Hostname: page-component-76fb5796d-22dnz Total loading time: 0 Render date: 2024-04-25T11:33:25.817Z Has data issue: false hasContentIssue false
  • English
  • Français

Ice motion on deformable sediments

Published online by Cambridge University Press:  20 January 2017

W. Haeberli
W. Haeberli*
Affiliation:
Versuchsanstalt für Wasserbau, Hydrologie und Glaziologie, Eidg. Technische Hochschule Zürich, Gloriastrasse 37/39, 8092 Zürich, Switzerland
Rights & Permissions [Opens in a new window]

Abstract

An abstract is not available for this content. As you have access to this content, full HTML content is provided on this page. A PDF of this content is also available in through the ‘Save PDF’ action button.
Type
Correspondence
Information
Journal of Glaciology , Volume 27 , Issue 96 , 1981 , pp. 365 - 366
Copyright
Copyright © International Glaciological Society 1981

The Editor,

Journal of Glaciology

Sir,

The phenomenon of the deformation of subglacial sediments under high pore-water pressure has recently entered the discussion about the dynamics of different ice masses. Reference LliboutryLliboutry (1977) assumed deformation of unfrozen subglacial sediments to occur in the case of Glaciar Hatunraju in the Cordillera Blanca, Peru. Reference Fisch, Fisch, Fisch and HacberliFisch and others (1978) and Reference Haeberli, Haeberli, King and FlotronHaeberli and others (1979) suggested that the deformation of sub-permafrost sediments under high pore-water pressure may account for the seasonal velocity variations of active rock glaciers in the Alps (Barsch and Hell, [1976]). Based on direct observations at the margin of Breiòamerkurjökull in Iceland, Reference Boulton and JonesBoulton and Jones (1979) proposed that the behaviour of Pleistocene ice sheets may have been largely influenced by the deformation of unfrozen subgtacial sediments. The present author feels uneasy about this direct comparison between a local observation at the margin of an actual glacier in a maritime climate and large-scale processes at the base of Pleistocene ice sheets under very different climatic conditions.

In their discussion about geologic evidence for former subglacial deformation of unfrozen sediments Reference Boulton and JonesBoulton and Jones (1979) make reference to tectonically disturbed Pleistocene morainic deposits described, e.g. by Reference KupschKupsch (1962) and Reference WoldstedtWoldstedt (1954, Reference Woldstedt1965), stating that the bed of Quaternary ice sheets in Europe and North America may have been unstable in parts. In the context of the current discussion this argumentation could be misleading. A long time ago it was already recognized that folding and overthrusting of layers of unconsolidated sediments up to tens of metres thick is only possible if the sediments are frozen and the rock matrix is cemented by ice (sec Kälin, 1971, for references). In a recent contribution Reference Schindler, Schindler, RÖthlisberger and GygerSchindler and others (1978) discussed the problem of stress transmission from the glacier to the sediments and concluded that shear stresses increase along the base of the glacier in the marginal zone, where the ice is frozen to the sediments. Some subglacial deformation of frozen sediments may take place, but the highest stresses and, thus, strong strains occur at the glacier front. In the strict sense of Reference Embleton and KingEmbleton and King (1968)—corresponding to the meaning of the German expression Stauch moränen—the “push moraines” described by Kupsch and Woldstedt are undoubtedly proglacial features in a permafrost condition and actually occur in Arctic and alpine permafrost regions only (Kälin, 1971; Haeberli, 1979). They cannot serve as examples for subglacial deformation of unfrozen sediments.

This point needs further consideration, because some of the phenomena involved may set important boundary conditions for a theory of deforming glacier beds. Pleistocene glaciers and ice sheets in Europe bad their ablation zones in an environment of a very cold continental climate and continuous permafrost. The maximum depression of the mean annual air temperature during the last glaciation was at least 10 to 12 deg (Washburn, [1979]). The mean annual air temperature at the equilibrium line of Alpine glaciers during this time was on the order of — 10°C. This does not necessarily imply that the glaciers were cold-based everywhere, but it certainly means that they were frozen to their (sediment) beds in a marginal zone of unknown extent. Such a marginal zone of cold ice and subglacial permafrost represents a barrier to all three parts of the dynamic and interacting ice-water-sediment system. The cold marginal zone especially acts as a barrier to the sediment flux at the base of the ice. The question of whether the flux of sediments through upward transportation from the bed to the surface at the boundary between cold- and warm-based ice (Weertman, 1961, 1966; Souchez, 1967; Hooke, 1968) is of the same order as the flux of sediments along the base of the glacier due to deformation of unfrozen subglacial sediments at a rate which is comparable to the sliding velocity of the glacier, needs quantitative consideration. It may also be useful to remember that even today wide parts of the beds of alpine glaciers do not consist of hard bedrock but of till as has been revealed by seismic reflection in earlier studies (see Süsstrunk, 1951, for references). This seems to contradict the assumption of an extremely effective erosional process at glacier beds consisting of unconsolidated sediments such as the process of fast largescale deformation of unfrozen subgiacial sediments proposed by Reference Boulton and JonesBoulton and Jones (1979).

References

Barsch, D., and Hell, G. [1976.] Photogrammetrische Bewegungsmessungen am Blockgletscher Murtèl 1, Oberengadin, Schweizer Alpen. Zeitschrift für Gletsckerkunde und Glazialgeologie, Bd. 11, Ht. 2, 1975 p. 111–42.Google Scholar
Boulton, G. S., and Jones, A. S. 1979. Stability of temperate ice caps and ice sheets resting on beds of deformable sediment. Journal of Glaciology. Vol. 24, No. 90, p. 29–43.CrossRefGoogle Scholar
Embleton, C., and King, C. A. M. 1968. Glacial and periglacial geomorphology. London, Edward Arnold Ltd..Google Scholar
srFisch, W., and others [1978.] Electrical D.C. resistivity soundings with long profiles on rock glaciers and moraines in the Alps of Switzerland, by SrFisch, W., JrFisch, W., and Hacberli, W. Zeitschrift für Gletsckerkunde und Glazialgeologie, Bd. 13, Ht. 1–2,1977 p. 239–60.Google Scholar
Haeberli, W. 1979. Holocene push-moraines in alpine permafrost. Geografiska Annaler, Vol. 61A, Nos. 1–2, p. 43–48.CrossRefGoogle Scholar
Haeberli, W., and others, 1979. Surface movement and lichen-cover studies at the active rock glacier near the Grubengletscher, Wallis, Swiss Alps, by Haeberli, W., King, L., and Flotron, A. Arctic and Alpine Research, Vol. 11, No. 4, p. 421–41.Google Scholar
Hooke, R. L. 1968. comments on “The formation of shear moraines: an example from south Victoria Land, Antarctica”. Journal of Glaciology, vol. 7 No. 50, p. 351–52. [Letter.]CrossRefGoogle Scholar
Kälin, M. 1971. The active push moraine of the Thompson Glacier, Axel Heiberg Island, Canadian Arctic Archipelago, Canada. A dissertation submitted to the Swiss Federal Institute of Technology, Zürich, for the degree of Doctor of Natural Sciences. Montreal, McGill University.(Dissertation No. 4671.)Google Scholar
Kupsch, W.O. 1962. Ice-thrust ridges in western Canada. Journal of Geology, Vol. 70, No. 5, p. 582–94.CrossRefGoogle Scholar
Lliboutry, L. A. 1977. Glaciological problems set by the control of dangerous lakes in Cordillera Blanca, Peru. II. Movement of a covered glacier embedded within a rock glacier. Journal of Glaciology, Vol. 18, No. 79, p. 255–73.Google Scholar
Schindler, C., and others, 1978. Glaziale Stauchungen in den Niederterrassen-Schottern des Aadorfer Feldes und ihre Deutung, Schindler, von C., RÖthlisberger, H., and Gyger, M.. Ecologae Geologicae Helvetiae, Vol. 71/1, p. 159–74 Google Scholar
Souchez, R. A. 1967. The formation of shear moraines: an example from south Victoria Land, Antarctica. Journal of Geology, Vol. 6, No. 48, p. 837–43.Google Scholar
Süsstrunk, A. 1951. Sondage du glacier par la méthode sismique La Houille Blanche, 6e An., Numéro spécial A, p. 309–19 CrossRefGoogle Scholar
Washburn, A. L. 1979. Geocryology: a survey of periglacial processes and environments. London, Edward Arnold Ltd.Google Scholar
Weertman, J. 1961. Mechanism for the formation of inner moraines found near the edge of cold ice caps and ice sheets. Journal of Glaciology, Vol. 3 No. 30 p. 965–78.Google Scholar
Weertman, J. 1966. Effect of a basal water layer on the dimensions of ice sheets. Journal of Glaciology, Vol. 6 No. 44, p. 191–207.CrossRefGoogle Scholar
Woldstedt, P. 1954. Das Eiszeitalter: Grundlinien einer Geologie des Quartärs. Bd. 1 Die allgemeinen Erscheinungen des Eiszeitalters. Zweite Auflage. Stuttgart, Ferdinand Enke Verlag.Google Scholar
Woldstedt, P. 1965. Das Eiszeitalter: Grundlinien einer Geologie des Quartärs. Bd. 3 Afrika, Asien, Australien, und Amerika im Eiszeitalter. Zweite Auflage. Stuttgart, Ferdinand Enke Verlag.Google Scholar