The Devensian periglacial record on Thanet, Kent, UK

The Devensian periglacial record on Thanet, Kent, is traced from c. 88 to 74 ka and from c. 24 to 12 ka by optical luminescence dating of aeolian sand and silt in the periglacial stratigraphy. The record commences before 88 ka with valley cutting at Pegwell Bay. Valley filling had begun by c. 88 ka...

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Published in:Permafrost and Periglacial Processes
Main Authors: J. B. Murton, M. D. Bateman, C. A. Baker, R. Knox, C. A. Whiteman
Format: Article in Journal/Newspaper
Language:unknown
Subjects:
Ice
Online Access:https://doi.org/10.1002/ppp.442
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spelling ftrepec:oai:RePEc:wly:perpro:v:14:y:2003:i:3:p:217-246 2023-05-15T16:26:18+02:00 The Devensian periglacial record on Thanet, Kent, UK J. B. Murton M. D. Bateman C. A. Baker R. Knox C. A. Whiteman https://doi.org/10.1002/ppp.442 unknown https://doi.org/10.1002/ppp.442 article ftrepec https://doi.org/10.1002/ppp.442 2020-12-04T13:31:25Z The Devensian periglacial record on Thanet, Kent, is traced from c. 88 to 74 ka and from c. 24 to 12 ka by optical luminescence dating of aeolian sand and silt in the periglacial stratigraphy. The record commences before 88 ka with valley cutting at Pegwell Bay. Valley filling had begun by c. 88 ka and continued to at least 74 ka, coinciding with a major episode of loess deposition in Europe. Permafrost aggradation commenced before c. 21 ka, brecciating near‐surface chalk by ice segregation in permafrost and the overlying active layer. Deposition of aeolian sand (coversand) occurred at c. 24–21 ka, correlating with the Older Coversand I in mainland Europe. Permafrost degradation commenced at c. 21 ka, probably due to climate warming during Greenland Interstadial 2. The resulting active‐layer deepening through ice‐rich permafrost initiated soft‐sediment deformation and formation of large‐scale patterned ground in an active layer c. 2 m deep. Renewed permafrost aggradation between c. 21.25 and 18 ka coincided with climate cooling during Greenland Stadial 2c and led to cryoturbation in a thinner active layer. Final permafrost degradation commenced no later than c. 14.7 ka, that is, the start of Greenland Interstadial 1e, and may have occurred to some extent during the climate warming associated with Greenland Stadial 2b (c. 19.5–16.9 ka). Renewed deposition of aeolian sand took place at c. 15.5 ka, coincident with loess deposition on Thanet. A final episode of aeolian sand deposition occurred at 12 ka, correlating with the Younger Coversand deposits that are widespread in northwest Europe and formed during Greenland Stadial 1. Copyright © 2003 John Wiley & Sons, Ltd. Article in Journal/Newspaper Greenland Ice permafrost RePEc (Research Papers in Economics) Greenland Permafrost and Periglacial Processes 14 3 217 246
institution Open Polar
collection RePEc (Research Papers in Economics)
op_collection_id ftrepec
language unknown
description The Devensian periglacial record on Thanet, Kent, is traced from c. 88 to 74 ka and from c. 24 to 12 ka by optical luminescence dating of aeolian sand and silt in the periglacial stratigraphy. The record commences before 88 ka with valley cutting at Pegwell Bay. Valley filling had begun by c. 88 ka and continued to at least 74 ka, coinciding with a major episode of loess deposition in Europe. Permafrost aggradation commenced before c. 21 ka, brecciating near‐surface chalk by ice segregation in permafrost and the overlying active layer. Deposition of aeolian sand (coversand) occurred at c. 24–21 ka, correlating with the Older Coversand I in mainland Europe. Permafrost degradation commenced at c. 21 ka, probably due to climate warming during Greenland Interstadial 2. The resulting active‐layer deepening through ice‐rich permafrost initiated soft‐sediment deformation and formation of large‐scale patterned ground in an active layer c. 2 m deep. Renewed permafrost aggradation between c. 21.25 and 18 ka coincided with climate cooling during Greenland Stadial 2c and led to cryoturbation in a thinner active layer. Final permafrost degradation commenced no later than c. 14.7 ka, that is, the start of Greenland Interstadial 1e, and may have occurred to some extent during the climate warming associated with Greenland Stadial 2b (c. 19.5–16.9 ka). Renewed deposition of aeolian sand took place at c. 15.5 ka, coincident with loess deposition on Thanet. A final episode of aeolian sand deposition occurred at 12 ka, correlating with the Younger Coversand deposits that are widespread in northwest Europe and formed during Greenland Stadial 1. Copyright © 2003 John Wiley & Sons, Ltd.
format Article in Journal/Newspaper
author J. B. Murton
M. D. Bateman
C. A. Baker
R. Knox
C. A. Whiteman
spellingShingle J. B. Murton
M. D. Bateman
C. A. Baker
R. Knox
C. A. Whiteman
The Devensian periglacial record on Thanet, Kent, UK
author_facet J. B. Murton
M. D. Bateman
C. A. Baker
R. Knox
C. A. Whiteman
author_sort J. B. Murton
title The Devensian periglacial record on Thanet, Kent, UK
title_short The Devensian periglacial record on Thanet, Kent, UK
title_full The Devensian periglacial record on Thanet, Kent, UK
title_fullStr The Devensian periglacial record on Thanet, Kent, UK
title_full_unstemmed The Devensian periglacial record on Thanet, Kent, UK
title_sort devensian periglacial record on thanet, kent, uk
url https://doi.org/10.1002/ppp.442
geographic Greenland
geographic_facet Greenland
genre Greenland
Ice
permafrost
genre_facet Greenland
Ice
permafrost
op_relation https://doi.org/10.1002/ppp.442
op_doi https://doi.org/10.1002/ppp.442
container_title Permafrost and Periglacial Processes
container_volume 14
container_issue 3
container_start_page 217
op_container_end_page 246
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