By M. Jakobsson, A. Grantz, Y. Kristoffersen (auth.), Professor Dr. Ruediger Stein, Dr. Robie W. MacDonald (eds.)
From the reviews:
"The e-book is a unprecedented compilation of fascinating details and a succession of vital interpretations concerning the construction, supply, degradation, and burial of natural subject within the world’s merely polar ocean. … the 3 positive aspects of the publication that make it fairly distinct are its content material, its presentation, and its timeliness. … end result of the means that Stein and Macdonald have so successfully built-in and arranged a wealth of knowledge concerning the Arctic, many forms of scientists would receive advantages from it." (Phillip A. Meyers, Polar checklist, Vol. forty-one (3), 2005)
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Extra resources for The Organic Carbon Cycle in the Arctic Ocean
Example text
The greatest loss of sea-ice cover occurs during the period from June to October (Fig. 8 c, Serreze et al. 2000). The trends in ice cover with time (Figs. 8 b) suggest that the wholesale clearing of ice from shelves during summer is a phenomenon of the 1990s, timed with (Russian Shelves) or slightly delayed from (Beaufort Shelves) the shift to strong positive AO index in 1989. Maslanik et al. (1996) draw the connection between increased cyclones and increased poleward transport of heat, which are observed during high index conditions, and the absence of ice in late summer over the Siberian shelves.
From the composition and distribution of ice-rafted glacial erratics in late Quaternary sediments from the central Arctic Ocean, specific continental source areas such as the Canadian Arctic Islands and parts of Eurasia can be identified, thus allowing paleo-current systems to be reconstructed (e. , Phillips and Grantz 2001). With sea-level rise, about 15,000 years ago the Bering land bridge was flooded (Hopkins 1979) and then gradually submerged (Dyke et al. 1996) allowing the Pacific Ocean access to the Arctic Ocean.
1995). Precipitation minus evaporation (P–E) integrated over a drainage basin should be equivalent to river discharge for the basin. Arctic rivers exhibit large interannual variation (Semiletov et al. 2000; Shiklomanov et al. 2000; Stewart 2000) making it difficult to link river flow to precipitation or temperature trends or to climate variables like the AO. For example, Shiklomanov et al. (2000) suggested little change in mean annual discharge for arctic rivers between the 1920s and 1990s whereas Semiletov et al.