Other
Scientific paper
Dec 1983
adsabs.harvard.edu/cgi-bin/nph-data_query?bibcode=1983gecoa..47.2233s&link_type=abstract
Geochimica et Cosmochimica Acta, vol. 47, Issue 12, pp.2233-2240
Other
19
Scientific paper
Iron silicate minerals (bronzite, fayalite), exposed to aqueous dissolution in the laboratory for up to 60 days at room temperature and pH 1, 1.5, and 6, have been studied for evidence of changes in surface composition, using XPS, and these results compared with those obtained from solution chemical analysis. In the absence of dissolved O 2 or at low pH (1-1.5) dissolution proceeds congruently after the initial formation of a thin (<10 Å) protonated surface layer depleted in Fe relative to Si. This layer is unstable and does not grow with time as attested to by long term congruent dissolution and by the formation of an amorphous silica surficial breakdown product at pH 1 and 1.5. In bronzite the layer is also slightly depleted in Mg but much less than it is in Fe due to the preferential occupation by Fe +2 of more weakly bonded M 2 sites. The behavior of the layer is similar to that found earlier on iron-free pyroxene ( et al. , 1981); in other words, because of its thinness and instability it is not diffusion-inhibiting or protective toward dissolution. In the presence of dissolved O 2 , as would be the case in most weathering solutions, dissolution of bronzite and fayalite results in the formation of two surface layers whose compositions were deduced by measurements of XPS binding energies. The outer layer, consisting of hydrous ferric oxide, is readily removed by ultrasonic cleaning and, most likely, is not protective toward dissolution. The inner layer consists of Fe +3 in a protonated or hydroxylated silicate (Mg-silicate in the case of bronzite) matrix. This layer appears to impede dissolution over the time scale of the experiment as attested to by parabolic dissolution rates. However, the layer does not continue to grow on the time scale of weathering because ultrasonically cleaned soil grains ( and , 1982) exhibit surface compositions similar to those found in the present month-long laboratory experiments. In other words, a thick , highly altered, diffusion-inhibiting, protective surface layer does not form at the acidic pH of most soils.
Berner Robert A.
Schott Jacques
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