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Solubility and Dissolution Kinetics of Dolomite in Ca–Mg–HCO3/CO3 Solutions at 25°C and 0.1 MPa Carbon Dioxide

Leslie A. Shermana and Phillip Barakb

a Dep. of Chemistry, Washington College, 300 Washington Ave., Chestertown, MD 21620-1197 USA
b Dep. of Soil Science, Univ. of Wisconsin-Madison, 1525 Observatory Dr., Madison, WI 53706-1299 USA



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Fig. 1 Literature values of the dolomite solubility product

 


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Fig. 2 Dissolution and precipitation in dolomite-seeded Ca–Mg–HCO3/CO3 solutions and deionized water: change in Ca2+ concentration over values in control unseeded solutions ({Delta}Ca2+) against change in alkalinity over values in control unseeded solutions ({Delta}Alk)

 


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Fig. 3 Calculated pIAPcalcite [= -log (Ca2+)(CO2-3)] in dolomite-seeded against control unseeded Ca–Mg–HCO3/CO3 solutions with 1:1, 2:1, and 4:1 Mg/Ca at 7, 14, 28, 56, 112, 224, 448, and 672 d. Dashed line indicates no difference between seeded and unseeded control

 


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Fig. 4 Calculated pIAPcalcite in calcite-seeded against control unseeded Ca–Mg–HCO3/CO3 solutions with 1:1, 2:1, and 4:1 Mg/Ca at 7, 14, 28, 56, 112, 224, and 448 d. Dashed line indicates no difference between seeded and unseeded control

 


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Fig. 5 Calculated pIAPdolomite [= -log (Ca2+)(Mg2+)(CO2-3)2] in dolomite-seeded against control unseeded Ca–Mg–HCO3/CO3 solutions with 1:1, 2:1, and 4:1 Mg/Ca at 7, 14, 28, 56, 112, 224, 448, and 672 d. Dashed line indicates no difference between seeded and unseeded control

 


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Fig. 6 Dissolution of dolomite in undersaturated Ca–Mg–HCO3–CO3 solutions with 1:1 Mg/Ca and in deionized water: (a) Change in Ca2+ over values in control unseeded solutions against change in Mg2+ concentrations over values in control unseeded solutions ({Delta}Ca2+ and {Delta}Mg2+, respectively). (b) Change in the sum of Ca2+ and Mg2+ concentrations over values in control unseeded solutions({Delta}Ca2+ + {Delta}Mg2+) against change in alkalinity over values in control unseeded solutions ({Delta}Alk)

 


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Fig. 7 Evaluation of successive reaction kinetic model of Chou et al. (1989) based on dolomite dissolution near equilibrium. Rate of change in alkalinity in dolomite-seeded Ca–Mg–HCO3–CO3 solutions, pIAPdolomite ranging from 17.0 to 19.0, plotted against (H+)2/(Ca2+)(HCO-3)

 


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Fig. 8 Relationship between the rate of change in alkalinity in dolomite-seeded Ca–Mg–HCO3/CO3 solutions and pIAPdolomite. Control lines are 95% confidence and prediction lines from the unseeded Ca–Mg–HCO3/CO3 solutions, corresponding with the hypothesis of no alkalinity change due to dolomite dissolution. Lines connect individual dolomite-seeded solutions from 0 to 672 d

 





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