By Donald L. Sparks
Lower than new editorial course, Advances in Agronomy either maintains its lengthy culture and expands to incorporate leading edge equipment and applied sciences. prime overseas scientists hide themes in plant and soil sciences, biotechnology, terrestrial ecosystems, and environmental concerns.The moment quantity lower than new editorial course, Advances in Agronomy, quantity forty seven specializes in environmental caliber and biotechnology. 4 articles on soil technological know-how conceal acid deposition, chemical shipping, and floor complexation. articles on crop technology survey type fingerprinting and corn evolution. This and similar volumes can be of curiosity to agronomists and biotechnologists in academe, undefined, and executive. Key gains* Acidic deposition in forested soils* Modeling natural and inorganic chemical delivery in soils* floor complexation versions in soil chemical structures* Fingerprinting crop forms* Evolution of corn
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Additional info for Advances in Agronomy, Vol. 47
The congruent dissolution of a primary silicate mineral can be represented as MAISi04 + 4H+ + M+ + A13+ + H4Si04 (18) where M is Ca, Mg, K, Na, or Fe or some combination thereof, and H+ represents a source of protons (N. M. Johnson, 1985). The reaction as written consumes H+, but is not a neutralization reaction because of the release of A13+. , 1985; N. M. , 1990) and can be represented by a combination of dissolution-precipitation reactions Ca(AI2Si2O8)+ 2H+ + 6HOH + Ca2++ 2AI(OH), + 2H,SiO, (anorthite) (19) (gibbsite) Anorthite is only used as an example in Eq.
The large buffer capacity of forest soil organic horizons means that the pH of the soil solution entering the underlying mineral horizons, in most cases, will not be directly influenced by H' inputs from acidic deposition. - and the acidity and basicity of the litter, which is the primary source of the soil organic matter. 2. Cation Exchange and Aluminum Solubility Titration of forest soil mineral horizons results in an S-shaped relationship between pH and the amount of acid or base added in the pH 4-7 range (Federer and Hornbeck, 1985; Magdoff and Bartlett, 1985).
M. , 1985) when plotted on activity ratio diagrams as a function of pH. Chemical models designed to predict changes in the activity of A13+ in soil solution due to acidic inputs often assume that gibbsite is the controlling phase for the activity of A13+ (Reuss and Johnson, 1986; Schecher and Driscoll, 1989). 0. 2 range. 66 for the coefficient of pH in Eq. , 1990). These results suggest that a separate solid phase is not controlling the activity of A13+ in soil solutions, at least in the upper surface horizons (Bloom and Grigal, 1985).
Advances in Agronomy, Vol. 47 by Donald L. Sparks