Late quaternary sedimentation in the eastern arctic basin: Stratigraphy and depositional environment

Markussen, Berit; Thiede, Jörn

doi:10.1016/s0031-0182(85)80016-x

Cited by 29 publications

(3 citation statements)

References 18 publications

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“… Green [1960] and Lagoe [1977, 1979] established much of what we know about the deep water Arctic species from data collected from the T‐3 ice island occupied by an international group of scientists for several years [ Clark et al , 1980]. These studies were added to by examination of material from the ice stations in the central Arctic (LOREX, FRAM, CESAR, and other sites [ Markussen et al , 1985; Scott and Vilks , 1991; Bergsten , 1994; Wollenburg and Kuhnt , 2000]). Osterman et al [1999] repeated some of the surface stations of previous studies and added new ones in the western Arctic.…”

Section: Previous Workmentioning

confidence: 99%

Foraminiferal assemblage changes over the last 15,000 years on the Mackenzie‐Beaufort Sea Slope and Amundsen Gulf, Canada: Implications for past sea ice conditions

et al. 2009

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Two cores, one from the Beaufort Sea Slope at 1000 m water depth (core 750) and one from the Amundsen Gulf at 426 m (core 124), were collected to help determine paleo–ice cover in the Holocene and late glacial of this area. Site 750 is particularly sensitive to changes in paleo–ice cover because it rests beneath the present ice margin of the permanent Arctic ice pack. Core 124 was sampled just in front of the former glacier that moved out into the Amundsen Gulf and started to recede about 13 ka B.P. Both cores have a strong occurrence of calcareous foraminifera in the upper few centimeters, but these disappear throughout most of the Holocene, suggesting more open water in that time period than present. In the sediments representing the end of the last glacial period (dated at ∼11,500–14,000 calibrated years B.P. (cal B.P.)) a calcareous fauna with an abundant planktic foraminiferal fauna suggests a return to almost permanent ice cover, much like the central Arctic today. Together with the foraminifera there was also abundant ice‐rafted debris (IRD) in both cores between 12,000 cal B.P. and ∼14,000 cal B.P., but those units are of different ages between cores, suggesting different events. The IRD in both cores appears to have the same magnetic and chemical signals, but their origins cannot be determined exactly until clay mineralogy is completed. There is abundant organic debris in both cores below the IRD units: the organics in core 750 are very diffuse and not visually identifiable, but the organic material in core 124 is clearly identifiable with terrestrial root fragments; these are 14C dated at over 37,000 years B.P. This is a marine unit as it also has glacial front foraminifera in the sediment with the organic debris that must have been originating from subglacial streams. The seismic and multibeam data both indicate glaciers did not cross the core 124 site.

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Section: Previous Workmentioning

confidence: 99%

Foraminiferal assemblage changes over the last 15,000 years on the Mackenzie‐Beaufort Sea Slope and Amundsen Gulf, Canada: Implications for past sea ice conditions

et al. 2009

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“…Age-depth relationships for Arctic Ocean sediments have been debated since the late 1990s and early 2000s (Backman et al, 2004) because different dating methods yielded different results (e.g., Jakobsson et al, 2001;Markussen et al, 1985;Steuerwald et al, 1968;Witte & Kent, 1988). As in most other ocean basins, magnetostratigraphy was widely used to constrain sediment age, with the uppermost polarity reversal strictly interpreted as the Brunhes-Matuyama polarity transition at ca.…”

Section: Introductionmentioning

confidence: 99%

Late Pleistocene Chronology of Sediments From the Yermak Plateau and Uncertainty in Dating Based on Geomagnetic Excursions

Wiers

Snowball

O’Regan

et al. 2019

Geochem Geophys Geosyst

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The Yermak Plateau is one of several regions in the Arctic Ocean where paleomagnetism yields controversial results. Despite low sedimentation rates, late Pleistocene paleomagnetic excursions have been reconstructed from many cores in the region, but they are characterized by considerably longer durations when compared to established ones. Self‐reversal during maghemitization of (titano)magnetite has been proposed as one explanation. Rock magnetic, 14C dating, sedimentological and stable isotope (δ18O) methods were employed to three new sediment cores to put paleomagnetic results in the context of the regional stratigraphy and chronology. Coherence of lithological parameters and δ18O variations validated the ratio of anhysteretic remanent susceptibility to bulk magnetic susceptibility (κARM/κ) as a parameter for cross‐core correlation. As established by earlier studies, we use the link between glacial/interglacial cycles and κARM/κ to tune our records to a global δ18O stack, which provides age models that are independent of radicarbon ages and paleomagnetic data. Our results show that zones of negative magnetic inclination are asynchronous across the plateau. Alternating field demagnetization data revealed that negative inclinations are contained in a medium‐high‐coercivity (>25–35 mT) magnetic phase that may be the result of postdepositional alteration of (titano)magnetite. We note a positive relationship between water depth and excursion duration, which may be driven by changes in water mass circulation on glacial/interglacial timescales.

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“…Since then, in situ data from many parts of the Arctic Ocean and its margins have shown that the idea of one giant Northern Hemisphere ice sheet during the LGM is not well substantiated and that the extension of LGM ice sheets in northern Eurasia was much smaller than supposed by the CLIMAP Project Members [1981] Working Group [cf. Hopkins , 1982, Markussen et al , 1985; Sher , 1995; Velichko et al , 1997; Velichko , 1995; Nørgaard‐Pedersen et al , 1998; Svendsen et al , 1999, Mangerud et al , 2002]. Despite this wealth of field data, the idea of a huge LGM ice sheet covering the entire northern Eurasian continental margin is still supported by some authors [e.g., Grosswald and Hughes , 2002].…”

Section: Introductionmentioning

confidence: 99%

Arctic Ocean during the Last Glacial Maximum: Atlantic and polar domains of surface water mass distribution and ice cover

et al. 2003

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[1] On the basis of 52 sediment cores, analyzed and dated at high resolution, the paleoceanography and climate of the Last Glacial Maximum (LGM) were reconstructed in detail for the Fram Strait and the eastern and central Arctic Ocean. Sediment composition and stable isotope data suggest three distinct paleoenvironments: (1) a productive region in the eastern to central Fram Strait and along the northern Barents Sea continental margin characterized by Atlantic Water advection, frequent open water conditions, and occasional local meltwater supply and iceberg calving from the Barents Sea Ice Sheet; (2) an intermediate region in the southwestern Eurasian Basin (up to 84-85°N) and the western Fram Strait characterized by subsurface Atlantic Water advection and recirculation, a moderately high planktic productivity, and a perennial ice cover that breaks up only occasionally; and (3) a central Arctic region (north of 85°N in the Eurasian Basin) characterized by a lowsalinity surface water layer and a thick ice cover that strongly reduces bioproduction and bulk sedimentation rates. Although the total inflow of Atlantic Water into the Arctic Ocean may have been reduced during the LGM, its impact on ice coverage and halocline structure in the Fram Strait and southwestern Eurasian Basin was strong.

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Late quaternary sedimentation in the eastern arctic basin: Stratigraphy and depositional environment

Cited by 29 publications

References 18 publications

Foraminiferal assemblage changes over the last 15,000 years on the Mackenzie‐Beaufort Sea Slope and Amundsen Gulf, Canada: Implications for past sea ice conditions

Foraminiferal assemblage changes over the last 15,000 years on the Mackenzie‐Beaufort Sea Slope and Amundsen Gulf, Canada: Implications for past sea ice conditions

Late Pleistocene Chronology of Sediments From the Yermak Plateau and Uncertainty in Dating Based on Geomagnetic Excursions

Arctic Ocean during the Last Glacial Maximum: Atlantic and polar domains of surface water mass distribution and ice cover

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