This section is only relevant when CAM 3.0 is coupled to a slab ocean. When sea ice is present, only a fraction of the melting potential from heat stored in the ocean actually reaches the ice at the base and side. The melting potential is
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(6.33) |
Usually only a fraction of is available to melt ice at the
base and side, and these fractions are determined from boundary-layer
theories at the ice-ocean interfaces. However, it is critical that the
sum of the fractions never exceeds one, otherwise ice formation might
become unstable. Hence we compute the upper-limit partitioning of
, even though these amounts are rarely
reached. The partitioning assumes
is dominated by shortwave
radiation and that shortwave radiation absorbed in the ocean surface
layer above the mean ice thickness causes side melting and below it
causes basal melting:
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(6.34) |
The heat flux for lateral melt is the product of the
vertically-summed, thickness-weighted
energy of melting of snow and ice
with the interfacial melting rate
and the total floe
perimeter
per unit floe area
. The interfacial melting rate
is taken from the empirical expression of Maykut and Perovich [124] based on
Marginal Ice Zone Experiment observations:
,
where
m s
deg
and
.
The lead-ice perimeter depends on the ice floe distribution and
geometry. For a mean floe diameter
and number of floes
,
and the floe area
[154].
Thus the heat flux for lateral melt is
, so that the actual amount used is:
The heat flux that is actually used by the ice model is then:
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(6.37) |
The net flux exchanged between ocean and ice also includes
the shortwave flux transmitted to the ocean through sea ice
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(6.38) |