Chemical and Clay Mineral Properties of a Red‐Yellow Podzolic Soil Derived from Muscovite Schist

Rich, C. I.; Obenshain, S. S.

doi:10.2136/sssaj1955.03615995001900030021x

Cited by 142 publications

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“…Nonexchangeable hydroxy-metal polymers (dominantly A1) in interlayers of soil vermiculite and smectite retard collapse of the basal spacing toward 1.0 nm with heat (MacEwan, 1950;Brown, 1953;Rich and Obenshain, 1955;Barnhisel and Bertsch, 1989). The resultant minerals are commonly referred to as hydroxy-interlayered vermiculite (HIV) or smectite (HIS).…”

Section: Introductionmentioning

confidence: 99%

“…Mechanisms and conditions of polymer formation within interlayers of vermiculite (Rich, 1960;Hsu and Bates, t 964) and montmoriUonite (Shen and Rich, 1962;Brydon and Kodama, 1966) have been studied via artificial synthesis of polymers within interlayers. Many soils of humid regions (i.e., the southeastern U.S.) contain abundant HIV in clay fractions (Fiskell and Perkins, 1970;Carlisle et al, 1978Carlisle et al, , 1981Carlisle et al, , 1985Carlisle et al, , 1988, particularly in near-surface horizons (Rich and Obenshain, 1955;Bryant and Dixon, 1963;Rich, 1968;Carlisle and Zelazny, 1973;Harris et aL, 1989).…”

Section: Introductionmentioning

confidence: 99%

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Dehydration of Hydroxy-Interlayered Vermiculite as a Function of Time and Temperature

Harris

1992

Clays and clay miner.

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Abstract--Nonexchangeable polymers in interlayers of expansible phyUosilicates influence thermal dehydration in ways not completely understood. Thermal dehydration of hydroxy-interlayered vermiculite (HIV) from Florida soils, for example, results in irreversible doo~ shifts. This study was conducted to characterize HIV dehydration as a function of time (t) and temperature (T), and to determine how reversibility of dehydration is affected by elevated T. Clay-sized HIV from 3 soils was heated incrementally and d-spacing shifts (Ad) were monitored by X-ray diffraction (XRD) at low relative humidity (RH). Samples were then mounted on a metal heating strip in the XRD focal plane and scanned repeatedly at constant T levels to monitor hd with t. Finally, Ad in response to RH shifts from <5% to >85% was determined at 25"C and at elevated temperatures. Incremental heating revealed a Ad plateau roughly corresponding to the z dimension of hexameric octahedrally coordinated AL The initial slope of Ad-vs-t curves increased with T. The same maximum Ad reached at 200"C was reached at 160"C, but more slowly. All samples exhibited reversible and irreversible dehydration, the former being attributable to sites in equilibrium with external vapor and the latter to sites requiring heat for desorption. Reversible sites were not perturbed by moderate heating, but were apparently eliminated by polymer dehydroxytation. The dehydration behavior of HIV could be explained by steric resistance of water vapor diffusion within a tortuous interlayer polymeric network. Alternatively, new polymer/oxygen-surface bonds exceeding the hydration energy of interlayer components could form via heat-induced re-articulation of polymer/oxygensurface bonds at smaller basal spacings.

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Section: Introductionmentioning

confidence: 99%

Section: Introductionmentioning

confidence: 99%

Dehydration of Hydroxy-Interlayered Vermiculite as a Function of Time and Temperature

Harris

1992

Clays and clay miner.

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“…This »pH-dependent acidity» which is usually supposed to be chiefly caused by weak acidic groups of organic matter, may be partly attributed to positively charged hydroxy-Al polymers. These complexes may be sorbed as surface coatings on soil particles, or they may block interlayer spaces of 2:1 clay minerals (Rich and Obenshain 1955, Barshad 1960, Clark 1964b, Coleman et al 1964, Schwertmann and Jackson 1964, de Villiers and Jackson 1967. Also part of the exchange sites of organic matter may be countered by fixed Al-or Al-hydroxy ions (Keränen 1946, Schnitzer and Skinner 1963, Clark 1964b, Schnitzer 1965, Pionke and Corey 1967, McLean and Owen 1969.…”

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confidence: 99%

Aluminium and acidity in Finnish soils

Kaila

1971

AFSci

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Abstract. In the present study an attempt was made to study by statistical methods the proportion of Al of the exchange acidity of 298 soil samples of various kind, and to what extent the titratable nonexchangeable acidity in these soils is connected with Al, when Al soluble in Tamm's acid oxalate was used as its indicator.Unbuffered N KCI replaced Al only from soil samples with a pH less than 5.3 in 0.01 M CaCl 2 . In this part of the material, Al corresponded, on the average, to one third of the exchange acidity of mineral soil samples, and to 16 per cent of that of organic soils. The amount of Al was usually the higher the lower the soil pH, but the correlation was close only in the group of clay soils.Titratable nonexchangeable acidity was estimated as the difference of the amount of acidity neutralized at pH 8.2 and the corresponding amount of exchange acidity replaced by unbuffered KCI. In 100 clay soil samples it was, on the average, 12.0 ± I*3 me/100 g, in 42 samples of silt and loam soils 8.8 ± 1.8 me/100 g, in 99 sandy soils 8.9 ±l.l me/ 100 g and in 57 organic soils 49.1 ± 6.8 me/100 g.There was no correlation between titratable nonexchangeable acidity and the clay content within various soil groups. In the clay soils exalate soluble Al alone explained 78.3 %, in the silt and loam soils 59.8 %, in the sandy soils 6.5 %, and in the organic soils 0.6 % of the variation in titratable nonexchangeable acidity. Taking into account the content of organic C increased the rate of explanation only to 82.1 % in clay soils, to 84.1 % in silt and loam soils, to 83,1 % in sandy soils, and to 63.7 % in the organic soils. Further, adding the soil pH increased the rate of explanation 5.8 to 9.6 per cent units in various soil groups, but considering of oxalate soluble Fe did no more distinctly increase the part of variation explained, except in the organic soils. Regression equations were calculated for the relationship of these variables.According to the partial correlation coefficients and to the the relative importance of oxalate soluble Al in explaining the variation in titratable nonexchangeable acidity was in the clay soils higher than even that of organic G content, but in the other mineral soil groups it was less important than both C content and pH; in the organic soils even oxalate soluble Fe appeared to be slightly more important.Modern concepts of soil acidity emphasize the role of aluminium. The exchange acidity replaced on leaching with unbuffered solution ofa neutral salt is claimed to be mainly due to monomeric trivalent aluminium ions (Coleman et al. 1959, Jackson 1963, Chernov 1964, at least in soils low in organic matter (Schwertmann 1961 McLean and Owen 1969). These forms of aluminium are not exchangeable with a neutral salt, but they are proton donors or OH acceptors, which will increase the consumption of base when acid soils are titrated. Hydroxy-Fe polymers are supposed to react in a similar way.In the present work an attempt is made to study with statistical methods to what extent titratable no...

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“…The coarse clay (2-0.2 p, Fig. 1) also contains small amounts of heat-stable chlorite along with small amounts of an intergradient, aluminous, chlorite-vermiculitemontmorillonite material (not heat stable) (Rich and Obenshain, 1955;Klages and White, 1957;Tamura, 1958;Dixon and Jackson, 1959) which decreases in abundance from the A horizon downward in the profile. Major minerals in the medium clay (0.2-0.08 p, Fig.…”

Section: Resultsmentioning

confidence: 99%

Chemical Weathering of Layer Silicate Clays in Loess-Derived Tama Silt Loam of Southwestern Wisconsin

Glenn

1959

Clays clay miner. (Natl. Conf. Clays Clay Miner.)

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Chemical weathering of layer silicate clay minerals in the major horizons of the Tama silt loam Prairie soil profile waa followed down to 10 ft, where the calcareous parent loeas was encountered, and on down to a depth of 13 ft. The predominant constituents of the clay fraction (-2 p) a t all depths in the soil profile were montmorillonite (42 percent) and illite (20 percent), although vermiculite (12 percent), kaolinite (6 percent) and amorphous material (16 percent) were a h in fair abundance. Deposition of secondary interlayer alumina was appreciable in the uppermost soil horizons but became less in amount in the deeper soil horizons. Quartz was not found in the clay fractions of less than 0 . 2~ in diameter a t any depth in the soil profile, although both quartz and feldspars occurred in the coaree clay.Vermiculite decreased from about 18 percent in the coarse clay and 6 percent in the fine clay of the deeper calcareous horizons to small amounts toward the soil surface, disappearing altogether in the fine clay (-0.08 p). Little variation was found in the montmorillonite percentage of the clay in the subsoil and lower horizons (64 to 76 percent of the fine clay), but a decreage in the 18A difFraction intensity of montmorillonite concurrent with an increme in amorphous silica and alumina (16 to 27 percent of the fine clay) waa obsemed in the upper, acid, soil horizons, suggesting that montmorillonite is not a stable weathering product in the latter. Elemental analyses of the fine clays showed about 1.1 out of 4 octahedral positions to be Fe, 2.6 to be Al, and 0.4 to be Mg. A slight decrease in Fe and increase in Al in the montmorillonite octahedral Sttructure occurred progressively in approaching the more intensely weathered zones near the soil surface.The results suggest that dioctahedrsl mantmorillonite has formed to considerable extent in both the calcareous and noncalcareous horizons by chemical weathering of trioctahedral ferromagnesian mica, through a vermiculite intermediate stage. The decrease in amount of the silt fractions of density greater than 2.66 g / c d (found to be composed mainly of biotite, chlorite, and amphiboles) in going from the calcareous horizons toward the soil surface approximately equalled the increase in montmoriuonite percentage of the soil, suggesting that mont&orionite of the loess originated by chemical weathering of the ferromannesian minerals of the silt. The genesis of the loessial montmorillonite begins long berore the free CaCOs has been leacged out (6 percent montmorillonite in the loess a t 13 ft) and continues to a maximum (14 percent) in the B horizon. Some eluviation of montmorillonite from the A horizon into the B horizon was evident.

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Chemical and Clay Mineral Properties of a Red‐Yellow Podzolic Soil Derived from Muscovite Schist

Cited by 142 publications

References 0 publications

Dehydration of Hydroxy-Interlayered Vermiculite as a Function of Time and Temperature

Dehydration of Hydroxy-Interlayered Vermiculite as a Function of Time and Temperature

Aluminium and acidity in Finnish soils

Chemical Weathering of Layer Silicate Clays in Loess-Derived Tama Silt Loam of Southwestern Wisconsin

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