuscript has been authored by Lawrence Berkeley National Laboratory under Contract No. DE-AC02-05CH11231 with the U.S. Department of Energy. The views and opinions of authors expressed in this article do not necessarily state or reflect those of the United States Government or any agency thereof or The Regents of the University of California.
- Buscheck TA, Nitao JJ: The impact of thermal loading on repository performance at Yucca Mountain: Part I. Modeling and Analysis. Nuclear Technology. 1993, 104: 418-448.Google Scholar
- Buscheck TA, Glascoe LG, Lee KH, Gansemer J, Sun Y, Mansoor K: Validation of the multiscale thermohydrologic model used for analysis of a proposed repository at Yucca Mountain. J of Contaminant Hydrology. 2003, 62-63: 421-440. 10.1016/S0169-7722(02)00157-2.View ArticleGoogle Scholar
- Haukwa CB, Wu YS, Bodvarsson GS: Modeling thermal-hydrological response of the unsaturated zone at Yucca Mountain, Nevada. J of Contaminant Hydrology. 2003, 62-63: 552-552.Google Scholar
- Spycher N, Sonnenthal E, Apps J: Fluid flow and reactive transport around potential nuclear waste emplacement tunnels at Yucca Mountain, Nevada. J of Contaminant Hydrology. 2003, 62-63: 653-674. 10.1016/S0169-7722(02)00183-3.View ArticleGoogle Scholar
- Sonnenthal E, Ito A, Spycher N, Yui M, Apps J, Sugita Y, Conrad M, Kawakami S: Approaches to modeling coupled thermal, hydrological, and chemical processes in the Drift Scale Heater Test at Yucca Mountain. International Journal of Rock Mechanics and Mining Sciences. 2005, 42: 698-719. 10.1016/j.ijrmms.2005.03.009.View ArticleGoogle Scholar
- Rosenberg ND, Gdowski GE, Knauss KG: Evaporative chemical evolution of natural waters at Yucca Mountain, Nevada. Applied Geochemistry. 2001, 16: 1231-1240. 10.1016/S0883-2927(01)00013-0.View ArticleGoogle Scholar
- Alai M, Sutton M, Carroll S: Evaporative evolution of Na-Cl-NO3-K-Ca-Mg-Si brine at 95°C: experiments and modeling relevant to Yucca Mountain, Nevada. Geochemical Transactions. 2005, 6: 31-45. 10.1186/1467-4866-6-31.View ArticleGoogle Scholar
- Carroll S, Craig L, Wolery T: Deliquescence of NaCl-NaNO3, KNO3-NaNO3, and NaCl-KNO3 salt mixtures from 90 to 120°C. Geochemical Transactions. 2005, 6: 19-30. 10.1186/1467-4866-6-19.View ArticleGoogle Scholar
- Olsen AA, Rimstidt JD: Corrosion of Yucca Mountain high-level radioactive waste canister material. Water-Rock Interaction, WRI-11. Edited by: Wanty RB, Seal RR. 2004, Balkema Publishers, New York, 1597-1599.Google Scholar
- Pulvirenti AL, Needham KM, Adel-Hadadi MA, Barkatt A, Marks CR, Gorman JA: Multiphase corrosion of engineered barrier materials. Corrosion. NACE International, March 28-April 1, 2004, New Orleans. 2004Google Scholar
- White DE, Truesdell AH: Geothermal reservoirs of Taiwan-an evaluation of existing data. Mining Research and Service Organization, MOEA Report. 1970, 105: 51-81.Google Scholar
- Ellis AJ, Mahon WAJ: Chemistry and geothermal systems. 1977, Academic Press, 392-Google Scholar
- Truesdell AH, Haizlip JR, Armannsson H, D'Amore F: Origin and transport of chloride in superheated geothermal steam. Geothermics. 1989, 18: 295-304. 10.1016/0375-6505(89)90039-4.View ArticleGoogle Scholar
- White DE, Waring GA: Volcanic Emanations. Data of Geochemistry, USGS Prof Paper 440-K. Edited by: Fleischer M. 1963, 29-Google Scholar
- Noguchi K, Goto T, Ueno S, Inahashi M: Geochemical investigation of the strong acid water from the bored wells in Hakone, Japan. U.N. Symposium on Geothermal Resources, Part 1. Geothermics. 1976, 2: 561-563. 10.1016/0375-6505(70)90056-8.View ArticleGoogle Scholar
- Ozawa T, Kamada M, Yoshida M, Sanemasa I: Genesis of hot springs, Part I genesis of acid hot springs. Journal of Japan Geothermal Energy Assoc. 1973, 10 (2): (Ser. No. 37)Google Scholar
- Lawless JV, Gonzales RC: Geothermal geology and review of exploration, Biliran Island. Proceedings of 4th New Zealand Geothermal Workshop. 1982, 161-167. Part 1Google Scholar
- Fournier RO, Thompson JM: Composition of steam in the system NaCl-KCl-H2O-quartz. Geochim cosmochim Acta. 1993, 57: 4365-4375. 10.1016/0016-7037(93)90488-I.View ArticleGoogle Scholar
- Bischoff JL, Rosenbauer JR, Fournier RO: The generationof HCl in the system CaCl2-H2O: Vapor-liquid relations from 380-500 °C. Geochimica et Cosmochimica Acta. 1996, 60: 7-16. 10.1016/0016-7037(95)00365-7.View ArticleGoogle Scholar
- Bekcham LJ, Fessler WA, Kise MA: Nitrosyl chloride. Chemical Reviews. 1951, 48: 319-396. 10.1021/cr60151a001.View ArticleGoogle Scholar
- Helgeson HC: Thermodynamics of hydrothermal systems at elevated temperatures and pressures. Am J Sci. 1969, 267: 729-804.View ArticleGoogle Scholar
- Glover RB: Calculation of the chemistry of some geothermal environments. DSIR New Zealand, Chemistry Division Report. 1982, CD 2323-Google Scholar
- Andreussi P, Corsi R, Guidi M, Marini L: Theoretical prediction of physical and chemical characteristics of the "first drop" of condensate from superheated geothermal steam. Implications for corrosion and scaling in turbines. Geothermics. 1994, 23: 233-255. 10.1016/0375-6505(94)90002-7.View ArticleGoogle Scholar
- Xu T, Sonnenthal E, Spycher N, Pruess K: TOUGHREACT -- A simulation program for non-isothermal multiphase reactive geochemical transport in variably saturated geologic media: applications for geothermal injectivity and CO2 geologic sequestration. Computers and Geosciences. 2006, 32: 145-165. 10.1016/j.cageo.2005.06.014.View ArticleGoogle Scholar
- Harvie CE, Møller N, Weare JH: The prediction of mineral solubilities in natural waters: the Na-K-Mg-Ca-H-Cl-SO4-OH-HCO3-CO3-CO2-H2O system to high ionic strengths at 25°C. Geochim Cosmochim Acta. 1984, 48: 723-751. 10.1016/0016-7037(84)90098-X.View ArticleGoogle Scholar
- Wolery T, Jove-Colon C, Rard J, Wijesinghe A: Pitzer database development: Description of the Pitzer geochemical thermodynamic database data0.ypf. Appendix I. In-Drift Precipitates/Salts Model (P. Mariner) Report ANL-EBS-MD-000045 REV 02. 2004, Las Vegas, Nevada: Bechtel SAIC CompanyGoogle Scholar
- Sterner SM, Felmy AR, Oakes CS, Pitzer KS: Correlation of thermodynamic data for aqueous electrolyte solutions to very high ionic strength using INSIGHT: Vapor saturated water activity in the system CaCl2-H2O to 250°C and Solid Saturation. International Journal of Thermophysics. 1998, 19 (3): 761-770.Google Scholar
- Pitzer KS, Oakes CS: Thermodynamics of calcium chloride in concentrated aqueous solutions and in crystals. Journal of Chemical and Engineering Data. 1994, 39 (3): 553-559. 10.1021/je00015a035.View ArticleGoogle Scholar
- Pitzer KS, Shi Y: Thermodynamics of calcium chloride in highly concentrated aqueous solution and in hydrated crystals. Journal of Solution Chemistry. 1993, 29 (2): 99-105. 10.1007/BF00650677.View ArticleGoogle Scholar
- Jove-Colon C, Wolery T, Rard J, Wijesinghe A, Jareck R, Helean K: Pitzer database development: Description of the Pitzer geochemical thermodynamic database data0.ypf.R2. Appendix I. In-Drift Precipitates/Salts Model, ANL-EBS-MD-000045 REV 03, DOC.20070306.0037. 2007, Las Vegas, Nevada: Sandia National LaboratoriesGoogle Scholar
- Barin I, Platzki G: Thermochemical Data of Pure Substances. Two volumes. 1995, New York, New York: VCH Publishers, 3View ArticleGoogle Scholar
- Johnson JW, Oelkers E, Helgeson HC: SUPCRT92: A software package for calculating the standard molal thermodynamic properties of minerals, gases, aqueous species and reactions from 1 to 5000 bar and 0 to 1000°C. Comput Geosci. 1992, 18: 899-947. 10.1016/0098-3004(92)90029-Q.View ArticleGoogle Scholar
- Zhang G, Spycher N, Xu T, Sonnenthal E, Steefel C: Reactive geochemical transport modeling of concentrated aqueous solutions with TOUGHREACT----Supplement to TOUGHREACT Users' Guide for Pitzer ion-interaction model. Lawrence Berkley National Laboratory. 2006, LBNL-57873, Berkeley, CaliforniaGoogle Scholar
- Zhang G, Spycher N, Sonnenthal E, Xu T, Steefel C: Modeling reactive multiphase flow and transport of concentrated solutions. Journal of nuclear technology. 2008, 164: 180-195.Google Scholar
- Ananthaswarmy J, Atkinson G: Thermodynamics of concentrated electronlyte mixtures, 5. A review of the thermodynamic properties of aqueous calcium chloride in the temperature range 273.15-373.15 K. J Chem Eng Data. 1985, 30: 120-10.1021/je00039a035.View ArticleGoogle Scholar
- Pruess K, Oldenburg C, Moridis G: TOUGH2 User's Guide. 1999, Report LBNL-4 Lawrence Berkeley National Laboratory, Berkeley, CaliforniaView ArticleGoogle Scholar
- Wagner W, Pruß A: The IAPW formulation 1995 for the thermodynamic properties of ordinary water substance for general scientific use. Jour Phys Ref Data. 2002, 31: 387-10.1063/1.1461829.View ArticleGoogle Scholar
- Lasaga AC: Kinetic theory in the earth sciences. 1998, Princeton University Press, Princeton, New JerseyGoogle Scholar
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