scholarly journals Fossil and recent soil formation in Late Pleistocene sand deposits in the eastern part of the Netherlands.

1976 ◽  
Vol 24 (3) ◽  
pp. 173-178
Author(s):  
S. Slager ◽  
A.G. Jongmans ◽  
L.J. Pons
Keyword(s):  
Biological Activity ◽  
The Netherlands ◽  
Late Pleistocene ◽  
Soil Formation ◽  
The Holocene ◽  
Aeolian Deposits ◽  
Soil Forming Processes

Along the Slinge Brook near Winterswijk, a profile was investigated which is assumed to consist of two aeolian deposits: Old Coversand I at the bottom and Old Coversand II at the top, between which a fluvioglacial deposit occurs, the Beuningen Complex. The profile, which now is well-drained, was poorly drained from the beginning of the Holocene up to some centuries ago. The following soil forming processes were recognized micromorphologically: decarbonation, biological activity, clay illuviation, decomposition of illuviated clay and one or two cycles of gleying. It was concluded that: (1) during the deposition of the Beuningen Complex a hydromorphic cycle may have occurred in this profile; (2) between the beginning of the Bolling interstadial and the rise of the watertable at the beginning of the Holocene, biological activity and clay illuviation occurred and possibly some decarbonation; (3) between the beginning of the Holocene and recent times a hydromorphic cycle (possibly the second) took place; (4) finally in recent times biological activity and decarbonation occur. (Abstract retrieved from CAB Abstracts by CABI’s permission)

The morphology and genesis of pseudogley phenomena in a Pleistocene loamy sand in the Netherlands.

1974 ◽  
Vol 22 (1) ◽  
pp. 22-30
Author(s):  
M.F. Van Oosten ◽  
S. Slager ◽  
A.G. Jongmans
Keyword(s):  
Biological Activity ◽  
The Netherlands ◽  
Iron Oxides ◽  
Late Pleistocene ◽  
Clay Fraction ◽  
Soil Formation ◽  
Loamy Sand ◽  
Fine Clay ◽  
Soil Forming Processes

[183.64:141.791]In a loamy sand profile with deep watertable, developed in Pleistocene deposits and showing mottling patterns and fine-textured bands and tongues, four soil-forming processes were recognizable: illuviation of fine clay and iron oxides, biological activity, pseudogleying, and breakdown of the clay fraction at the upper side of the illuviation horizon. The genesis of this soil can be explained by assuming that soil formation started where frost wedges occurred in the profile during the late Pleistocene and proceeded further at these points than in other parts of the soil. (Abstract retrieved from CAB Abstracts by CABI’s permission)

Morphology, genesis, and distribution of calcareous material in Late Weichselian sediments of the Rhine and Meuse rivers in the eastern part of the Netherlands.

1986 ◽  
Vol 34 (4) ◽  
pp. 441-448
Author(s):  
A.G. Jongmans ◽  
R. Miedema
Keyword(s):  
Biological Activity ◽  
The Netherlands ◽  
Cross Section ◽  
Field Investigation ◽  
The Holocene ◽  
Late Weichselian ◽  
Calcareous Sediment

In Late Weichselian sediments of the rivers Rhine and Meuse locally and haphazardly calcareous sediments were deposited. Field investigation of a cross section through a calcareous sediment and subsequent micromorphological investigation of biological activity, decalcification and clay illuviation indicate that such local occurrences are slabs of frozen, calcareous sediments, transported and redeposited as floes during periglacial conditions. Sedimentation of the calcareous material is probably of Bolling age and was accompanied by bioturbation. Decalcification, transport and resedimentation as floes occurred during the Old Dryas. Early in the Allerod the material was strongly bioturbated. Clay illuviation should be dated in the Young Dryas and gley and pseudogley formation, finally, in the Holocene. (Abstract retrieved from CAB Abstracts by CABI’s permission)

scholarly journals On soil genesis in temperate humid climate. VIII. The formation of a "udalfic" eutrochrepi.

1970 ◽  
Vol 18 (3) ◽  
pp. 207-214 ◽  
Author(s):  
J. Van Schuylenborgh ◽  
S. Slager ◽  
A.G. Jongmans
Keyword(s):  
Biological Activity ◽  
Clay Minerals ◽  
Redox Processes ◽  
Humid Climate ◽  
Soil Genesis ◽  
Fe Oxide ◽  
The Holocene ◽  
Differential Movement ◽  
The Difference ◽  
Soil Forming Processes

The active soil-forming processes occurring in a Holocene alluvial deposit were: the formation, along voids, of illuvial cutans consisting of clay minerals, Fe oxide and fine matric components (matriferriargillans), differential movement of clay minerals, kaolinite being most mobile; partial transformation of smectites into kandites; disturbance of cutans by biological activity resulting in the formation of papules; redox processes leading to the formation of micro-segregation of Fe oxide. The difference in character and location of matriferriargillans and ferriargillans is discussed. The former are thought to have been synthesized in the Holocene period and the latter in Pleistocene times. The soil is classifiable as a dystric eutrochrept, but as plasma movement generally occurs only in "dystric" (decalcified) material, the soil could be classified as a "udalfic" eutrochrept. (Abstract retrieved from CAB Abstracts by CABI’s permission)

scholarly journals Fossil and recent soil formation in lateleistocene loess deposits in the southern part of the Netherlands.

1978 ◽  
Vol 26 (3) ◽  
pp. 326-335
Author(s):  
S. Slager ◽  
A.G. Jongmans ◽  
R. Miedema ◽  
L.J. Pons
Keyword(s):  
Calcium Carbonate ◽  
The Netherlands ◽  
Western Europe ◽  
Soil Formation ◽  
Soil Surface ◽  
Preferential Orientation ◽  
The Holocene ◽  
Animal Burrows ◽  
Animal Activity ◽  
Loess Deposits

In the younger, Weichselian (Wurm, Wisconsin) loess deposits in the south of the Netherlands there is a horizon with fossil pedotubules (filled animal burrows). These pedotubules, 3 mm ( plus or minus 1 mm) in diameter, unbranched, without preferential orientation, are most abundant in the zone extending from about 30 cm above the decalcification boundary (situated 2-3 m below the soil surface) to some decimeters below it. They are rare in the B3t horizon of the overlying Hapludalf. Their lower extension boundary occurs some 2 m below the decalcification boundary. These tubules result from fossil animal activity followed by decalcification, mainly of a Boelling soil surface. A loess layer some 2 m thick was probably deposited in the post-Boelling period; the lower part of this layer has a lamellae spot zone. Micromorphological evidence shows that the lamellae spot zone was originally at the actual soil surface. Consequently a geogenic origin of the lamellae spot zone rather than a pedogenic origin seems likely. Soil formation subsequently intensified the textural differences. It is suggested that the post-Boelling loess was free of calcium carbonate at the beginning of the Holocene and was deposited non-calcareously or was decalcified synsedimentarily. In Western Europe, loess soils formed from Pleistocene deposits probably matured earlier in the Holocene than has been assumed hitherto. (Abstract retrieved from CAB Abstracts by CABI’s permission)

scholarly journals Late Pleistocene and Early Holocene aeolian deposits of Tasmania and their climatic implications – Corrigendum

2021 ◽  
pp. 1-2
Author(s):  
Peter D. McIntosh ◽  
Christina Neudorf ◽  
Olav B. Lian ◽  
Adrian J. Slee ◽  
Brianna Walker ◽  
...  
Keyword(s):  
Late Pleistocene ◽  
Early Holocene ◽  
Aeolian Deposits

scholarly journals Soil Formation, Subaerial Sedimentation Processes and Ancient Cultures during MIS 2 and the Deglaciation Phase MIS 1 in the Baikal–Yenisei Siberia (Russia)

Geosciences ◽  
2021 ◽  
Vol 11 (8) ◽  
pp. 323
Author(s):  
Galina Vorobieva ◽  
Nadezhda Vashukevich ◽  
Natalia Berdnikova ◽  
Ivan Berdnikov ◽  
Dmitry Zolotarev ◽  
...  
Keyword(s):  
Soil Formation ◽  
Climatic Conditions ◽  
Initial Profile ◽  
Formation Type ◽  
Cultural Layers ◽  
Human Habitation ◽  
Soil Forming Processes ◽  
First Time ◽  
Sedimentation Processes ◽  
Humus Horizons

The time of Sartan glaciation in the Baikal–Yenisei Siberia, is comparable with that of MIS 2 and the deglaciation phase MIS 1. Loess loams, aeolian–colluvial sands and sandy loams represent subaerial sediments. There are four subhorizons (sr1, sr2, sr3 and sr4) in the Sartan horizon (sr). Sedimentary and soil-forming processes at different stratigraphic levels are considered. Differing soil formation types of cold periods are distinguished. Soils of the interstadial type with the A-C profile are represented only in the Early Sartan section of this paper. The soils of the pleniglacial type are discussed throughout the section. Their initial profile is O-C, TJ-C and W-C. Plant detritus remnants or poor thin humus horizons are preserved in places from the upper horizons. We propose for the first time for the interphasial soil formation type of cold stages to be distinguished. This is represented in the sections by the preserved BCm, BCg, Cm and Cg horizons of 15–20 cm thick. The upper horizons are absent in most sections. According to the surviving fragments, these were organogenous (O, TJ and T) and organomineral (AO and W) horizons. The sedimentation and soil formation features are considered from the perspective reconstruction of the Sartan natural and climatic conditions. Buried Sartan soils often contain cultural layers. Soil formation shows a well-defined periodicity of natural condition stabilization, which allowed ancient populations to adapt actively to various situations. Archaeologists’ interest in fossil soils is based on the ability of soils to “record” information about the natural and climatic conditions of human habitation.

Pedogenesis and tephrochronology of loess derived soils, Hinton, Alberta

1980 ◽  
Vol 17 (1) ◽  
pp. 52-59 ◽  
Author(s):  
J. Dumanski ◽  
S. Pawluk ◽  
C. G. Vucetich ◽  
J. D. Lindsay
Keyword(s):  
Climatic Change ◽  
Volcanic Ash ◽  
Soil Formation ◽  
Gradual Change ◽  
The Holocene ◽  
Loess Deposition

The loess derived soils of the Hinton district provide a record of soil formation for the entire postglacial period. Loess originates from the shorelines of Brûlé Lake and from the sandbars and braided channels of the Athabasca River.The geochronology of the loess, as established through the study of paleosols and volcanic ash beds, indicates that loess deposition was continual but irregular. Soil formation occurred contemporaneously with loess deposition, and varying soil morphologies were attributed to differing local rates of loess accumulation. There was no evidence for marked climatic change during the Holocene in the study area, but increased loess supply after 4000 years BP may reflect gradual change.

scholarly journals The Ice-Rich Permafrost Sequences as a Paleoenvironmental Archive for the Kara Sea Region (Western Arctic)

2021 ◽  
Vol 9 ◽  
Author(s):  
I. D. Streletskaya ◽  
A. A. Pismeniuk ◽  
A. A. Vasiliev ◽  
E. A. Gusev ◽  
G. E. Oblogov ◽  
...  
Keyword(s):  
Late Pleistocene ◽  
Marine Sediments ◽  
Isotope Composition ◽  
Kara Sea ◽  
Coastal Sediments ◽  
Organic Carbon Content ◽  
Ground Ice ◽  
Geochemical Composition ◽  
The Holocene ◽  
Mis 3

The Kara Sea coast and part of the shelf are characterized by wide presence of the ice-rich permafrost sequences containing massive tabular ground ice (MTGI) and ice wedges (IW). The investigations of distribution, morphology and isotopic composition of MTGI and IW allows paleoenvironmental reconstructions for Late Pleistocene and Holocene period in the Kara Sea Region. This work summarizes result of long-term research of ice-rich permafrost at eight key sites located in the Yamal, Gydan, Taimyr Peninsulas, and Sibiryakov Island. We identified several types of ground ice in the coastal sediments and summarized data on their isotopic and geochemical composition, and methane content. We summarized the available data on particle size distribution, ice chemical composition, including organic carbon content, and age of the enclosing ice sediments. The results show that Quaternary sediments of the region accumulated during MIS 5 – MIS 1 and generally consisted of two main stratigraphic parts. Ice-rich polygenetic continental sediments with syngenetic and epigenetic IW represent the upper part of geological sections (10–15 m). The IW formed in two stages: in the Late Pleistocene (MIS 3 – MIS 2) and in the Holocene cold periods. Oxygen isotope composition of IW formed during MIS 3 – MIS 2 is on average 6‰ lower than that of the Holocene IW. The saline clay with rare sand layers of the lower part of geological sections, formed in marine and shallow shelf anaerobic conditions. MTGI present in the lower part of the sections. The MTGI formed under epigenetic freezing of marine sediments immediately after sea regression and syngenetic freezing of marine sediments in the tidal zone and in the conditions of shallow sea.

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