Symposium Discussion: Some Notes on the Last Deglaciation in Northern Europe Compared with Canadian Conditions

Zonneveld, J. I. S.; Mitchell, J Malone; Orvig, Svenn; Müller, Fr.; Fyles, J G; Ford, Derek C.; Hare, F. Kenneth; Barry, Roger G.; Andrews, John T.; Macpherson, Joyce Brown

doi:10.2307/1550030

Cited by 8 publications

(6 citation statements)

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“…Prest's (1969) areas are always less than those on the Bryson et al (1969) map for the same period. A tentative isochrone map at a very large scale for Europe (Zonneveld 1973) has been used for that area plus a broad knowledge of the European literature on the topic of deglaciation chronology. A major question mark surrounds the extent of glacial ice in the European-USSR arctic.…”

Section: Description Of a Load Model: Ice4mentioning

confidence: 99%

Glacial-Isostatic Adjustment-I. The Forward Problem

Peltier¹,

Andrews²

2007

Geophysical Journal of the Royal Astronomical Society

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446

132

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The isostatic adjustment of a radially stratified visco-elastic spheroid is treated using space-time Green functions for the associated surface mass load boundary value problem. These impulse response functions are convolved with a Heaviside function to give the time dependent deformation of the planet which would be produced by a unit point mass brought up from infinity at t = 0 and allowed to remain on the surface. The resulting ' Heaviside Green functions ' can be employed to simulate al! of the important signatures of glacial isostatic adjustment. Given a space-time dependent surface mass load consisting of ice sheet ablation histories and a model of the simultaneous filling of the ocean basins, these source terms are simply convolved with the Heaviside Green function appropriate to a specific response signature. A realistic model of the spatial distribution of the main late Pleistocene ice loads and of their temporal disintegration is constructed. The response of two visco-elastic earth models is computed and compared to a global set of relaxation data (relative sea-level curves). On the basis of this initial comparison of theory and observation the possibility that the lower mantle has a viscosity which is significantly in excess of the viscosity of the upper mantle is excluded. In addition, clear evidence of the presence of the lithosphere has been found in relaxation data from sites which were near the edge of the Laurentide ice sheet. Such data should therefore prove useful as a basis for analysis of lateral variations in lithosphere thickness. Further extensions of the calculation are suggested.

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Section: Description Of a Load Model: Ice4mentioning

confidence: 99%

Glacial-Isostatic Adjustment-I. The Forward Problem

Peltier¹,

Andrews²

2007

Geophysical Journal of the Royal Astronomical Society

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446

132

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“…The maximum extent of the ice sheet occurred between about 20 OOO and 18 000 yr BP and the early decay apparently occurred as a series of retreats possibly followed by minor readvances. According to the syntheses by Zonneveld (1973) and Andersen (1981), the final retreat was rapid after about 10 OOO yr ago and the ice sheet vanished by 8000yr BP. Peltier & Andrews (1976) give the basic ice model Z ( t ) for the northern hemisphere ice sheets of Laurentia and Fennoscandia.…”

Section: Ice Modelmentioning

confidence: 99%

“…(The stress relaxation constant, therefore, is referred to the I4C time-scales.) In the reconstruction of the Fennoscandian model of [and presumably also by Zonneveld (1973), upon which the ICE1 and ARC3 models are based] ages have not been corrected for either fractionation or reservoir effects (Andersen 1981). Typically, for carbonate material, the fractionation correction is about 430 f 50 yr while the ocean reservoir correction for this material is reasonably constant at about -400 f 50 yr over a range of middle latitudes and the neglect of both corrections appears to be reasonable.…”

Section: Time-scalementioning

confidence: 99%

Holocene glacial rebound and sea-level change in NW Europe

Lambeck

Johnston

Nakada

1990

Geophysical Journal International

174

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S U M M A R Y Observations of Late Pleistocene and Holocene sea-level change relative to the crust exhibit very considerable variations across NW Europe in consequence of the response of the Earth's crust to the deglaciation of Fennoscandia and of the water added to the oceans from the melting of all Late Pleistocene ice sheets. Inversion of sea-level observations from a site near the centre of the Fennoscandian ice sheet and from three sites located beyond the margin of the ice sheet at the time of maximum glaciation yield a range of plausible models for the Earth's response and for the ice models. Further constraints on this range of models is placed by a comparison of observed sea-levels with predicted values at other sites near the former ice sheet margins. The resulting mantle parameters are: upper mantle viscosity (3-5) X 10'' Pa s; lower mantle viscosity (2-7) X loz1 Pa s; lithospheric thickness 100-150 km. These values represent effective parameters that describe the response of the Earth to surface loading of short to intermediate wavelengths on a time-scale of 104yr. The lower mantle viscosity is poorly constrained but the marked increase from upper to lower mantle is a characteristic of all plausible solutions. The inversion places a constraint on the total volume of ice in the Fennoscandian ice sheet such that the equivalent sea-level rise from this contribution is about 13-14 m. A less well-determined constraint of about 10 m equivalent sea-level rise is suggested for the Barents-Kara ice sheet. The inversion also indicates that a small amount of melt-water, from ice sheets far away from Europe, continued to be added into the oceans during Late Holocene time so as to raise the equivalent sea-level by about 3 m during the past 6000 yr, consistent with similar inversions of data from sites in the Australian and Pacific regions.

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“…Considerable variation can be expected from the time melting began at about 18,000 yr B.P. to the present (Zonneveld, 1973;Andersen, 1981). Parallel to the retreat of the ice dome, numerous local fresh-water lakes were formed beween the ice and the surrounding land areas.…”

Section: Study Areamentioning

confidence: 99%

Late- and Postglacial Sea-Level Change and Paleoenvironments in the Oder Estuary, Southern Baltic Sea

Müller¹

2001

Quat. res.

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Knowledge of sea-level change in the southern Baltic Sea region is important for understanding the variations in late Pleistocene and Holocene sea-level change across northern Europe. These variations are a consequence of the response of the Earth's crust to the deglaciation of Fennoscandia and of the water added to the oceans from the melting of all Pleistocene ice sheets. The sedimentological and geochemical composition of five sediment cores from the lagoonal Oder Estuary offers new observational evidence for sea-level change and coastal development in the southern Baltic Sea region. The combined use of several geochemical proxies (organic carbon, nitrogen, calcium carbonate and biogenic opal contents, Corg/S and Corg/N ratios, δ13C values of organic matter, and δ15N values) is a new approach for the study area. The chemical evidence of this multiproxy approach allows clear identification of several stages in the development of the lagoonal environment: postglacial lake stages with sandy sedimentation during the Older Dryas and the Allerød stades, lacustrine phases with high autochthonous productivity during the Atlantic stade, terrestrial stages with peat formation at the beginning of the Subboreal stade, sedimentation as a result of marine transgression, and brackish sedimentation after the formation of sand spits and barrier islands during the Subatlantic stade. The stages are the result of regional sea-level change owing to complex shoreline development. They support the tentative sea-level curve proposed nearly 20 years ago for the region. In addition, changes in Oder River input in response to climate conditions is monitored. Whereas high terrigenous input of organic matter from the Oder River occurred during periods of humid climate during the Allerød, Atlantic, and Subatlantic stades, Oder River discharge decreased with drier and cooler climate conditions during the Subboreal stade. Furthermore, the geochemical evidence points to local anomalies such as the significance of river input and additional sulfate supply into the Oder lagoon for the composition of the sediments. Overall, the results provide a framework for future studies, which would allow for a more detailed comparison with other, similar environments.

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Symposium Discussion: Some Notes on the Last Deglaciation in Northern Europe Compared with Canadian Conditions

Cited by 8 publications

References 0 publications

Glacial-Isostatic Adjustment-I. The Forward Problem

Glacial-Isostatic Adjustment-I. The Forward Problem

Holocene glacial rebound and sea-level change in NW Europe

Late- and Postglacial Sea-Level Change and Paleoenvironments in the Oder Estuary, Southern Baltic Sea

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