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Kaolinite and Halloysite Derived from Sequential Transformation of Pedogenic Smectite and Kaolinite-Smectite in a 120 ka Tropical Soil Chronosequence

Published online by Cambridge University Press:  01 January 2024

P. C. Ryan ,
F. J. Huertas ,
F. W. C. Hobbs  and
L. N. Pincus
P. C. Ryan*
Affiliation:
Geology Department, Middlebury College, Middlebury, Vermont 05753, USA Instituto Andaluz de Ciencias de la Tierra (CSIC-Universidad de Granada), 18100, Armilla, Granada, Spain
F. J. Huertas
Affiliation:
Instituto Andaluz de Ciencias de la Tierra (CSIC-Universidad de Granada), 18100, Armilla, Granada, Spain
F. W. C. Hobbs
Affiliation:
Geology Department, Middlebury College, Middlebury, Vermont 05753, USA Department of Materials Science and Engineering, University of Wisconsin, Madison, Wisconsin 53706, USA
L. N. Pincus
Affiliation:
Geology Department, Middlebury College, Middlebury, Vermont 05753, USA School of Forestry and Environmental Studies, Yale University, New Haven, Connecticut 06511, USA
*
*E-mail address of corresponding author: [email protected]
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Abstract

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Tropical soils range from nutrient-depleted lateritic soils rich in halloysite or kaolinite to Inceptisols rich in interstratified kaolinite-smectite (K-S), smectite, or related 2:1 clays. Given the strong influence of clay minerals on tropical soil quality, better understanding of factors influencing their occurrence is important for modeling and managing tropical environments. This study examines the alteration of smectite to kaolinite by way of intermediate K-S and halloysite in a 120 ka moist tropical chronosequence. Iron-rich smectite (11.6 ± 2.2% Fe2O3) is the dominant mineral in Holocene soils (1–8 ka) originating from sediments rich in plagioclase and clinopyroxene. The cation exchange capacity (CEC) of smectite is 54–84 cmolc/kg and pH is 6.1 to 7.4. Within 50 ka, smectite fixes Al-hydroxy complexes into interlayers, K+ is retained preferentially over Ca2+, and 2:1 layers are stripped of tetrahedral sheets; the resulting K-S inherits flaky smectite crystal habit and the 2:1 layers — which only expand partially — include Al-hydroxy smectite and some illite-like layers. After 50 ka, the dominant mineral is K-S, the CEC is 18–28 cmolc/kg, and the pH is 5.3. Flaky Fe-kaolinite with ~10% residual smectite layers and halloysite (7.4% Fe2O3) also occur in 50 ka soil. The 120 ka soils are dominated by flaky Fe-kaolinite (<10% residual smectite layers) and halloysite (4.9% Fe2O3), and Fe-poor hexagonal kaolinite also occurs (5–10% of soil). The CEC is 11–16 cmolc/kg and the pH is 4.7–5.3.

Changes in crystal chemistry of the soil clays (decreasing Fe, Mg, Ca, and K; increasing Al) over time reflects two reaction mechanisms: (1) cell-preserved transformation of smectite layers to kaolinite layers that accompanies conversion of smectite to K-S and eventually kaolinite; this results in the formation of flaky Fe-rich kaolinites after 50 ka; and (2) dissolution of K-S followed by crystallization of halloysite. Neoformation of hexagonal kaolinite and/or halloysite with low Fe (<3% Fe2O3) follows dissolution of Fe-kaolinite or halloysite after 100 ka. This sequence is probably common in moist tropical soils and these findings may inform modeling of soil composition in tropical landscapes where tectonic, volcanic, or geomorphic activity periodically exposes unweathered parent material, producing a range of soil ages.

Keywords

ChronosequenceHalloysiteInterstratifiedKaoliniteSmectiteSoilSoil AgeTropical
Type
Article
Information
Clays and Clay Minerals , Volume 64 , Issue 5 , October 2016 , pp. 639 - 667
Copyright
Copyright © Clay Minerals Society 2016

Footnotes

This paper is published as part of a special section on the subject of ‘Clays in the Critical Zone,’ arising out of presentations made during the 2015 Clay Minerals Society-Euroclay Conference held in Edinburgh, UK.

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