THE NEAR-SURFACE LAYER OF THE OCEAN
ice zone can, however, lead to the coupling of the drifting ice with the
internal wave field thus increasing the drag coefficient. This effect has been
observed during MIZEX (Morrison et al., 1987; McPhee and Kantha, 1989).
At times when winds are blowing off the ice, the ice edges of the ocean
are generally the site of regularly spaced (~20 km) surface bands of ice floes.
McPhee et al. (1987) suggested that this is a result of the coupling between
the internal wave field and ice floes; this coupling is possible due to stable
salinity stratification in the near-surface layer of the ocean maintained by
melting along the ice edges.
Smith and Nelson (1985) observed a dense phytoplankton bloom near a
receding ice edge off the coast of Victoria Land in the Antarctic. The bloom
area extended 250 km from the ice edge and was confined to waters where
melting ice had reduced salinity. Presumably, stable salinity stratification in
this area favored phytoplankton growth and accumulation.
An extensive phytoplankton bloom in the northern Gerlache Strait was
studied during the Research on Antarctic Coastal Ecosystem Rates (RACER;
see Karl, 1991). The bloom abruptly declined when the mixing layer depth
changed. It was concluded that the phytoplankton bloom was controlled
largely by the physical processes in the water column.
284
ice zone can, however, lead to the coupling of the drifting ice with the
internal wave field thus increasing the drag coefficient. This effect has been
observed during MIZEX (Morrison et al., 1987; McPhee and Kantha, 1989).
At times when winds are blowing off the ice, the ice edges of the ocean
are generally the site of regularly spaced (~20 km) surface bands of ice floes.
McPhee et al. (1987) suggested that this is a result of the coupling between
the internal wave field and ice floes; this coupling is possible due to stable
salinity stratification in the near-surface layer of the ocean maintained by
melting along the ice edges.
Smith and Nelson (1985) observed a dense phytoplankton bloom near a
receding ice edge off the coast of Victoria Land in the Antarctic. The bloom
area extended 250 km from the ice edge and was confined to waters where
melting ice had reduced salinity. Presumably, stable salinity stratification in
this area favored phytoplankton growth and accumulation.
An extensive phytoplankton bloom in the northern Gerlache Strait was
studied during the Research on Antarctic Coastal Ecosystem Rates (RACER;
see Karl, 1991). The bloom abruptly declined when the mixing layer depth
changed. It was concluded that the phytoplankton bloom was controlled
largely by the physical processes in the water column.
284