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Jökull - 01.12.1987, Qupperneq 77

Jökull - 01.12.1987, Qupperneq 77
affecting the Ásbakkar diamicton, is exposed (Fig. 17), showing the lower uninverted limb, a streaked out trough hinge zone and part of the inverted limb. The exposure trends N-S, and as the fold axis trends 105°- 285° with an axial plane dipping about 18° towards 15°, the exposure cuts the fold sub-perpendicularly to the fold axis. Therefore, folded surfaces sub-parallell to the axial plane are exposed, and examples of “slaty cleav- age-like” axial plane foliations can be seen above the streaked out trough hinge zone. The fold geometry in- dicates a deforming push from approximately NNE. Faults and joints The Ásbakkar diamicton, south of about 3700 m, is transected by a number of major normal and low angled reverse (thrust) faults (Fig. 2). The thrust fault planes are usually slightly concave upwards. Measurements of 10 fault planes revealed apparent dips between 28° and 42° towards NW-N. At 4975 m the Asbakkar diamicton is transected by a thrust fault, running slightly concavely upwards from the base of the sequence (Fig. 18). Imme- diately below the thrust plane there is a body of stratified sand, which has been subject to fault drag. The drag has overturned the sand with a minimum displacement of about 5 m along the thrust plane. The displacement strike of the sand body measured 80°-260°, which is perpendicular to the direction of the section and in- dicates a displacement approximately normal to the out- cropping trace of the fault, towards SSE-S. The thrust faults belong to the same dislocation pattern as the large-scale folds, showing a direction of maximal stress from north. The Ásbakkar diamicton and the glaciomarine facies of the Látrar beds are at places heavily jointed. The most apparent joints are sub-vertical to vertical joints, usually spaced at 10-25 cm intervals. Sometimes the joints can be traced over entire unit thicknesses, giving the cliff face a columnar-like appearance. In connection with folds and faults, straight to undulating, sub-parallel fractures occur (Fig. 6A). They appear to strike parallel to the associated sheared structure, and dip in opposite directions to shear planes and axial planes. Similar joints in sub-till sediments have been described as tension fractures by Hicock and Dreimanis (1985). Glaciodynamic deformations: a discussion Although the study of glaciotectonic structures has a long tradition (for short reviews, see Berthelsen 1978, Aber 1982, Hicock and Dreimanis 1985), many funda- mental problems of their development still remain to be satisfactorily explained. There are two schools of thought as to whether large scale dislocations take place mainly in front of advancing glaciers (e.g. Berthelsen 1979), or beneath advancing glaciers via compressive flow in the basal zone (e.g. Moran 1971). Another funda- mental problem with regard to the conditions at the base of the ice is whether glaciotectonic deformations devel- op in frozen or unfrozen sediments, and consequently the role of basal meltwater, pore-water pressure and permeability of the substratum. Two basic concepts have been presented regarding the connection between the basal/frontal situation and the development of gla- ciotectonic structures: A “permafrost concept” which assumes that the effect of differential glacier load and shearing stress is transmitted from the moving glacier to its frozen pro- and substratum, causing the formation of glaciotectonic structures (e.g. Moran et al. 1980, Aber 1982). The other concept calls upon the combined effect of differential ice loading and hydrodynamic mecha- nisms to account for the development of glaciotectonic structures, and points out the potential importance of Fig. 16. Deformation structures. (A) A thrust fault de- veloped from an angular fold in the Ásbakkar diamicton below the Melar diamicton at 1525 m. The inverted limb of the fold has been replaced by a slide plane. Drawn from a photograph; (B) A schematic field sketch of an open, asymmetrical anticlinal structure, developed in the Látrar glaciomarine facies beneath the Melar dia- micton at 2400 m. 16. mynd. Dœmi um sköruð og kýtt jarðlög. 75
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