ArticleThe depletion and regeneration of dissolution-active sites at the mineral-water interface:: I. Fe, Al, and In sesquioxides
Introduction
Mineral dissolution has been the subject of extensive study because of its importance in a variety of geochemical processes ranging from global elemental cycling and climate control to acid rain effects and biochemical strategies for nutrient acquisition. Our understanding of the effects of pH, solution composition, and adsorbed species on dissolution rate is based largely on steady state dissolution measurements. For example, dissolution rates are often related to the concentration of protons or organic (or inorganic) ligands adsorbed to the mineral surface (e.g., Stumm and Wieland, 1990). Such surface complexation approaches to dissolution kinetics are based explicitly on the assumption that the surface is in a steady state configuration; that is, the surface concentration of metal centers participating in dissolution, and their collective overall reactivity toward dissolution, are time independent. Here, in contrast, we utilize pH-jump-induced dissolution transients, caused by temporally changing concentrations and reactivities of dissolution-active surface metal centers, to obtain information about dissolution processes that cannot be obtained from steady state experiments.
Initially elevated dissolution rates that decay to a steady state are a virtually universal observation in mineral dissolution experiments Holt and King 1955, Holdren and Berner 1979, Schott et al 1981, Chou and Wollast 1985, Carroll-Webb and Walther 1988, Knauss et al 1993, Hellmann 1995, Maurice et al 1995, Kraemer and Hering 1997, Malmstrom and Banwart 1997. Occasionally dissolution rates increase to a steady state, e.g., quartz at pH > 10 (Knauss and Wolery, 1988). Such initial transients show that the approach of dissolution rate to steady state takes time, and have been attributed to artifacts of sample preparation Petrovic 1981a, Petrovic 1981b, Schott et al 1981, the formation of altered layers on mineral surfaces Casey and Bunker 1990, Hellmann 1995, or transient adjustments of surface topography or particle size distribution toward a steady state configuration Holdren and Berner 1979, Dibble and Tiller 1981. Rate transients, however, are not limited to the onset of dissolution, but have been reported in response to cycles in pH Chou and Wollast 1984, Spokes and Jickells 1996, Samson and Eggleston 1998, increases in ligand concentration Mast and Drever 1987, Wieland and Stumm 1992, Kraemer and Hering 1997, and changes in electrolyte composition (Sjöberg, 1989). Furthermore, such transients have been shown to contain useful information about dissolution mechanisms. For example, Holt and King (1955) related rapid initial dissolution rates to the adsorption of silicic acid to quartz surfaces, and Chou and Wollast (1984) used pH-jump-induced albite dissolution transients to obtain information about the formation, thickness, and composition of altered or leached layers on the feldspar surface. Similarly, we follow these authors in using nonsteady state phenomena as a window on oxide dissolution mechanisms.
A previous study of nonsteady state hematite dissolution (Samson and Eggleston, 1998) showed that following downward pH-jumps to pH 1, a consistent, reproducible, and regenerable nonsteady state period of elevated dissolution rate occurs and lasts for over 36 h. The results were consistent with the depletion at low pH and regeneration at higher pH of a reservoir of Fe surface sites active for dissolution at pH 1 in response to cycles in pH. Such active sites can be thought of in different ways. We interpreted the data with regard to long-standing crystal growth and dissolution models (e.g., Burton-Cabrera-Frank, BCF; Burton et al., 1951) that assume the existence of “adsorbed nutrient”, e.g., Fe3+ on hematite, that is structurally distinct from metal centers in the solid surface structure. We attributed the transients to the release of this adsorbed Fe.
Here, we report results for nonsteady state dissolution of corundum (α-Al2O3) and cubic indium sesquioxide (In2O3) in response to pH-jumps, compare them to results for hematite (α-Fe2O3), and use the data to test a simple hypothesis: because the same fundamental processes of ligand exchange and detachment of metal centers govern both steady state and nonsteady state dissolution, both the steady state and nonsteady state dissolution rates of these trivalent metal sesquioxides correlate with the water exchange rates of the corresponding aqueous ions. The model originally developed for hematite (Samson and Eggleston, 1998) is refined in order to describe the wider range of nonsteady state behavior defined by the new data. Finally, we reconsider the idea that the amount of solute released in the transients is directly related to the adsorption of nutrient to the oxide surface (e.g., FeIII to hematite, or Al to corundum), and consider whether the amount of adsorbed nutrient involved in transient dissolution is, at the initial higher pH, controlled by equilibrium or by steady state kinetics.
Section snippets
Experimental methods
We used the isostructural minerals α-Al2O3 and α-Fe2O3 (corundum structure, space group Rc), but a third suitable analog (e.g., corundum structure of a metal with a stable oxidation state and known water exchange rate that differs significantly from those of Al3+ and Fe3+) was not readily obtainable. In2O3, which has a cubic structure (space group Ia3), but the same stoichiometry, was taken as the best alternative.
Results
The steady state dissolution rates at pH 1 for the three sesquioxides correlate with the water exchange rates for the hexaaqua ions (Fig. 3). With respect to nonsteady state dissolution following downward pH-jumps to pH 1, there are consistent, reproducible, pH-dependent transients for all three sesquioxides (Fig. 4) as discussed individually below.
The results of downward pH-jump experiments with hematite (Fig. 4a) are described elsewhere (Samson and Eggleston, 1998). Briefly, following a
Discussion
Our hypothesis that steady state dissolution rates correlate with the rates of water exchange for the corresponding aqueous ions is supported by the data (Fig. 3). We have also shown that pH-jumps to pH 1 from higher pH consistently produce transients that are initial-pH-dependent, reproducible, and regenerable (Fig. 4).
Because the hematite and corundum powders were cycled between pH 1 and higher pH, the elevated dissolution rates that occur in response to downward pH-jumps might be interpreted
Conclusions and summary
- 1.
The steady state dissolution rates of α-Fe2O3, α-Al2O3, and In2O3 at pH 1 correlate with the water exchange rates of the corresponding aqueous ions. The range in the dissolution rates for the three phases, however, is considerably less than the 7 orders of magnitude difference in the water exchange rates for the aqueous ions, suggesting that factors other than the inherent properties of the metal may limit the extent to which dissolution rates vary for isostructural (or nearly isostructural)
Acknowledgements
We are grateful to Pradeep Agarwal and Steve Higgins for their valuable assistance with the reactor equations. We also thank Steve Boese for analytical assistance, and three anonymous reviewers for their thorough reviews and helpful comments. Financial support was provided by The National Science Foundation (Grant #EAR-9527031 to CME).
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Present address: Division of Engineering and Applied Sciences, Harvard University, Cambridge, MA 02138 USA.
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Present address: United States Geological Survey, University of NV-Reno, Reno, NV 89557 USA.