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Quantification of Mixed-Layer Clays in Multiple Saturation States Using NEWMOD2: Implications for the Potassium Uplift Hypothesis in the SE United States

Published online by Cambridge University Press:  01 January 2024

Jason C. Austin ,
Daniel D. Richter  and
Paul A. Schroeder Open the ORCID record for Paul A. Schroeder [Opens in a new window]
Jason C. Austin
Affiliation:
Department of Geology, University of Georgia, Athens, GA 30602-2501, USA Nicholas School of the Environment, Duke University, Durham, NC 27708, USA
Daniel D. Richter
Affiliation:
Nicholas School of the Environment, Duke University, Durham, NC 27708, USA
Paul A. Schroeder*
Affiliation:
Department of Geology, University of Georgia, Athens, GA 30602-2501, USA
*
*E-mail address of corresponding author: schroe@uga.edu
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Abstract

Quantification of mineral assemblages in near-surface Earth materials is a challenge because of the often abundant and highly variable crystalline and chemical nature of discrete clay minerals. Further adding to this challenge is the occurrence of mixed-layer clay minerals, which is complicated because of the numerous possible combinations of clay layer types, as defined by their relative proportions and the ordering schemes. The problem of ensuring accurate quantification is important to understanding landscape evolution because mineral abundances have a large influence on ecosystem function. X-ray diffraction analysis of the variable cation-saturated clay fraction in soil and regolith from the Calhoun Critical Zone observatory near Clinton, South Carolina, USA, was coupled with modeling using NEWMOD2 to show that mixed-layer clays are often dominant components in the mineral assemblages. Deep samples in the profile (>6.5 m) contain mixed-layer kaolinite/smectite, kaolinite/illite-like, kaolinite-vermiculite, illite-like/biotite, and illite-like/vermiculite species (with ‘illite-like’ defined herein as Fe-oxidized 2:1 layer structure with a negative layer charge of ~0.75 per unit formula, i.e. weathered biotite). The 2:1 layers in the mixed-layer structures are proposed to serve as exchange sites for K+, which is known to cycle seasonally between plant biomass and subsurface weathering horizons. Forested landscapes have a greater number of 2:1 layer types than cultivated landscapes. Of two nearby cultivated sites, the one higher in landscape position has fewer 2:1 layer types. Bulk potassium concentrations for the forested and two cultivated sites show the greatest abundances in the surface forested site and lowest abundance in the surface upland cultivated site. These observations suggest that landscape use and landscape position are factors controlling the mixed-layer mineral assemblages in Kanhapludults typical of the S.E. United States Piedmont. These mixed-layer clays are key components of the proposed mechanism for K+ uplift concepts, whereby subsurface cation storage may occur in the interlayer sites (with increased negative 2:1 layer charge) during wetter reduced conditions of the winter season and as biomass decay releases cation nutrients. Cation release from the mixed-layer clays (by decreased 2:1 layer charge) occurs under drier oxidized conditions during the growing seasons as biota utilize cation nutrients. The types and abundances of mixed layers also reflect long-term geologic factors including dissolution/alteration of primary feldspar and biotite and the subsequent transformation and dissolution/precipitation reactions that operate within the soil horizons. Thus, the resulting mixed-layer clay mineral assemblages are often complex and heterogeneous at every depth within a profile and across landscapes. X-ray diffraction (XRD) assessment, using multiple cation saturation state and modeling, is essential for quantifying the clay mineral assemblage and pools for cation nutrients, such as potassium, in the critical zone.

Keywords

Biotite weatheringCritical zone observatoryKanhapludultKaoliniteMixed-layer clayPotassium uplift
Type
Article
Information
Clays and Clay Minerals , Volume 68 , Issue 1 , February 2020 , pp. 67 - 80
Copyright
Copyright © Clay Minerals Society 2020

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References

Austin, J., Perry, A., Richter, D. D., & Schroeder, P. (2018). Modifications of 2: 1 clay minerals in a kaolinite-dominated Ultisol under changing land-use regimes. Clays and Clay Minerals, 66, 61–73.CrossRefGoogle Scholar
Bacon, A. R. (2014). Pedogenesis and anthropedogenesis on the southern piedmont. PhD thesis. Durham: Duke University.Google Scholar
Bacon, A. R., Richter, D. D., Bierman, P. R., & Hood, D. H. (2012). Coupling meteoric 10Be with pedogenic losses of 9Be to improve soil residence time estimates on an ancient North American soil. Geology, 40, 847–850.CrossRefGoogle Scholar
Balogh-Brunstad, Z., Keller, C. K., Bormann, B.T., O'Brien, R., Wang, D., & Hawley, G. (2008). Chemical weathering and chemical denudation dynamics through ecosystem development and disturbance. Global Biogeochemical Cycles, 22, 11.CrossRefGoogle Scholar
Barcellos, D., Cyle, K. T., & Thompson, A. (2018). Faster redox fluctuations can lead to higher iron reduction rates in humid forest soils. Biogeochemistry, 137, 367–378.CrossRefGoogle Scholar
Barnhisel, R. I., & Bertsch, P. M. (1989). Chlorites and hydroxyinterlayered vermiculite and smectite. In Dixon, J. B. & Weed, S. B. (Eds.), Minerals in Soil Environments (pp. 729–788). Madison, Wisconsin: Soil Science Society of America.Google Scholar
Barre, P., Montagnier, C., Chenu, C., Abbadie, L., & Velde, B. (2008). Clay minerals as a soil potassium reservoir: Observation and quantification through X-ray diffraction. Plant and Soil, 302, 213–220.CrossRefGoogle Scholar
Barre, P., Velde, B., & Abbadie, L. (2007a). Dynamic role of “illite-like” clay minerals in temperate soils: Facts and hypotheses. Biogeochemistry, 82, 77–88.CrossRefGoogle Scholar
Barre, P., Velde, B., Catel, N., & Abbadie, L. (2007b). Soil-plant potassium transfer: Impact of plant activity on clay minerals as seen from X-ray diffraction. Plant and Soil, 292, 137–146.CrossRefGoogle Scholar
Billings, S.A., Hirmas, D., Sullivan, P.L., Lehmeier, C.A., Bagchi, S., Min, K., Brecheisen, Z., Hauser, E., Stair, R., Flournoy, R., & Richter, D.D. (2018). Loss of deep roots limits biogenic agents of soil development that are only partially restored by decades of forest regeneration. Elementa – Science of the Anthropocene, 6.CrossRefGoogle Scholar
Cornu, S., Montagne, D., Hubert, F., Barre, P., & Caner, L. (2012). Evidence of short-term clay evolution in soils under human impact. Comptes Rendus Geoscience, 344, 747–757.CrossRefGoogle Scholar
Diaz, M., Robert, J. L., Schroeder, P. A., & Prost, R. (2010). Farinfrared study of the influence of the octahedral sheet composition on the K+-layer interactions in synthetic phlogopites. Clays and Clay Minerals, 58, 263–271.CrossRefGoogle Scholar
Dumon, M., & Van Ranst, E. (2016). Pyxrd v0.6.7: A free and open-source program to quantify disordered phyllosilicates using multi-specimen X-ray diffraction profile fitting. Geoscientific Model Development, 9, 41–57.CrossRefGoogle Scholar
Gier, S., Ottner, F., & Johns, W. D. (1998). Layer-charge heterogeneity in smectites of I-S phases in pelitic sediments from the molasse basin, Austria. Clays and Clay Minerals, 46, 670–678.CrossRefGoogle Scholar
Hillier, S., & Butler, B. (2018). New XRD data-based approaches to soil mineralogy. Spectroscopy, 33, 34–36.Google Scholar
Hochella, M. F., Mogk, D. W., Ranville, J., Allen, I. C., Luther, G. W., Marr, L. C., McGrail, B. P., Murayama, M., Qafoku, N. P., Rosso, K. M., Sahai, N., Schroeder, P. A., Vikesland, P., Westerhoff, P., & Yang, Y. (2019). Natural, incidental, and engineered nanomaterials and their impacts on the Earth system. Science, 363, 1414.CrossRefGoogle ScholarPubMed
Huggett, J. M., & Cuadros, J. (2005). Low-temperature illitization of smectite in the late eocene and early oligocene of the Isle of Wight (Hampshire Basin), UK. American Mineralogist, 90, 1192–1202.CrossRefGoogle Scholar
Jenny, H. (1941). Factors of Soil Formation: A system of Quantitative Pedology (p. 281). New York: Dover Publications.Google Scholar
Jobbagy, E. G., & Jackson, R. B. (2004). The uplift of soil nutrients by plants: Biogeochemical consequences across scales. Ecology, 85, 2380–2389.CrossRefGoogle Scholar
Joussein, E., Petit, S., Churchman, J., Theng, B., Righi, D., & Delvaux, B. (2005). Halloysite clay minerals – A review. Clay Minerals, 40, 383–426.CrossRefGoogle Scholar
Lagaly, G. (1982). Layer charge heterogeneity in vermiculites. Clays and Clay Minerals, 30, 215–222.CrossRefGoogle Scholar
Lanson, B. (2011). Modelling of X-ray diffraction profiles: Investigation of defect lamellar structure crystal chemistry. Pp. 151–190 in: Layered Mineral Structures and their Application in Advanced Technologies (Brigatti, M.F., and Mottana, A., editors). 11, European Mineralogical Union and the Mineralogical Society of Great Britain & Ireland, London.CrossRefGoogle Scholar
Lanson, B., Sakharov, B. A., Claret, F., & Drits, V. A. (2009). Diagenetic smectite-to-illite transition in clay-rich sediments: A reappraisal of X-ray diffraction results using the multi-specimen method. American Journal of Science, 309, 476–516.CrossRefGoogle Scholar
Le Dred, R. (1978). Formation de complexes mica-vermiculitehalogenure de metal alcalin. Clay Minerals., 13, 187–197.CrossRefGoogle Scholar
Lybrand, R., Austin, J., Schroeder, P.A., Zaharescu, D., & Gallery, R. (2017). Cross-scale perspectives on mineral weathering in the critical zone. Paper no. 195–13 in: Abstracts with Programs - Geological Society of America. 49, Seattle, Washington, USA.CrossRefGoogle Scholar
Lybrand, R.A., Austin, J.C., Fedenko, J., Gallery, R.E., Rooney, E., Schroeder, P.A., Zaharescu, D.G., & Qafoku, O. (2019). A coupled microscopy approach to assess the nano-landscape of weathering. Scientific Reports, 9.CrossRefGoogle Scholar
MacEwan, D. M. C., & Wilson, M. J. (1980). Interlayer and intercalation complexes of clay minerals. In: G.W. Brindley & G. Brown (Eds.), Crystal Structures of Clay Minerals and their X-ray Identification. London (pp. 197–248).: Mineralogical Society.Google Scholar
Meunier, A. (2007). Soil hydroxy-interlayered minerals: A re-interpretation of their crystallochemical properties. Clays and Clay Minerals, 55, 380–388.CrossRefGoogle Scholar
Officer, S. J., Tillman, R. W., Palmer, A. S., & Whitton, J. S. (2006). Variability of clay mineralogy in two New Zealand steep-land topsoils under pasture. Geoderma, 132, 427–440.CrossRefGoogle Scholar
Ramirez, S., Righi, D., & Petit, S. (2005). Alteration of smectites induced by hydrolytic exchange. Clay Minerals, 40, 15–24.CrossRefGoogle Scholar
Reynolds, R. C. Jr. (1980). Interstratified clay minerals. In Brindley, G. W. & Brown, G. (Eds.), Crystal Structures of Clay Minerals and their X-ray Identification (pp. 249–303). London: Mineralogical Society.CrossRefGoogle Scholar
Reynolds, R. C. (1985). Newmod a computer program for the calculation of one-dimensional X-ray diffraction patterns of mixedlauered clays. Hanover, New Hampshire, USA, Reynolds Jr.Google Scholar
Reynolds, R. C. (1986). The Lorentz-polarization factor and preferred orientation in oriented clay aggregates. Clays and Clay Minerals, 34, 359–367.CrossRefGoogle Scholar
Richter, D., & Markewitz, D. (1995). How deep is soil? BioScience., 45, 600–699.CrossRefGoogle Scholar
Schroeder, P. A. (1992). Far-infrared study of the interlayer torsional-vibrational mode of mixed-layer illite smectites. Clays and Clay Minerals, 40, 81–91.CrossRefGoogle Scholar
Schroeder, P. A. (2018). Clays in the Critical Zone. Cambridge, UK: Cambridge University Press.CrossRefGoogle Scholar
Schroeder, P. A., Kim, J. G., & Melear, N. D. (1997). Mineralogical and textural criteria for recognizing remnant Cenozoic deposits on the Piedmont: Evidence from Sparta and Greene County, Georgia, USA. Sedimentary Geology, 108, 195–206.CrossRefGoogle Scholar
Smith, D. W. (1977). Ionic hydration enthalpies. Journal of Chemical Education, 54, 540.CrossRefGoogle Scholar
Stucki, J. W. (1988). Structural iron in smectites. In: Stucki, J. W., Goodman, B. A., & Schwertmann, U. (Eds.), Iron in Soils and Clay Minerals (Vol. 217, pp. 625–676). Springer: Dordrecht, The Netherlands: Springer.CrossRefGoogle Scholar
Toby, B. H. (2006). R factors in Rietveld analysis: How good is good enough? Powder Diffraction, 21, 67–70.CrossRefGoogle Scholar
Trimble, S.W. (2008). Man-induced soil erosion on the southern Piedmont, 1700–1970. pp. 70. Soil and Water Conservation Society, Department of Geography, UCLA, Los Angeles, California, USA.Google Scholar
Yuan, H., & Bish, D. L. (2010). NEWMOD plus, a new version of the NEWMOD program for interpreting X-ray powder diffraction patterns from interstratified clay minerals. Clays and Clay Minerals, 58, 318–326.CrossRefGoogle Scholar
Viennet, J.-C., Hubert, F., Ferrage, E., Tertre, E., Legout, A., & Turpault, M.-P. (2015). Investigation of clay mineralogy in a temperate acidic soil of a forest using X-ray diffraction profile modeling; beyond the HIS and HIV description. Geoderma, 241, 75–86.CrossRefGoogle Scholar
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