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For sea ice, L is the effective latent heat of sea ice and is the density of sea ice. These two parameters depend on sea-ice salinity, temperature, and volumetric gas fraction, as well as sea-ice thermal conductivity. The growth rate of sea ice in turn determines the saline content of the newly frozen ice.
First-year sea ice is ice that is thicker than young ice but has no more than one year growth. In other words, it is ice that grows in the fall and winter (after it has gone through the new ice – nilas – young ice stages and grows further) but does not survive the spring and summer months (it melts away). The thickness of this ice typically ...
The Arctic sea ice minimum is the day in a given year when Arctic sea ice reaches its smallest extent, occurring at the end of the summer melting season, normally during September. Arctic Sea ice maximum is the day of a year when Arctic sea ice reaches its largest extent near the end of the Arctic cold season, normally during March. [14]
The Arctic has already lost about half of its sea ice, compared to the 1980s at the end of the summer. It is known that more warming has delayed ice formation, and resulted in thinner sea ice growth.
Sea ice mass balance is the balance of how much the ice grows in the winter and melts in the summer. For Arctic sea ice virtually all of the growth occurs on the bottom of the ice. Melting occurs on both the top and the bottom of the ice. In the vast majority of cases all of the snow melts during the summer, typically in just a couple of weeks.
The Arctic sea ice covers less area in the summer than in the winter. The multi-year (i.e. perennial) sea ice covers nearly all of the central deep basins. The Arctic sea ice and its related biota are unique, and the year-round persistence of the ice has allowed the development of ice endemic species, meaning species not found anywhere else.
The classical Stefan problem aims to describe the evolution of the boundary between two phases of a material undergoing a phase change, for example the melting of a solid, such as ice to water. This is accomplished by solving heat equations in both regions, subject to given boundary and initial conditions.
Sea ice freeboard is the difference between the height of the surface of sea ice and the water in open leads. Since 85–95% of snow-free sea ice is usually located below the waterline, the computation of the thickness is fairly simple; [ 3 ] however, accurate measurement of ice freeboard is hindered by several factors including snow cover, and ...