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  • A rational explanation of cross-profile morphology for glacial valleys and of glacial valley development
  • The purpose of this paper is, first to present an explanation of the cross-profile morphology based on the physical process of glacier flow and second to interpret development of the glacial valley cross-profile.
  • A rational explanation of cross-profile morphology for glacial valleys and of glacial valley development : a further note
  • The AA. discovered a misinterpretation in their original paper entitled : a rational explanation of cross-profile morphology for glacial valleys and of glacial valley development in earth surface processes and landforms, vol. 13, No 8, p. 707-716
  • A discussion of Hirano and Aniya's (1988, 1989) explanation of glacial-valley cross profile development, and reply
  • Late glacial hydrology of the upper Pite River Valley, Swedish Lapland
  • Morphological development of dunes in a subarctic environment, central Kobuk Valley, northwestern Alaska
  • The morphology of the dune fields is described by airphoto interpretation supplemented by field observations. Dune forms indicate that both present-day and former wind directions are parallel to the valley axis. Therefore it is proposed that wind
  • directions have not changed significantly since the last glacial time.
  • Submarine valleys can be subdivided into several types which differ considerably in genesis and morphology| besides submerged fluvial and glacial valleys (inherited relict features), several types of submarine valleys seem to be accounted
  • for by turbidity currents, i.e. submarine canyons, submarine gullies, abyssal valleys of continental rise and ocean floor. Rift valleys are formed by tectonics only| tectonic fractures contribute considerably into formation of submarine canyons and transversal
  • gorges crossing mid-oceanic ridges. Bottom abyssal currents are not sufficiently studied, but it is beyond any doubt that they participate in the formation of submarine valleys in deep ocean zones, in particular in inter-depression passes. It seems
  • that valleys due to turbidity currents were greatly influenced by Pleistocene glaciations. Ice edge was often situated close to shelf edge and debris melted from the ice created large turbidity currents which eroded not only continental slope but abyssal zones
  • Late-glacial and post-glacial development of the valleys of the Oulanka river basin, north-eastern Finland
  • Inherent factors in the flow of valley, glaciers as a possible influence in the formation of stepped glacial valleys
  • Source and origin of Roxana silt and middle Wisconsinan midcontinent glacial activity
  • Roxana distribution suggests the major source was drainage from the upper Mississippi River valley, and variations in loess thickness in Illinois can be explained by consideration of valley width, depth, orientation and post depositional erosion
  • The Gaick area is a landscape of selective linear glacial erosion. Deep weathering of Moine psammites occurs on preglacial slopes but is absent from glacially-overdeepened valleys. The weathering is of gruss type and its thickness, together
  • Glacio-karst closed depressions are the major large scale karst landforms of the Eastern Massif of the Picos de Europa. During valley glaciation the major depressions functioned as cirques, with smaller depressions also developing in the floor
  • of glacial troughs and in glacier margin locations. The major glacio-karst depressions developed at the locations of pre-glacial features where topo-climatic factors favoured snow accumulation.
  • Up to one fourth of the isotopic change in foraminifera found in deep-sea cores (or some 0.3 /) may be due to a gradual change in the isotopic composition of the Antarctic and Greenland ice sheets. Therefore the peak-to-valley variation of the 0
  • of formanifera cannot be used as a measure of the size of glacial ice sheets or of sea level lowerings unless corrected for this factor. The early stadial of a glacial (e.g. Weichselian at around 55,000 B.P.) might have been more intense than as appears from
  • The Weichselian Late Glacial in a small Lowland valley (Mark river, Belgium and the Netherlands)
  • Particle size, shape, and load in a cold and a temperate valley glacier
  • a wide range of silt and boulder sizes. Crushing into smaller pieces, rather than the removal of asperities is postulated as the dominant process of glacial erosion. Sediment loads are given for the glacial streams.
  • The AA. interpret the sedimentological, pedological, stratigraphic and thermoluminescence data as indicating that the period of loess deposition in the Kashmir valley dates to the last 200,000 yrs, with loess deposition and palaeosol formation
  • occurring during both glacial and interglacial phases.
  • Several abrasion surfaces, erosion net of submerged river valleys of glacial period were found due to research during diving, echosounding, submarine photographing, subbottom profiling and studies of quaternary sediments columns of the Seichell
  • and the Amirant banks. Temporal changes in sedimentation process connected with geomorphologic situation during the holocene oceanic level rise are shown. Double delay of post-glacial oceanic level rise and even its fall about 2-2,5 and 0,5-1,0 th.y.B.P
  • Kartometryczne metody wyznaczania zasiegu form m odoglacjalnych na przyk adzie Wysoczyzny Kolnenskiej. (Cartometric methods in determining the extent of young-glacial forms. A case study of the Kolno Upland)
  • and basins without outflows, per sq. km. The morphographic criterion consists in an analysis of the system of morphological forms and the spatial situation of the valleys. These methods allowed to investigate the extent of the maximal spread of the Baltic
  • Morphology, mass wasting and forest ecology of a post-glacial re-entrant valley in the Niagara escarpment
  • Late-Glacial and Postglacial sedimentation in Lake Superior based on seismic-reflection profiles
  • , acoustically transparent layer overlying a strong reflector, and (III) relatively thick sediment with internal acoustic reflectors. These profiles, in conjunction with sediment cores from the area, reveal that varved glacial-lacustrine sediment settled out
  • than 100 m| bottom currents prevent deposition or erode bottom sediment in certain deep-water (>200m) valleys| and lacustrine sediment is disturbed by creep or slumping off Grand Portage, Minnesota, and by other processes such as dewatering in many
  • of calcite crystalls rooted in the decalcified cortex| c. the mobilisation of iron and its precipitation in the shape of hydroxides. The same features are characteristic for areas of present day permafrost especially for valley lowlands with coarse glacial