By Kurt M. Cuffey, W. S. B. Paterson
Now in its 4th version, this vintage textual content covers the actual rules underlying the habit of glaciers -- terrestrial ice our bodies originating as accumulations of snow -- together with mountain glaciers, small ice caps, ice sheets, and cabinets. New fabric on weather switch contains interactions among ice sheets and the sea and surroundings, paleoclimate reconstruction utilizing ice cores, Quaternary weather historical past and the ice a long time, and sea point upward thrust. The ebook additionally explores themes of curiosity to geologists and geophysicists, together with glacial connections to geomorphology, sedimentation, isostasy, and tectonics.
-Completely up to date and revised, with 30% new fabric together with weather change
-Accessible to scholars, and a necessary advisor for researchers
-Authored via preeminent glaciologists
Read or Download The Physics of Glaciers (4th Edition) PDF
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Extra resources for The Physics of Glaciers (4th Edition)
Example text
3): approximately 900 to 1600 m in central Greenland and 500 to 1200 m in central East Antarctica (Kipfstuhl et al. 2001). Within these transition zones, clathrates and bubbles coexist. Salamatin et al. (1997; 2001; 2004) constructed a plausible model for this process, albeit one that probably oversimplifies the situation (Shimada and Hondoh 2004; Kipfstuhl et al. 2001). 3 Texture and Recrystallization The distribution of grain sizes and shapes in polycrystalline ice constitute the texture. Grain size is quantified by an effective diameter (D), radius, or cross-sectional area.
The driving force for densification is the weight of overburden (the load). Per unit horizontal area, at depth z below the surface, the load amounts to P = g ρ(z)dz. Only the ice grains, not the voids, support the load; the grain-load stress, P∗ , equals ρi P/ρ. The rate of densification should increase with P∗ . 2. The effective driving force depends not just on the applied load but on the difference between the vertical and horizontal stresses. This is related to the geometry of the ice skeleton.
Air spaces are filled in this way. Refreezing of large quantities of meltwater to form ice layers and lenses represents 28 Chapter 2 a rapid transition from snow to ice. The time needed to complete the transformation varies widely between different areas according to the amount of meltwater. A superimposed-ice zone represents the extreme case in which snow transforms to ice in a single summer. 3, gives an example. Because melting and refreezing increase the average density of the firn, they also reduce the elevation of the surface by a small amount.