Landscape development in response to climatic change during Oxygen Isotope Stage 5 in the southern Siberian loess region

Boreas ◽  
2004 ◽  
Vol 33 (2) ◽  
pp. 164-180 ◽  
Author(s):  
Jiri Chlachula ◽  
Rob Kemp ◽  
Catherine Jessen ◽  
Adrian Palmer ◽  
Phillip Toms
Keyword(s):  
Oxygen Isotope ◽  
Climatic Change ◽  
Landscape Development ◽  
Oxygen Isotope Stage ◽  
Loess Region

Landscape development in response to climatic change during Oxygen Isotope Stage 5 in the southern Siberian loess region

Boreas ◽  
2008 ◽  
Vol 33 (2) ◽  
pp. 164-180 ◽  
Author(s):  
JIRI CHLACHULA ◽  
ROB A. KEMP ◽  
CATHERINE A. JESSEN ◽  
ADRIAN P. PALMER ◽  
PHILLIP S. TOMS
Keyword(s):  
Oxygen Isotope ◽  
Climatic Change ◽  
Landscape Development ◽  
Oxygen Isotope Stage ◽  
Loess Region

Wolverine in Northern England at About 83,000 yr B.P.: Faunal Evidence for Climatic Change during Isotope Stage 5

1985 ◽  
Vol 24 (1) ◽  
pp. 73-86 ◽  
Author(s):  
Antony J. Sutcliffe ◽  
Thomas C. Lord ◽  
Russell S. Harmon ◽  
Miro Ivanovich ◽  
Angela Rae ◽  
...  
Keyword(s):  
Calcium Carbonate ◽  
Oxygen Isotope ◽  
Climatic Change ◽  
Faunal Assemblage ◽  
Oxygen Isotope Stage ◽  
Uranium Series ◽  
Cave Sediments ◽  
Uranium Series Dating ◽  
Absolute Age ◽  
Carbonate Deposits

Cave sediments from Stump Cross Cave in northern England contain Pleistocene mammal remains. Uranium-series dating of calcium carbonate deposits closely associated with the fossiliferous horizons has established an absolute age of 83,000 ± 6000 yr B.P. for a faunal assemblage largely comprised of wolverines (Gulo gulo). This date lies firmly within the younger portion of oxygen-isotope stage 5. The occurrence of wolverines in the vicinity of Stump Cross Cave at ca. 83,000 yr B.P. indicates a significant climatic deterioration from ca. 120,000 yr B.P., when an Ipswichian interglacial fauna with hippopotamus was present in this part of northern England.

Inter-profile correlation of the Chinese loess/paleosol sequences during Marine Oxygen Isotope Stage 5 and indications of pedogenesis

2005 ◽  
Vol 24 (1-2) ◽  
pp. 195-210 ◽  
Author(s):  
Qingsong Liu ◽  
Subir K. Banerjee ◽  
Michael J. Jackson ◽  
Chenglong Deng ◽  
Yongxin Pan ◽  
...  
Keyword(s):  
Oxygen Isotope ◽  
Chinese Loess ◽  
Oxygen Isotope Stage

A paleoclimatic evaluation of marine oxygen isotope stage 11 in the high-northern Atlantic (Nordic seas)

2000 ◽  
Vol 24 (1) ◽  
pp. 27-39 ◽  
Author(s):  
Henning A Bauch ◽  
Helmut Erlenkeuser ◽  
Jan P Helmke ◽  
Ulrich Struck
Keyword(s):  
Oxygen Isotope ◽  
Nordic Seas ◽  
Oxygen Isotope Stage ◽  
Northern Atlantic

Palynology of Oxygen Isotope Stage 6 and Substage 5e from the Cover Beds of a Marine Terrace, Taranaki, New Zealand

1990 ◽  
Vol 34 (1) ◽  
pp. 86-100 ◽  
Author(s):  
M. Royd Bussell
Keyword(s):  
New Zealand ◽  
Oxygen Isotope ◽  
Major Change ◽  
Oxygen Isotope Stage ◽  
Long Period ◽  
Marine Terraces ◽  
Tree Ferns ◽  
Glacial Stage ◽  
Marine Platform ◽  
Organic Deposits

AbstractCover beds on uplifted Quaternary marine terraces in the Taranaki-Wanganui area of New Zealand include organic deposits which yield abundant pollen. In the west at Ohawe, marine shore platform deposits are overlain by laterally extensive lignites and laharic breccia, interbedded with alluvium and capped by tephra-rich loess. Following a time of presumably interglacial marine deposition on the platform, a long period of glacial climate is suggested by pollen floras dominated by grass and shrubland taxa. Trees were sparse, but the abundance of podocarps, Nothofagus, and tree ferns increased during at least one interval, suggesting minor climatic amelioration. Near the top of the section, a major change in regional vegetation is recorded by a dominance of pollen derived from podocarp-hardwood forest taxa, including Ascarina, interpreted as indicating a fully interglacial climate. The marine platform, previously assigned to oxygen isotope substage 5e, is now placed in stage 7. The overlying deposits were deposited during glacial stage 6, while interglacial substage 5e is recorded by sediment and pollen assemblages near the top of the section.

scholarly journals Reconstructing Pleistocene Climatic Change from the Oxygen Isotope Composition of Sediments: A Review

1984 ◽  
Vol 5 ◽  
pp. 43-46 ◽  
Author(s):  
Curt Covey
Keyword(s):  
Oxygen Isotope ◽  
Climatic Change ◽  
Isotope Composition ◽  
Climatic Changes ◽  
Oxygen Isotope Composition ◽  
Glacial Ice ◽  
Complicating Factors ◽  
Data Source

The isotope composition of ocean sediments is the chief data source for Pleistocene climatic changes. It is generally believed that the18O/16O ratio of a sample indicates the global total of glacial ice at the time the sample was deposited. This is roughly correct, but numerous complicating factors limit the accuracy of the isotope proxies.

Changes in the Thermal Climate in Northwestern Europe during Marine Oxygen Isotope Stage 3, Estimated from Fossil Insect assemblages

2002 ◽  
Vol 57 (3) ◽  
pp. 401-408 ◽  
Author(s):  
G. Russell Coope
Keyword(s):  
Oxygen Isotope ◽  
Ice Cores ◽  
Temperate Climate ◽  
Northern Europe ◽  
Oxygen Isotope Stage ◽  
Fossil Insect ◽  
Before And After ◽  
Beetle Assemblages ◽  
Thermal Climate ◽  
The Times

AbstractMore than 30 fossil coleopteran (beetle) assemblages have been recorded from oxygen isotope stage 3 in northern Europe, comprising several hundred identified species. Using the mutual climatic range method for quantifying palaeotemperatures, these assemblages show that the climates of the times can be divided into two distinct interstadial types. One, a short phase of temperate/oceanic climate occurred between 43,000 and 42,000 14C yr B.P. when conditions were not much different from those of the present day. In spite of the temperate climate, trees did not colonize northwestern Europe at this time. Two, both before and after this temperate interlude there were phases of cold/continental climate during which summers were too cold for trees to grow and winters were of Siberian intensity. It is possible that periods of even colder conditions intervened from time to time between the interstadial but, because of the intensity of the cold, biological systems were so inhibited that no fossil evidence for them can be found in northern Europe. Evidence for them must be sought in the fossil records from the warmer parts of southern Europe or in the physical evidence in the Greenland ice cores.

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