Page 103 - Geothermal Energy Renewable Energy and The Environment
P. 103
88 Geothermal Energy: Renewable Energy and the Environment
Lasaga, A. C. 1986. “Metamorphic Reaction Rate Laws and Development of Isograds.” Mineralogical Magazine
50:359–73.
Lasaga, A. C., J. M. Soler, J. Ganor, T. E. Burch, and K. L. Nagy. 1994. “Chemical Weathering Rate Laws and
Global Geochemical Cycles.” Geochimica Cosmochimica Acta 58:2361–86.
Meike, A., and W. E. Glassley. 1990. “In-Situ Observation of the Alpha/Beta Cristobalite Transition
Using High Voltage Electron Microscopy.” Materials Research Society Symposium Proceedings V
176:631–39.
Palmer, D. A., R. Fernandez-Prini, and A. H. Harvey, ed. 2004a. Aqueous Systems at Elevated
Temperatures and Pressures: Physical Chemistry in Water, Steam and Hydrothermal Solutions. London:
Elsevier, Ltd.
Palmer, D. A., J. M. Simonson, and J. P. Jensen. 2004b. “Partitioning of Electrolytes to Steam and Their
Solubility in Steam.” Chapter 12 in Aqueous Systems at Elevated Temperatures and Pressures: Physical
Chemistry in Water, Steam and Hydrothermal Solutions, eds. D. A. Palmer, R. Fernandez-Prini, and A. H.
Harvey, 409–41. London: Elsevier, Ltd.
Reed, M. J., and R. H. Mariner. 1991. Quality Control of Chemical and Isotopic Analyses of Geothermal Water
Samples. Proceedings, 16th Workshop on Geothermal Reservoir Engineering, Stanford University, SGP-
TR-134, pp. 9–13.
Steefel, C. I., D. J. DePaolo, and P. Lichtner, P. 2005. “Reactive Transport Modeling: An Essential Tool and
New Research Approach for the Earth Sciences.” Earth and Planetary Science Letters 15:539–58.
Steefel, C. I., and A. C. Lasaga. 1994. “A Coupled Model for Transport of Multiple Chemical Species and Kinetic
Precipitation/Dissolution Reactions with Application to Reactive Flow in Single Phase Hydrothermal
Systems.” American Journal of Science 294:529–92.
Steefel, C. I., and S. B. Yabusaki. 1996. “OS3D/GIMRT: Software for Modeling Multicomponent-
Multidimensional Reactive Transport.” User’s Manual and Programmer’s Guide, Version 1.0.
Velbel, M. A. 1989. “Effect of Chemical Affinity on Feldspar Hydrolysis Rates in Two Natural Weathering
Systems.” Chemical Geology 78:245–53.
Whittaker, E. J. W., and R. Muntus. 1970. “Ionic Radii for Use in Geochemistry.” Geochmica et Cosmochimica
Acta 34:945–66.
Wood, B. J., and J. V. Walther. 1983. “Rates of Hydrothermal Reaction.” Science 222:413–15.
Xu, T., and K. Pruess. 2001. “Modeling Multiphase Non-Isothermal Fluid Flow and Reactive Geochemical
Transport in Variably Saturated Fractured Rocks: 1. Methodology.” American Journal of Science
301:16–33.
sIdebar 5.1 water analyses
Most reported chemical analyses of water are reported in mg/kg of solution, which equals parts per million (ppm) by
weight, or in mg/l of solution. However, most chemical calculations are carried out using moles/kg of solvent (which
can be either steam or liquid water). Moles/kg of solvent is called molality, and the unit is molal, abbreviated m.
Using a variety of methods, it has been established that one mole of a substance contains 6.0221e23 atoms (or
molecules), which is often called Avogadro’s number. The gram formula weight of a substance, also known as the
molecular weight, is the mass, in grams, of Avogadro’s number of atoms of that substance. These masses have been
tabulated for known elements and compounds and can be accessed either in reference materials or online. An
excellent reference for molecular weights of compounds is the National Institute of Standards and Technology (NIST)
(http://www.nist.gov and http://webbook.nist.gov/chemistry/).
Converting from mg/kg of solute species i to the molal concentration of i requires calculating the number of
moles of i in the solution and multiplying that quantity by the amount of solvent in 1 kg of the solution:
molal conc. of i = [(mg/kg i )/(1000 × mol. wt. of i)] × (1000/(1000-∑(z)/1000), (5S.1)
where ∑(z) is the sum of the concentration of all dissolved species.
Conversions such as this, where the number of moles of a species is determined, is an important first step in
establishing the quality of an analysis. A poor quality analysis can lead to miscalculations of reservoir temperature or
other important resource estimates, which can become costly errors. An important test of the quality of an analysis
is to determine the charge balance. Since all solutions are electrically neutral, the total negative charge attributable
to the number of moles of anions must exactly match the total positive charge attributable to the number of moles
of cations. For example, in a chemical analysis of a water that has only dissolved salt (i.e., halite = NaCl), the only
solutes in the water will be sodium (Na ) and chlorine (Cl ) ions and a negligible amount of NaCl (aq). If the analysis
+
–
+
is of high quality, the number of moles of Na multiplied by the charge on the sodium atom (i.e., 1.0) computed
from the reported concentrations should be within a few percentage of the computed number of moles of Cl mul-
–
tiplied by the charge on the chlorine atom (i.e., –1.0). If the difference is greater than 10%, the analysis should be
considered inadequate and not used. For more complex solutions, the total positive and negative charges (computed