AGR 2320 Lecture Notes - Lecture 22: Flocculation, Clay Minerals, Illite
11 Nov 2016
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Agr 2320 lecture 22 types of clay soils and weathering. Additional sheet of oh octahedrally coordinated to mg sandwiched between a 2:1 structure to give a 2:1:1 structure. Figure 1: comparison of soil structures (john lauzon, 2016) Eventually amount of cations in layers will equal to cations in soil water: equilibrium. Happens by random action: cations continually leaving; cations continually coming on exchange sites. Cation exchange capacity is always full: exchanging, but full. Know the change of clay in time due to weathering. Oxides of fe and al ph dependant cation exchange on clay. As ph goes up, cation exchange capacity of soil increases a little bit. As ph goes up, bigger potential to lose h: hydrogen can be released from the oh group, causing overall charge to be a little more ve charged. As ph increases, organic matter in soil increases. On has a lot of calcium and magnesium in soil.
