Two-step deglaciation at the oxygen isotope stage 6/5E transition: The Zeifen-Kattegat climate oscillation

Seidenkrantz, Marit‐Solveig; Bornmalm, Lennart; Johnsen, S. J.; Knudsen, Karen Luise; Kuijpers, Antoon; Lauritzen, Stein‐Erik; Leroy, Suzanne A G; Mergeal, Isabelle; Schweger, Charles E.; Vliët-Lanoé, Brigitte van

doi:10.1016/0277-3791(95)00086-0

Cited by 91 publications

(32 citation statements)

References 38 publications

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“…2e). Although previous studies (20,40,41) Strikingly and importantly, the phase relationships between the various signals were quite different during the warming that marked the transition from Melisey I to St. Germain I. At that time there appears to have been synchrony between Antarctic warming, SST increase in the Atlantic west of Iberia and onset of the interstadial at Monticchio at 107.60 ka B.P., whereas the marked rise in CH 4 recorded in the same Antarctic ice core as the ␦D record of warming, lagged this event by Ϸ1.5 ka.…”

Section: Discussionmentioning

confidence: 64%

Evidence for last interglacial chronology and environmental change from Southern Europe

Brauer

Allen

Mingram

et al. 2007

Proc. Natl. Acad. Sci. U.S.A.

233

215

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Establishing phase relationships between earth-system components during periods of rapid global change is vital to understanding the underlying processes. It requires records of each component with independent and accurate chronologies. Until now, no continental record extending from the present to the penultimate glacial had such a chronology to our knowledge. Here, we present such a record from the annually laminated sediments of Lago Grande di Monticchio, southern Italy. Using this record we determine the duration (17.70 ؎ 0.20 ka) and age of onset (127.20 ؎ 1.60 ka B.P.) of the last interglacial, as reflected by terrestrial ecosystems. This record also reveals that the transitions at the beginning and end of the interglacial spanned only Ϸ100 and 150 years, respectively. Comparison with records of other earthsystem components reveals complex leads and lags. During the penultimate deglaciation phase relationships are similar to those during the most recent deglaciation, peaks in Antarctic warming and atmospheric methane both leading Northern Hemisphere terrestrial warming. It is notable, however, that there is no evidence at Monticchio of a Younger Dryas-like oscillation during the penultimate deglaciation. Warming into the first major interstadial event after the last interglacial is characterized by markedly different phase relationships to those of the deglaciations, warming at Monticchio coinciding with Antarctic warming and leading the atmospheric methane increase. Diachroneity is seen at the end of the interglacial; several global proxies indicate progressive cooling after Ϸ115 ka B.P., whereas the main terrestrial response in the Mediterranean region is abrupt and occurs at 109.50 ؎ 1.40 ka B.P.Eemian ͉ phase relationships ͉ pollen ͉ varves R econstructing the phase relationships between major earthsystem components relies on precise, accurate, and independent chronologies. However, absolute dating of geological records beyond the range of radiocarbon (more than Ϸ50 ka B.P.) is problematic, and age estimates for records of the last interglacial (LI) commonly rely on indirect dating approaches (1-4), often either by tuning to the time scale of orbital variations (2) or ''wiggle-matching'' to another record and applying its chronology (3, 4). Until now no continuous continental record extending from the present through the LI to the penultimate glacial had its own internal chronology to our knowledge. Thus timing and duration of the LI, as reflected in continental, marine, and ice-core records, and the phase relationships between these major earth-system components during marine oxygen isotope stage (MIS) 6-4, have been the subject of much debate (1, 5-9). Shackleton (9) first proposed correspondence between the LI and MIS 5e, whereas Woillard (10) subsequently demonstrated such apparent correspondence in a continental record. More recently, however, pollen, alkenone, and ␦ 18 O analyses of marine cores from locations close to the Iberian peninsula have shown asynchrony between changes in terrestrial veg...

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Section: Discussionmentioning

confidence: 64%

Evidence for last interglacial chronology and environmental change from Southern Europe

Brauer

Allen

Mingram

et al. 2007

Proc. Natl. Acad. Sci. U.S.A.

233

215

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“…(Fernald, 1965); (N) Nuyakuk (Elias and Short, 1992); (CB) Ch'ijees Blu! (Matthews et al, 1990;Schweger and Matthews, 1991); (HC) Hungry Creek (Schweger and Matthews, 1991); (T) Toklat River (Elias et al, 1996); (LB) Lituya Bay (Mann, 1986); (CR) Copper River Basin (Ager, 1989); (P) Palisades of the Yukon (BegeH t et al, 1991); (S) Squirrel Lake (P. Anderson in Hamilton and Brigham-Grette, 1991); (KY) Koyukuk River (Hamilton and Brigham-Grette, 1991;Seidenkrantz et al, 1996); HM, Hogatza Mine (Hamilton and Brigham-Grette, 1991); (I) Imuruk Lake (Colinvaux, 1964;Shackleton, 1982); (BC) Birch Creek (Edwards and McDowell, 1991); (HL) Holitna Lowland (Waythomas et al, 1993); (F) Fairbanks (PeH weH et al, 1997;this study). replaced by aspen parkland, and when a value of around !150 mm is reached, cool steppe replaces aspen parkland (Hogg, 1994). However, evidence that the Eva Forest Bed itself was deformed by the creation of a thaw depression suggests that permafrost was present during at least part of the last interglacial period.…”

Section: Inferences Based On Pollen and Macrofossil Studiesmentioning

confidence: 99%

“…Well-studied, spruce-pollen-bearing or spruce-macrofossil-bearing localities associated with the Old Crow tephra are numerous in the interior of Alaska and Yukon Territory, and include sites at Ch'ijees Blu! (Matthews et al, 1990;Schweger and Matthews, 1991), at the Palisades of the Yukon (BegeH t et al, 1991), along the Koyukuk River (Hamilton and Brigham-Grette, 1991;Seidenkrantz et al, 1996); at Hogatza Mine (Hamilton and Brigham-Grette, 1991), along Birch Creek (Edwards and McDowell, 1991), and in the Holitna Lowland (Waythomas et al, 1993). Localities showing extensions of boreal forest onto what is at present tundra are found on the Seward and Baldwin Peninsulas along the Cowpack River and at Nome, Deering, Kotzebue, and Imuruk Lake (Brigham-Grette and Hopkins, 1995;Colinvaux, 1964;Shackleton, 1982).…”

Section: Other Last Interglacial Boreal Forest Evidence In Alaska Andmentioning

confidence: 99%

Vegetation and paleoclimate of the last interglacial period, central Alaska

Muhs

Ager

Begét

2001

Quaternary Science Reviews

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Follow this and additional works at: https://digitalcommons.unl.edu/usgsstaffpub Part of the Earth Sciences CommonsThis Article is brought to you for free and open access by the US Geological Survey at DigitalCommons@University of Nebraska -Lincoln. It has been accepted for inclusion in USGS Staff --Published Research by an authorized administrator of DigitalCommons@University of Nebraska -Lincoln.Muhs, Daniel R.; Ager, Thomas A.; and Begét, James E., "Vegetation and paleoclimate of the last interglacial period, central Alaska" (2001 AbstractThe last interglacial period is thought to be the last time global climate was signi"cantly warmer than present. New stratigraphic studies at Eva Creek, near Fairbanks, Alaska indicate a complex last interglacial record wherein periods of loess deposition alternated with periods of soil formation. The Eva Forest Bed appears to have formed about the time of or after deposition of the Old Crow tephra (dated to &160 to &120 ka), and is therefore correlated with the last interglacial period. Pollen, macrofossils, and soils from the Eva Forest Bed indicate that boreal forest was the dominant vegetation and precipitation may have been greater than present around Fairbanks during the peak of the last interglacial period. A new compilation of last interglacial localities indicates that boreal forest was extensive over interior Alaska and Yukon Territory. Boreal forest also extended beyond its present range onto the Seward and Baldwin Peninsulas, and probably migrated to higher elevations, now occupied by tundra, in the interior. Comparison of last interglacial pollen and macrofossil data with atmospheric general circulation model results shows both agreement and disagreement. Model results of warmer-than-present summers are in agreement with fossil data. However, numerous localities with boreal forest records are in con#ict with model reconstructions of an extensive cool steppe in interior Alaska and much of Yukon Territory during the last interglacial.

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“…It is suggested that erosion occurred between 180-150 ka BP and wind drift deposited between 150-130 ka BP (Fig. 10b) prior to the Eemian interglacial (Seidenkrantz et al, 1996).…”

Section: Landscape Chronologymentioning

confidence: 99%

“…MIS 8 (Saalian II) is brief but very cold and arid, whereas the MIS 6 (Saalian III) is much less arid and colder toward its end (Seidenkrantz et al, 1996). Common traces for permafrost occurrences are the development of metric polygonal patterns due to ground thermal contraction (Dylik & Maarleveld, 1976;Washburn, 1979).…”

Section: Introductionmentioning

confidence: 99%

Periglacial morphogenesis in the Paris basin: insight from geophysical survey and consequences for the fate of soil pollution

Thiry¹,

Oort²,

Thiesson³

et al. 2013

Geomorphology

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Two-step deglaciation at the oxygen isotope stage 6/5E transition: The Zeifen-Kattegat climate oscillation

Cited by 91 publications

References 38 publications

Evidence for last interglacial chronology and environmental change from Southern Europe

Evidence for last interglacial chronology and environmental change from Southern Europe

Vegetation and paleoclimate of the last interglacial period, central Alaska

Periglacial morphogenesis in the Paris basin: insight from geophysical survey and consequences for the fate of soil pollution

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