Mineralization in soils

The inorganic component of soil is dominated by four elements O, Si, Al, and Fe (Jackson, 1964). Together with Mg, Ca, Na, and K they constitute 99% of the soil mineral matter (see Table 8-2). Minerals in soil are divided into primary and secondary minerals. Primary minerals, which occur in igneous, metamorphic, and sedimentary rocks, are inherited by soil... 

Kittrick, J. A. (1977). Mineral equilibria and the soil system. In "Minerals in Soil Environments" (J. B. 

White, A. F. (1995). Chemical weathering rates of silicate minerals in soils. In "Chemical Weathering Rates of Silicate Minerals" (A. F. White and S. L. Brantley, eds), Mineralogical Society of America, Washington, DC, Reviews in Mineralogy 31, 407-461. 

Ogunseitan OA, BH Olson (1993) Effect of 2-hydroxybenzoate on the rate of naphthalene mineralization in soil. Appl Microbiol Biotechnol 38 799-807. 

S. Bjarna.son, Calculation of gross nitrogen immobilization and mineralization in soil. J. Soil Sci. 39 393 (1988). 

Hsu PH (1989) Aluminum hydroxides and oxyhydroxides. In Dixon JB, Weed SB (ed) Minerals in soil environments, 2nd edn, pp 331-378 Inskeep WP, McDermott TR, Fendorf S (2002) Arsenic (V)/(III) cycling in soils and natural waters chemical and microbiological processes. In Frankenberger WT Jr (ed) Environmental chemistry of arsenic. Marcel Dekker, New York, pp 183-215... 

White, A. F., 1995, Chemical weathering rates of silicate minerals in soils. Reviews in Mineralogy 31,407 161. 

At the continental- to subcontinental-scale the relative proportions of major minerals in soils are largely controlled by parent material and climate factors. In turn, the distributions of many major and trace elements are strongly influenced by soil mineralogy, especially the presence or absence of quartz (Eberl Smith 2009 Bern 2009). 

Schwertmann, U. Taylor, R.M. 1989. Iron oxides. In Dixon, J.B. and Weed, S.B. (eds.) Minerals in soil environments, 2ed. Madison, Soil Science Society of America, 379-438. 

Hydrolysis reactions occur by nucleophilic attack at a carbon single bond, involving either the water molecule directly or the hydronium or hydroxyl ion. The most favorable conditions for hydrolysis, e.g. acidic or alkaline solutions, depend on the nature of the bond which is to be cleaved. Mineral surfaces that have Bronsted acidity have been shown to catalyze hydrolysis reactions. Examples of hydrolysis reactions which may be catalyzed by the surfaces of minerals in soils include peptide bond formation by amino acids which are adsorbed on clay mineral surfaces and the degradation of pesticides (see Chapter 22). 

Pignatello JJ. 1986. Ethylene dibromide mineralization in soils under aerobic conditions. AppI Environ Microbiol 51 588-592. 

In Minerals in Soils. Soil Science Society of America, Madison, WI, pp 730-789 Barshad I (1960) Thermodynamics of water adsorption and desorption on montmoriUonite. Qays Clay Miner. 8 84-101... 

Dixon JB (1989) Kaolin and serpentine group minerals. In Dixon JB, Weed SB (eds) Minerals in Soils. Soil Science Society of America, Madison, Wl, pp 468-527 Dress LR, Wilding LP, Smeck NE, Senkayi AL (1989) Silica in Soils Quartz and disordered silica polymorphs. In Dixon JB, Weed SB (eds.) Minerals in Soil Environment, 2edn. Soil Science Society of America, Madison, Wl. 

The following elements are associated with copper-molybdenum mineralization in soils at Tameapa Cu, Mo, Au, Ag, Pb, Zn, V, W, Ni, As, Sb, Bi, and Se. As expected, copper and molybdenum show the strongest response to copper-molybdenum mineralization at both Pico Prieto and Venado. 

Iron oxides in soils have in common that they are of extremely small crystal size and/or low crystal order. This, in combination with their low concentration (only tens g kg in most soils) explains why soil iron oxides have escaped identification for a long time in spite of their obvious existence as seen from the soil colour. In the past, therefore, Fe oxides in surface environments have been considered to be amorphous to X-rays and often called limonite , which mineralogically, is an obsolete term. Furthermore, in order to identify the clay minerals in soils properly, Fe oxides are usually removed before X-ray diffraction methods are applied (Alexander et al., 1939 Mehra Jackson, 1960). 

Chiarizia, R. Horwitz, E.P. (1991) New formulations for iron oxides dissolution. Hydrometallurgy 27 339-360 Childs, C.W Wilson, A.D. (1983) Iron oxide minerals in soils of the Ha apai Group, Kingdom of Tonga. Aust. J. Soil Res. 21 489-503 Childs, C.W. (1992) Ferrihydrite A review of structure, properties and occurrence in relation to soils. Z. Pflanzenemahr. Bodenk. 155 441-448... 

Scheinost, A.C. Chavernas, A. Barron,V. Tor-rent, J. (1998) Use and limitations of second-derivative diffuse reflectance spectroscopy in the visible to near-infrared range to identify and quantify Fe oxide minerals in soils. Clay Min. Soc. 46 528-536... 

Stanjek, H. (2000) Formation processes of ferri-magnetic minerals in soils. Habil.-Schrift Techn. Univ. Miinchen. 162 pp... 

Table 7.2 lists the most common non-silicate minerals in soils. Not included are the common silicate minerals, which are the same as those listed in Table 7.1, with clays... 

Common non-silicate minerals in soils (after shulze [63]). 

Natural occurrences in hydrothermal areas show that the replacement of analcite + quartz by albite probably takes place near 150-180°C (Coombs, et al., 1959) at several hundred meters depth. The observed upper limit of analcite appears to be 100-125°C in deeply buried rocks in Japan 5Km depth). In other rocks for which no temperature data are available analcite can be found to coexist with sodium feldspar (High and Picard, 1965 Iijima and Utada, 1966 Iijima and Hay, 1968 Otalora, 196A Callegari and Jobstribitzer, 1964 Gulbrandsen and Cressman, 1960). Several authors have indicated that analcite replaces other zeolites in buried sequences of rocks (Moiola, 1970 Sheppard, 1970 Iijima and Hay, 1968 Iijima, 1970 Gude and Sheppard, 1967) but this is certainly not the rule since analcite is frequently associated with other zeolites as a primary mineral in soils sediments and sedimentary rocks (Hay, 1966). 

JACKSON (M.L.), TYLER (S.A.) and WILLIS (A.L.), BOURBEAU (G.A.), PENNINGTON (R.P.), 1948. Weathering sequences of clay size minerals in soils and sediments. Joum. Phys. Colloid Chem. J 2, 1237-60. 

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