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Cation‐Exchange Capacity as a Function of Organic Matter, Total Clay, and Various Clay Fractions in a Soil Toposequence
Author(s) -
Wilding L. P.,
Rutledge E. M.
Publication year - 1966
Publication title -
soil science society of america journal
Language(s) - English
Resource type - Journals
SCImago Journal Rank - 0.836
H-Index - 168
eISSN - 1435-0661
pISSN - 0361-5995
DOI - 10.2136/sssaj1966.03615995003000060034x
Subject(s) - cation exchange capacity , soil water , organic matter , clay minerals , clay soil , chemistry , soil science , soil organic matter , mineralogy , geology , organic chemistry
Soil cation‐exchange capacity (CEC) as determined for A and B horizons of Miami, Celina, Crosby, and Brookston soils was statistically partitioned using multiple linear regression analyses into the following sets of components: [1] organic matter (OM) and total clay; and [2] OM, 2‐0.2µ, and <0.2µ clay. Coefficients of multiple correlation ( R ) for independent variables used in regression components [2] are of larger magnitude but not significantly different from components [1]. R values for components [1] range from .76 to .87 and for components [2] from .78 to .92. Organic matter contributes most to the CEC in A horizons whereas <0.2µ clay contributes greatest to the CEC of B horizons for soils of this toposequence. With one exception, 2–0.2µ clay is not significantly correlated with CEC in either A or B horizons. The average CEC of OM for Brookston A horizons is lower than for other toposequence members (154 vs. ca. 200 meq/100 g), whereas for B horizons it is considerably greater (361 vs. ca. 290 meq/100 g). The average CEC of fine clay in B horizons progressively increases with decrease in drainage class, varying from about 70 meq/100 g in Miami to 121 meq/100 g in Brookston.