| 227 |
with a constant ice conductivity. It is expressed as |
with a constant ice conductivity. It is expressed as |
| 228 |
$(K/h)(T_{w}-T_{0})$, where $K$ is the ice conductivity, $h$ the ice |
$(K/h)(T_{w}-T_{0})$, where $K$ is the ice conductivity, $h$ the ice |
| 229 |
thickness, and $T_{w}-T_{0}$ the difference between water and ice |
thickness, and $T_{w}-T_{0}$ the difference between water and ice |
| 230 |
surface temperatures. TThis type of model is often refered to as a |
surface temperatures. This type of model is often refered to as a |
| 231 |
``zero-layer'' model. The surface heat flux is computed in a similar |
``zero-layer'' model. The surface heat flux is computed in a similar |
| 232 |
way to that of \citet{parkinson79} and \citet{manabe79}. |
way to that of \citet{parkinson79} and \citet{manabe79}. |
| 233 |
|
|
| 234 |
The conductive heat flux depends strongly on the ice thickness $h$. |
The conductive heat flux depends strongly on the ice thickness $h$. |
| 235 |
However, the ice thickness in the model represents a mean over a |
However, the ice thickness in the model represents a mean over a |
| 252 |
\citet{menemenlis05}, this flux is not assumed to instantaneously melt |
\citet{menemenlis05}, this flux is not assumed to instantaneously melt |
| 253 |
or create ice, but a time scale of three days is used to relax $T_{w}$ |
or create ice, but a time scale of three days is used to relax $T_{w}$ |
| 254 |
to the freezing point.} |
to the freezing point.} |
| 255 |
|
% |
| 256 |
The parameterization of lateral and vertical growth of sea ice follows |
The parameterization of lateral and vertical growth of sea ice follows |
| 257 |
that of \citet{hibler79, hibler80}. |
that of \citet{hibler79, hibler80}. |
| 258 |
|
|
| 259 |
On top of the ice there is a layer of snow that modifies the heat flux |
On top of the ice there is a layer of snow that modifies the heat flux |
| 260 |
and the albedo \citep{zhang98}. If enough snow accumulates so that its |
and the albedo \citep{zhang98}. Snow modifies the effective |
| 261 |
weight submerges the ice and the snow is flooded, a simple mass |
conductivity according to |
| 262 |
conserving parameterization of snowice formation (a flood-freeze |
\[\frac{K}{h} \rightarrow \frac{1}{\frac{h_{s}}{K_{s}}+\frac{h}{K}},\] |
| 263 |
algorithm following Archimedes' principle) turns snow into ice until |
where $K_s$ is the conductivity of snow and $h_s$ the snow thickness. |
| 264 |
the ice surface is back at $z=0$ \citep{leppaeranta83}. |
If enough snow accumulates so that its weight submerges the ice and |
| 265 |
|
the snow is flooded, a simple mass conserving parameterization of |
| 266 |
|
snowice formation (a flood-freeze algorithm following Archimedes' |
| 267 |
|
principle) turns snow into ice until the ice surface is back at $z=0$ |
| 268 |
|
\citep{leppaeranta83}. |
| 269 |
|
|
| 270 |
Effective ice thickness (ice volume per unit area, |
Effective ice thickness (ice volume per unit area, |
| 271 |
$c\cdot{h}$), concentration $c$ and effective snow thickness |
$c\cdot{h}$), concentration $c$ and effective snow thickness |
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