Argillic Horizons in Modern Loess Soils in an Ustic Soil Moisture Regime: Comparative Studies in Forest-Steppe and Steppe Areas from Eastern Europe and the United States

Bronger, A.

doi:10.1007/978-1-4612-3030-4_2

Cited by 32 publications

(12 citation statements)

References 45 publications

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“…Argillic Bt horizons are common in loess parent materials and are the soil bodies most exhaustively studied (e.g., Murphy and Kemp, 1987;Bronger and Bruhn, 1990;Bronger, 1991). Nonetheless, the discontinuous argillic horizons and horizontal cyclic sequences of the paired Bt and AC horizon rarely have been investigated and are poorly referenced in previous international pedologic and geologic literature.…”

Section: Introductionmentioning

confidence: 97%

Genesis of pedons with discontinuous argillic horizons in the Holocene loess mantle of the southern Pampean landscape, Argentina

Blanco

Stoops

2007

Journal of South American Earth Sciences

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Section: Introductionmentioning

confidence: 97%

Genesis of pedons with discontinuous argillic horizons in the Holocene loess mantle of the southern Pampean landscape, Argentina

Blanco

Stoops

2007

Journal of South American Earth Sciences

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“…The origin of these texture-contrast soils has been contentious. Bronger (1978Bronger ( , 1991 concluded that these soils are largely the result of a lithologic discontinuity in loess deposits, and that the clay-rich subsoil horizons mapped as Bt horizons show no evidence of illuvial clay coatings in thin section. Bronger described soil B horizon microfabrics in Nebraska as rich in aggregates due to biological activity that resulted from paleopedogenesis.…”

Section: Introductionmentioning

confidence: 99%

Late Quaternary climate change, loess sedimentation, and soil profile development in the central Great Plains: A pedosedimentary model

Jacobs

Mason

2007

Geological Society of America Bulletin

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Research on soil genesis often assumes a "top-down" model, in which the soil profi le develops downward from a stable land surface. This model is inapplicable to upland landscapes affected by frequent dust deposition, where soils grow upward as they develop. On the central Great Plains, late Quaternary loess sections proximal to immediate source areas contain the Brady Soil, a prominent marker separating late Pleistocene Peoria Loess from Holocene Bignell Loess. Farther from immediate dust source areas, the Brady Soil and Bignell Loess are not recognizable in the fi eld. On loess tablelands in these distal regions, surface soils typically contain a prominent, clay-rich B horizon below a thick silty A horizon. Assuming top-down pedogenesis, this could be interpreted as a postglacial soil profi le formed in Peoria Loess, with the B horizon produced by weathering and clay illuviation. We propose a strikingly different interpretation, in which the upper B horizon at distal sites is the Brady Soil A horizon that has been transformed by burial, organic matter loss, and modern subsoil structure formation processes. The overlying modern A horizon represents Bignell Loess. Properties of the Brady Soil at proximal sites (a distinctive burrowed zone, high clay content and TiO 2 /ZrO 2 , and low volcanic glass content) can be traced to the B horizon in distal soils. A decrease in smectite abundance above the Brady Soil at proximal sites is identifi able at the top of the clay-rich B horizon in distal soils. The spatial variation of clay content in loess and soil horizons is best explained by eolian sedimentation patterns. The higher clay content in the Brady Soil and distal B horizons defi nes a fi ne-grained zone that represents a late phaseof Peoria Loess accumulation. Evidence of chemical weathering is minimal, and illuvial clay is rare to absent in the clay-rich B horizons. Illuvial clay does often occur deep in the solum and is related to the depth below the top of the Brady Soil. The depth of occurrence of illuvial clay is not related to modern climate parameters, although depth to secondary carbonate appears to be in equilibrium with modern climate. Upland soils in the central Great Plains are composite soils; their properties are the result of a pedosedimentary history linked to regional climate change that has infl uenced sedimentation and pedogenesis since the late Pleistocene.

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“…in woodlands, which were located in the steppe during the Early Holocene. Under the forest vegetation of these woodlands, the decalcification was more intense than under the steppe vegetation and lessivage could occur (Bronger, 1991;Rohdenburg and Meyer, 1968).…”

Section: Study Area and Sitesmentioning

confidence: 97%

Occurrence, formation, and micromorphology of gypsum in soils from the Central-German Chernozem region

Dultz

Kühn

2005

Geoderma

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Argillic Horizons in Modern Loess Soils in an Ustic Soil Moisture Regime: Comparative Studies in Forest-Steppe and Steppe Areas from Eastern Europe and the United States

Cited by 32 publications

References 45 publications

Genesis of pedons with discontinuous argillic horizons in the Holocene loess mantle of the southern Pampean landscape, Argentina

Genesis of pedons with discontinuous argillic horizons in the Holocene loess mantle of the southern Pampean landscape, Argentina

Late Quaternary climate change, loess sedimentation, and soil profile development in the central Great Plains: A pedosedimentary model

Occurrence, formation, and micromorphology of gypsum in soils from the Central-German Chernozem region

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