Planets - User contributions [en]

Slab ocean model

2022-05-11T09:00:51Z

Bcharnay:

== A brief description of the slab ocean model ==

The slab ocean model is from Codron [2012]. This model uses the same horizontal grid as the GCM and is composed of two layers. The first layer (50 m depth) represents the surface mixed layer, where the exchanges with the atmosphere take place. The second layer (150 m depth) represents
the deep ocean. The transport of heat by the ocean circulation is given by two components. First, the impact of subgrid-scale eddies is represented by horizontal diffusion, with a uniform diffusivity in both layers. Then, the mean wind-driven circulation is computed by calculating
the Ekman mass fluxes in the surface layer from the surface wind stress and taking an opposite return flow at depth. These mass fluxes are then used to advect the ocean temperature horizontally. In the case of divergent horizontal mass fluxes, the upwelling or downwelling mass flux is obtained by continuity. This simplified model reproduces the global meridional oceanic heat transport quite closely compared to a full GCM.

The oceanic model also computes the formation of oceanic ice. Sea ice forms when the ocean temperature falls below –1.8°C and melts when its temperature rises above freezing. The changes in ice extent and thickness are computed based on energy conservation, keeping the ocean temperature at –1.8°C as long as ice is present. A layer of snow can be present above the ice. The surface albedo is then that of snow, or for bare ice:
A = A$$^\rm{max}_\rm{ice}$$ – (A$$^\rm{max}_\rm{ice}$$ – A$$^\rm{min}_\rm{ice}$$ ) exp(–h$$_\rm{ice}$$/h$$^0_\rm{ice}$$)
with A the albedo, A$$^\rm{max}_\rm{ice}$$ = 0.65 the maximal albedo, A$$^\rm{min}_\rm{ice}$$ =0.2 the minimal albedo, hice the ice thickness (in m) and h$$^0_\rm{ice}$$ = 0.5 m. The albedo over the ice-free ocean is taken to be equal to 0.07. The value for the maximal sea ice albedo we used (i.e., 0.65) is classical for GCMs.

== Variables of the slab ocean model which can be written as outputs in diagfi.nc ==

<ul>
<li>tslab1/tslab2: temperature of the two ocean layers (K)
<li>pctsrf_sic: fraction of sea ice
<li>sea_ice: mass of sea ice (kg/m$$^2$$)
<li>tsea_ice: temperature of the sea ice surface (K)
<li>dt_hdiff1/dt_hdiff2: heating of the ocean layers by diffusion (K/s)
<li>dt_ekman1/dt_ekman2: heating of the ocean layers by Ekman transport (K/s)
</ul>

== Technical aspects ==
The slab ocean model is activated in callphys.def with:
ok_slab_ocean = .true.

The sea ice model is activated in callphys.def with:
ok_slab_sic = .true.

The horizontal heat transport is activated in callphys.def with:
ok_slab_heat_transp = .true.
The horizontal heat transport cannot be activated in parallel at the moment.

Values of A$$^{max}_{ice}$$ and A$$^{min}_{ice}$$ are fixed in slab_ice_h.F90

Slab ocean model

2022-05-11T08:59:57Z

Bcharnay:

Slab ocean model

2022-05-11T08:53:57Z

Bcharnay:

Slab ocean model

2022-05-11T08:52:26Z

Bcharnay:

The slab ocean model is from Codron [2012]. This model uses the same horizontal grid as the GCM and is composed of two layers. The first layer (50 m depth) represents the surface mixed layer, where the exchanges with the atmosphere take place. The second layer (150 m depth) represents
the deep ocean. The transport of heat by the ocean circulation is given by two components. First, the impact of subgrid-scale eddies is represented by horizontal diffusion, with a uniform diffusivity in both layers. Then, the mean wind-driven circulation is computed by calculating
the Ekman mass fluxes in the surface layer from the surface wind stress and taking an opposite return flow at depth. These mass fluxes are then used to advect the ocean temperature horizontally. In the case of divergent horizontal mass fluxes, the upwelling or downwelling mass flux is obtained by continuity. This simplified model reproduces the global meridional oceanic heat transport quite closely compared to a full GCM.

The oceanic model also computes the formation of oceanic ice. Sea ice forms when the ocean temperature falls below –1.8°C and melts when its temperature rises above freezing. The changes in ice extent and thickness are computed based on energy conservation, keeping the ocean temperature at –1.8°C as long as ice is present. A layer of snow can be present above the ice. The surface albedo is then that of snow, or for bare ice:
A = A$$^\rm{max}_\rm{ice}$$ – (A$$^\rm{max}_\rm{ice}$$ – A$$^\rm{min}_\rm{ice}$$ ) exp(–h$$_\rm{ice}$$/h$$^0_\rm{ice}$$)
with A the albedo, A$$^\rm{max}_\rm{ice}$$ = 0.65 the maximal albedo, A$$^\rm{min}_\rm{ice}$$ =0.2 the minimal albedo, hice the ice thickness (in m) and h$$^0_\rm{ice}$$ = 0.5 m. The albedo over the ice-free ocean is taken to be equal to 0.07. The value for the maximal sea ice albedo we used (i.e., 0.65) is classical for GCMs.

== Variables of the slab ocean model which can be written as outputs in diagfi.nc ==

<ul>
<li>tslab1/tslab2: temperature of the two ocean layers (K)
<li>pctsrf_sic: fraction of sea ice
<li>sea_ice: mass of sea ice (kg/m$$^2$$)
<li>tsea_ice: temperature of the sea ice surface (K)
<li>dt_hdiff1/dt_hdiff2: heating of the ocean layers by diffusion (K/s)
<li>dt_ekman1/dt_ekman2: heating of the ocean layers by Ekman transport (K/s)
</ul>

== Technical aspects ==
The slab ocean model is activated in callphys.def with:
ok_slab_ocean = .true.

The sea ice model is activated in callphys.def with:
ok_slab_sic = .true.

The horizontal heat transport is activated in callphys.def with:
ok_slab_heat_transp = .true.
The horizontal heat transport cannot be activated in parallel at the moment.

Values of A$$^{max}_{ice}$$ and A$$^{min}_{ice}$$ are fixed in slab_ice_h.F90

Slab ocean model

2022-05-11T08:48:20Z

Bcharnay: /* Variables of the slab ocean which can be written in diagfi.nc */

The slab ocean model is from Codron [2012]. This model uses the same horizontal grid as the GCM and is composed of two layers. The first layer (50 m depth) represents the surface mixed layer, where the exchanges with the atmosphere take place. The second layer (150 m depth) represents
the deep ocean. The transport of heat by the ocean circulation is given by two components. First, the impact of subgrid-scale eddies is represented by horizontal diffusion, with a uniform diffusivity in both layers. Then, the mean wind-driven circulation is computed by calculating
the Ekman mass fluxes in the surface layer from the surface wind stress and taking an opposite return flow at depth. These mass fluxes are then used to advect the ocean temperature horizontally. In the case of divergent horizontal mass fluxes, the upwelling or downwelling mass flux is obtained by continuity. This simplified model reproduces the global meridional oceanic heat transport quite closely compared to a full GCM.

The oceanic model also computes the formation of oceanic ice. Sea ice forms when the ocean temperature falls below –1.8°C and melts when its temperature rises above freezing. The changes in ice extent and thickness are computed based on energy conservation, keeping the ocean temperature at –1.8°C as long as ice is present. A layer of snow can be present above the ice. The surface albedo is then that of snow, or for bare ice:
A = A$$^\rm{max}_\rm{ice}$$ – (A$$^\rm{max}_\rm{ice}$$ – A$$^\rm{min}_\rm{ice}$$ ) exp(–h$$_\rm{ice}$$/h$$^0_\rm{ice}$$)
with A the albedo, A$$^\rm{max}_\rm{ice}$$ = 0.65 the maximal albedo, A$$^\rm{min}_\rm{ice}$$ =0.2 the minimal albedo, hice the ice thickness (in m) and h$$^0_\rm{ice}$$ = 0.5 m. The albedo over the ice-free ocean is taken to be equal to 0.07. The value for the maximal sea ice albedo we used (i.e., 0.65) is classical for GCMs.

== Variables of the slab ocean model which can be written in diagfi.nc ==

<ul>
<li>tslab1/tslab2: temperature of the two ocean layers (K)
<li>pctsrf_sic: fraction of sea ice
<li>sea_ice: mass of sea ice (kg/m$$^2$$)
<li>tsea_ice: temperature of the sea ice surface (K)
<li>dt_hdiff1/dt_hdiff2: heating of the ocean layers by diffusion (K/s)
<li>dt_ekman1/dt_ekman2: heating of the ocean layers by Ekman transport (K/s)
</ul>

== Technical aspects ==
The slab ocean model is activated in callphys.def with:
ok_slab_ocean = .true.

The sea ice model is activated in callphys.def with:
ok_slab_sic = .true.

The horizontal heat transport is activated in callphys.def with:
ok_slab_heat_transp = .true.
The horizontal heat transport cannot be activated in parallel at the moment.

Values of A$$^{max}_{ice}$$ and A$$^{min}_{ice}$$ are fixed in slab_ice_h.F90

Slab ocean model

2022-05-11T08:47:10Z

Bcharnay:

The slab ocean model is from Codron [2012]. This model uses the same horizontal grid as the GCM and is composed of two layers. The first layer (50 m depth) represents the surface mixed layer, where the exchanges with the atmosphere take place. The second layer (150 m depth) represents
the deep ocean. The transport of heat by the ocean circulation is given by two components. First, the impact of subgrid-scale eddies is represented by horizontal diffusion, with a uniform diffusivity in both layers. Then, the mean wind-driven circulation is computed by calculating
the Ekman mass fluxes in the surface layer from the surface wind stress and taking an opposite return flow at depth. These mass fluxes are then used to advect the ocean temperature horizontally. In the case of divergent horizontal mass fluxes, the upwelling or downwelling mass flux is obtained by continuity. This simplified model reproduces the global meridional oceanic heat transport quite closely compared to a full GCM.

The oceanic model also computes the formation of oceanic ice. Sea ice forms when the ocean temperature falls below –1.8°C and melts when its temperature rises above freezing. The changes in ice extent and thickness are computed based on energy conservation, keeping the ocean temperature at –1.8°C as long as ice is present. A layer of snow can be present above the ice. The surface albedo is then that of snow, or for bare ice:
A = A$$^\rm{max}_\rm{ice}$$ – (A$$^\rm{max}_\rm{ice}$$ – A$$^\rm{min}_\rm{ice}$$ ) exp(–h$$_\rm{ice}$$/h$$^0_\rm{ice}$$)
with A the albedo, A$$^\rm{max}_\rm{ice}$$ = 0.65 the maximal albedo, A$$^\rm{min}_\rm{ice}$$ =0.2 the minimal albedo, hice the ice thickness (in m) and h$$^0_\rm{ice}$$ = 0.5 m. The albedo over the ice-free ocean is taken to be equal to 0.07. The value for the maximal sea ice albedo we used (i.e., 0.65) is classical for GCMs.

== Variables of the slab ocean which can be written in diagfi.nc ==

<ul>
<li>tslab1/tslab2: temperature of the two ocean layers (K)
<li>pctsrf_sic: fraction of sea ice
<li>sea_ice: mass of sea ice (kg/m$$^2$$)
<li>tsea_ice: temperature of the sea ice surface (K)
<li>dt_hdiff1/dt_hdiff2: heating of the ocean layers by diffusion (K/s)
<li>dt_ekman1/dt_ekman2: heating of the ocean layers by Ekman transport (K/s)
</ul>

== Technical aspects ==
The slab ocean model is activated in callphys.def with:
ok_slab_ocean = .true.

The sea ice model is activated in callphys.def with:
ok_slab_sic = .true.

The horizontal heat transport is activated in callphys.def with:
ok_slab_heat_transp = .true.
The horizontal heat transport cannot be activated in parallel at the moment.

Values of A$$^{max}_{ice}$$ and A$$^{min}_{ice}$$ are fixed in slab_ice_h.F90

Slab ocean model

2022-05-11T08:44:56Z

Bcharnay:

The slab ocean model is from Codron [2012]. This model uses the same horizontal grid as the GCM and is composed of two layers. The first layer (50 m depth) represents the surface mixed layer, where the exchanges with the atmosphere take place. The second layer (150 m depth) represents
the deep ocean. The transport of heat by the ocean circulation is given by two components. First, the impact of subgrid-scale eddies is represented by horizontal diffusion, with a uniform diffusivity in both layers. Then, the mean wind-driven circulation is computed by calculating
the Ekman mass fluxes in the surface layer from the surface wind stress and taking an opposite return flow at depth. These mass fluxes are then used to advect the ocean temperature horizontally. In the case of divergent horizontal mass fluxes, the upwelling or downwelling mass flux is obtained by continuity. This simplified model reproduces the global meridional oceanic heat transport quite closely compared to a full GCM.

The oceanic model also computes the formation of oceanic ice. Sea ice forms when the ocean temperature falls below –1.8°C and melts when its temperature rises above freezing. The changes in ice extent and thickness are computed based on energy conservation, keeping the ocean temperature at –1.8°C as long as ice is present. A layer of snow can be present above the ice. The surface albedo is then that of snow, or for bare ice:
A = A$$^\rm{max}_\rm{ice}$$ – (A$$^\rm{max}_\rm{ice}$$ – A$$^\rm{min}_\rm{ice}$$ ) exp(–h$$_\rm{ice}$$/h$$^0_\rm{ice}$$)
with A the albedo, A$$^\rm{max}_\rm{ice}$$ = 0.65 the maximal albedo, A$$^\rm{min}_\rm{ice}$$ =0.2 the minimal albedo, hice the ice thickness (in m) and h$$^0_\rm{ice}$$ = 0.5 m. The albedo over the ice-free ocean is taken to be equal to 0.07. The value for the maximal sea ice albedo we used (i.e., 0.65) is classical for GCMs.

== Variables of the slab ocean which can be written in diagfi.nc ==

tslab1/tslab2: temperature of the two ocean layers (K)

pctsrf_sic: fraction of sea ice

sea_ice: mass of sea ice (kg/m$$^2$$)

tsea_ice: temperature of the sea ice surface (K)

dt_hdiff1/dt_hdiff2: heating of the ocean layers by diffusion (K/s)

dt_ekman1/dt_ekman2: heating of the ocean layers by Ekman transport (K/s)

== Technical aspects ==
The slab ocean model is activated in callphys.def with:
ok_slab_ocean = .true.

The sea ice model is activated in callphys.def with:
ok_slab_sic = .true.

The horizontal heat transport is activated in callphys.def with:
ok_slab_heat_transp = .true.
The horizontal heat transport cannot be activated in parallel at the moment.

Values of A$$^{max}_{ice}$$ and A$$^{min}_{ice}$$ are fixed in slab_ice_h.F90

Slab ocean model

2022-05-11T08:44:30Z

Bcharnay:

The slab ocean model is from Codron [2012]. This model uses the same horizontal grid as the GCM and is composed of two layers. The first layer (50 m depth) represents the surface mixed layer, where the exchanges with the atmosphere take place. The second layer (150 m depth) represents
the deep ocean. The transport of heat by the ocean circulation is given by two components. First, the impact of subgrid-scale eddies is represented by horizontal diffusion, with a uniform diffusivity in both layers. Then, the mean wind-driven circulation is computed by calculating
the Ekman mass fluxes in the surface layer from the surface wind stress and taking an opposite return flow at depth. These mass fluxes are then used to advect the ocean temperature horizontally. In the case of divergent horizontal mass fluxes, the upwelling or downwelling mass flux is obtained by continuity. This simplified model reproduces the global meridional oceanic heat transport quite closely compared to a full GCM.

The oceanic model also computes the formation of oceanic ice. Sea ice forms when the ocean temperature falls below –1.8°C and melts when its temperature rises above freezing. The changes in ice extent and thickness are computed based on energy conservation, keeping the ocean temperature at –1.8°C as long as ice is present. A layer of snow can be present above the ice. The surface albedo is then that of snow, or for bare ice:
A = A$$^\rm{max}_\rm{ice}$$ – (A$$^\rm{max}_\rm{ice}$$ – A$$^\rm{min}_\rm{ice}$$ ) exp(–h$$_\rm{ice}$$/h$$^0_\rm{ice}$$)
with A the albedo, A$$^\rm{max}_\rm{ice}$$ = 0.65 the maximal albedo, A$$^\rm{min}_\rm{ice}$$ =0.2 the minimal albedo, hice the ice thickness (in m) and h$$^0_\rm{ice}$$ = 0.5 m. The albedo over the ice-free ocean is taken to be equal to 0.07. The value for the maximal sea ice albedo we used (i.e., 0.65) is classical for GCMs.

== Variables of the slab ocean which can be written in $$diagfi.nc$$ ==

tslab1/tslab2: temperature of the two ocean layers (K)

pctsrf_sic: fraction of sea ice

sea_ice: mass of sea ice (kg/m$$^2$$)

tsea_ice: temperature of the sea ice surface (K)

dt_hdiff1/dt_hdiff2: heating of the ocean layers by diffusion (K/s)

dt_ekman1/dt_ekman2: heating of the ocean layers by Ekman transport (K/s)

== Technical aspects ==
The slab ocean model is activated in callphys.def with:
ok_slab_ocean = .true.

The sea ice model is activated in callphys.def with:
ok_slab_sic = .true.

The horizontal heat transport is activated in callphys.def with:
ok_slab_heat_transp = .true.
The horizontal heat transport cannot be activated in parallel at the moment.

Values of A$$^{max}_{ice}$$ and A$$^{min}_{ice}$$ are fixed in slab_ice_h.F90

Slab ocean model

2022-05-11T08:43:41Z

Bcharnay:

The slab ocean model is from Codron [2012]. This model uses the same horizontal grid as the GCM and is composed of two layers. The first layer (50 m depth) represents the surface mixed layer, where the exchanges with the atmosphere take place. The second layer (150 m depth) represents
the deep ocean. The transport of heat by the ocean circulation is given by two components. First, the impact of subgrid-scale eddies is represented by horizontal diffusion, with a uniform diffusivity in both layers. Then, the mean wind-driven circulation is computed by calculating
the Ekman mass fluxes in the surface layer from the surface wind stress and taking an opposite return flow at depth. These mass fluxes are then used to advect the ocean temperature horizontally. In the case of divergent horizontal mass fluxes, the upwelling or downwelling mass flux is obtained by continuity. This simplified model reproduces the global meridional oceanic heat transport quite closely compared to a full GCM.

The oceanic model also computes the formation of oceanic ice. Sea ice forms when the ocean temperature falls below –1.8°C and melts when its temperature rises above freezing. The changes in ice extent and thickness are computed based on energy conservation, keeping the ocean temperature at –1.8°C as long as ice is present. A layer of snow can be present above the ice. The surface albedo is then that of snow, or for bare ice:
A = A$$^\rm{max}_\rm{ice}$$ – (A$$^\rm{max}_\rm{ice}$$ – A$$^\rm{min}_\rm{ice}$$ ) exp(–h$$_\rm{ice}$$/h$$^0_\rm{ice}$$)
with A the albedo, A$$^\rm{max}_\rm{ice}$$ = 0.65 the maximal albedo, A$$^\rm{min}_\rm{ice}$$ =0.2 the minimal albedo, hice the ice thickness (in m) and h$$^0_\rm{ice}$$ = 0.5 m. The albedo over the ice-free ocean is taken to be equal to 0.07. The value for the maximal sea ice albedo we used (i.e., 0.65) is classical for GCMs.

== Variables of the slab ocean which can be written in diagfi.nc ==

tslab1/tslab2: temperature of the two ocean layers (K)

pctsrf_sic: fraction of sea ice

sea_ice: mass of sea ice (kg/m$$^2$$)

tsea_ice: temperature of the sea ice surface (K)

dt_hdiff1/dt_hdiff2: heating of the ocean layers by diffusion (K/s)

dt_ekman1/dt_ekman2: heating of the ocean layers by Ekman transport (K/s)

== Technical aspects ==
The slab ocean model is activated in callphys.def with:
ok_slab_ocean = .true.

The sea ice model is activated in callphys.def with:
ok_slab_sic = .true.

The horizontal heat transport is activated in callphys.def with:
ok_slab_heat_transp = .true.
The horizontal heat transport cannot be activated in parallel at the moment.

Values of A$$^{max}_{ice}$$ and A$$^{min}_{ice}$$ are fixed in slab_ice_h.F90

Slab ocean model

2022-05-11T08:36:48Z

Bcharnay:

The slab ocean model is from Codron [2012]. This model uses the same horizontal grid as the GCM and is composed of two layers. The first layer (50 m depth) represents the surface mixed layer, where the exchanges with the atmosphere take place. The second layer (150 m depth) represents
the deep ocean. The transport of heat by the ocean circulation is given by two components. First, the impact of subgrid-scale eddies is represented by horizontal diffusion, with a uniform diffusivity in both layers. Then, the mean wind-driven circulation is computed by calculating
the Ekman mass fluxes in the surface layer from the surface wind stress and taking an opposite return flow at depth. These mass fluxes are then used to advect the ocean temperature horizontally. In the case of divergent horizontal mass fluxes, the upwelling or downwelling mass flux is obtained by continuity. This simplified model reproduces the global meridional oceanic heat transport quite closely compared to a full GCM.

The oceanic model also computes the formation of oceanic ice. Sea ice forms when the ocean temperature falls below –1.8°C and melts when its temperature rises above freezing. The changes in ice extent and thickness are computed based on energy conservation, keeping the ocean temperature at –1.8°C as long as ice is present. A layer of snow can be present above the ice. The surface albedo is then that of snow, or for bare ice:
A = A$$^\rm{max}_\rm{ice}$$ – (A$$^\rm{max}_\rm{ice}$$ – A$$^\rm{min}_\rm{ice}$$ ) exp(–h$$_\rm{ice}$$/h$$^0_\rm{ice}$$)
with A the albedo, A$$^\rm{max}_\rm{ice}$$ = 0.65 the maximal albedo, A$$^\rm{min}_\rm{ice}$$ =0.2 the minimal albedo, hice the ice thickness (in m) and h$$^0_\rm{ice}$$ = 0.5 m. The albedo over the ice-free ocean is taken to be equal to 0.07. The value for the maximal sea ice albedo we used (i.e., 0.65) is classical for GCMs.

== Technical aspects ==
The slab ocean model is activated in callphys.def with:
ok_slab_ocean = .true.

The sea ice model is activated in callphys.def with:
ok_slab_sic = .true.

The horizontal heat transport is activated in callphys.def with:
ok_slab_heat_transp = .true.
The horizontal heat transport cannot be activated in parallel at the moment.

Values of A$$^{max}_{ice}$$ and A$$^{min}_{ice}$$ are fixed in slab_ice_h.F90

Slab ocean model

2022-05-11T08:33:15Z

Bcharnay:

The slab ocean model is from Codron [2012]. This model uses the same horizontal grid as the GCM and is composed of two layers. The first layer (50 m depth) represents the surface mixed layer, where the exchanges with the atmosphere take place. The second layer (150 m depth) represents
the deep ocean. The transport of heat by the ocean circulation is given by two components. First, the impact of subgrid-scale eddies is represented by horizontal diffusion, with a uniform diffusivity in both layers. Then, the mean wind-driven circulation is computed by calculating
the Ekman mass fluxes in the surface layer from the surface wind stress and taking an opposite return flow at depth. These mass fluxes are then used to advect the ocean temperature horizontally. In the case of divergent horizontal mass fluxes, the upwelling or downwelling mass flux is obtained by continuity. This simplified model reproduces the global meridional oceanic heat transport quite closely compared to a full GCM, both for actual Earth and for a simulated global ocean case [Marshall et al., 2007].

The oceanic model also computes the formation of oceanic ice. Sea ice forms when the ocean temperature falls below –1.8°C and melts when its temperature rises above freezing. The changes in ice extent and thickness are computed based on energy conservation, keeping the ocean temperature at –1.8°C as long as ice is present. A layer of snow can be present above the ice. The surface albedo is then that of snow, or for bare ice:
A = A$$^\rm{max}_\rm{ice}$$ – (A$$^\rm{max}_\rm{ice}$$ – A$$^\rm{min}_\rm{ice}$$ ) exp(–h$$_\rm{ice}$$/h$$^0_\rm{ice}$$)
with A the albedo, A$$^\rm{max}_\rm{ice}$$ = 0.65 the maximal albedo, A$$^\rm{min}_\rm{ice}$$ =0.2 the minimal albedo, hice the ice thickness (in m) and h$$^0_\rm{ice}$$ = 0.5 m. The albedo over the ice-free ocean is taken to be equal to 0.07. The value for the maximal sea ice albedo we used (i.e., 0.65) is classical for GCMs.

== Technical aspects ==
The slab ocean model is activated in callphys.def with:
ok_slab_ocean = .true.

The sea ice model is activated in callphys.def with:
ok_slab_sic = .true.

The horizontal heat transport is activated in callphys.def with:
ok_slab_heat_transp = .true.
The horizontal heat transport cannot be activated in parallel at the moment.

Values of A$$^{max}_{ice}$$ and A$$^{min}_{ice}$$ are fixed in slab_ice_h.F90

Slab ocean model

2022-05-11T08:31:24Z

Bcharnay:

The slab ocean model is from Codron [2012]. This model uses the same horizontal grid as the GCM and is composed of two layers. The first layer (50 m depth) represents the surface mixed layer, where the exchanges with the atmosphere take place. The second layer (150 m depth) represents
the deep ocean. The transport of heat by the ocean circulation is given by two components. First, the impact of subgrid-scale eddies is represented by horizontal diffusion, with a uniform diffusivity in both layers. Then, the mean wind-driven circulation is computed by calculating
the Ekman mass fluxes in the surface layer from the surface wind stress and taking an opposite return flow at depth. These mass fluxes are then used to advect the ocean temperature horizontally. In the case of divergent horizontal mass fluxes, the upwelling or downwelling mass flux is obtained by continuity. This simplified model reproduces the global meridional oceanic heat transport quite closely compared to a full GCM, both for actual Earth and for a simulated global ocean case [Marshall et al., 2007].

The oceanic model also computes the formation of oceanic ice. Sea ice forms when the ocean temperature falls below –1.8°C and melts when its temperature rises above freezing. The changes in ice extent and thickness are computed based on energy conservation, keeping the ocean temperature at –1.8°C as long as ice is present. A layer of snow can be present above the ice. The surface albedo is then that of snow, or for bare ice:
A = A$$^\rm{max}_\rm{ice}$$ – (A$$^\rm{max}_\rm{ice}$$ – A$$^\rm{min}_\rm{ice}$$ ) exp(–h$$_\rm{ice}$$/h$$^0_\rm{ice}$$)
with A the albedo, A$$^\rm{max}_\rm{ice}$$ = 0.65 the maximal albedo, A$$^\rm{min}_\rm{ice}$$ =0.2 the minimal albedo, hice the ice thickness (in m) and h$$^0_\rm{ice}$$ = 0.5 m. The albedo over the ice-free ocean is taken to be equal to 0.07. The value for the maximal sea ice albedo we used (i.e., 0.65) is classical for GCMs.

== Technical aspects ==
The slab ocean model is activated in callphys.def with:

ok_slab_ocean = .true.

The sea ice model is activated in callphys.def with:
ok_slab_sic = .true.

The horizontal heat transport is activated in callphys.def with:
ok_slab_heat_transp = .true.
The horizontal heat transport cannot be activated in parallel at the moment.

Values of A$$^{max}_{ice}$$ and A$$^{min}_{ice}$$ are fixed in slab_ice_h.F90

Slab ocean model

2022-05-11T08:26:44Z

Bcharnay:

The slab ocean model is from Codron [2012]. This model uses the same horizontal grid as the GCM and is composed of two layers. The first layer (50 m depth) represents the surface mixed layer, where the exchanges with the atmosphere take place. The second layer (150 m depth) represents
the deep ocean. The transport of heat by the ocean circulation is given by two components. First, the impact of subgrid-scale eddies is represented by horizontal diffusion, with a uniform diffusivity in both layers. Then, the mean wind-driven circulation is computed by calculating
the Ekman mass fluxes in the surface layer from the surface wind stress and taking an opposite return flow at depth. These mass fluxes are then used to advect the ocean temperature horizontally. In the case of divergent horizontal mass fluxes, the upwelling or downwelling mass flux is obtained by continuity. This simplified model reproduces the global meridional oceanic heat transport quite closely compared to a full GCM, both for actual Earth and for a simulated global ocean case [Marshall et al., 2007].

The oceanic model also computes the formation of oceanic ice. Sea ice forms when the ocean temperature falls below –1.8°C and melts when its temperature rises above freezing. The changes in ice extent and thickness are computed based on energy conservation, keeping the ocean temperature at –1.8°C as long as ice is present. A layer of snow can be present above the ice. The surface albedo is then that of snow, or for bare ice:
A = A$$^{max}_{ice}$$ – (A$$^{max}_{ice}$$ – A$$^{min}_{ice}$$ ) exp(–h$$_{ice}$$/h$$^0_{ice}$$)
with A the albedo, A$$^{max}_{ice}$$ = 0.65 the maximal albedo, A$$^{min}_{ice}$$ =0.2 the minimal albedo, hice the ice thickness (in m) and h$$^0_{ice}$$ = 0.5 m. The albedo over the ice-free ocean is taken to be equal to 0.07. The value for the maximal sea ice albedo we used (i.e., 0.65) is classical for GCMs.

== Technical aspects ==
The slab ocean model is activated in callphys.def with:

ok_slab_ocean = .true.

The sea ice model is activated in callphys.def with:
ok_slab_sic = .true.

The horizontal heat transport is activated in callphys.def with:
ok_slab_heat_transp = .true.
The horizontal heat transport cannot be activated in parallel at the moment.

Values of A$$^{max}_{ice}$$ and A$$^{min}_{ice}$$ are fixed in slab_ice_h.F90

Slab ocean model

2022-05-11T08:18:28Z

Bcharnay:

The slab ocean model is from Codron [2012]. This model uses the same horizontal grid as the GCM and is composed of two layers. The first layer (50 m depth) represents the surface mixed layer, where the exchanges with the atmosphere take place. The second layer (150 m depth) represents
the deep ocean. The transport of heat by the ocean circulation is given by two components. First, the impact of subgrid-scale eddies is represented by horizontal diffusion, with a uniform diffusivity in both layers. Then, the mean wind-driven circulation is computed by calculating
the Ekman mass fluxes in the surface layer from the surface wind stress and taking an opposite return flow at depth. These mass fluxes are then used to advect the ocean temperature horizontally. In the case of divergent horizontal mass fluxes, the upwelling or downwelling mass flux is obtained by continuity. This simplified model reproduces the global meridional oceanic heat transport quite closely compared to a full GCM, both for actual Earth and for a simulated global ocean case [Marshall et al., 2007].

The oceanic model also computes the formation of oceanic ice. Sea ice forms when the ocean temperature falls below –1.8°C and melts when its temperature rises above freezing. The changes in ice extent and thickness are computed based on energy conservation, keeping the ocean temperature at –1.8°C as long as ice is present. A layer of snow can be present above the ice. The surface albedo is then that of snow, or for bare ice:
A = A$$^{max}_{ice}$$ – (A$$^{max}_{ice}$$ – A$$^{min}_{ice}$$ ) exp(–h$$_{ice}$$/h$$^0_{ice}$$)
with A the albedo, A$$^{max}_{ice}$$ = 0.65 the maximal albedo, A$$^{min}_{ice}$$ =0.2 the minimal albedo, hice the ice thickness (in m) and h$$^0_{ice}$$ = 0.5 m. The albedo over the ice-free ocean is taken to be equal to 0.07. The value for the maximal sea ice albedo we used (i.e., 0.65) is classical for GCMs.

== Technical aspects ==
The slab ocean model is activated in callphys.def with:
ok_slab_ocean = .true.
# sea-ice
ok_slab_sic = .false.
# heat transport
ok_slab_heat_transp = .false. ....

Values of A$$^{max}_{ice}$$ and A$$^{min}_{ice}$$ are fixed in slab_ice_h.F90

Slab ocean model

2022-05-11T08:16:21Z

Bcharnay:

The slab ocean model is from Codron [2012]. This model uses the same horizontal grid as the GCM and is composed of two layers. The first layer (50 m depth) represents the surface mixed layer, where the exchanges with the atmosphere take place. The second layer (150 m depth) represents
the deep ocean. The transport of heat by the ocean circulation is given by two components. First, the impact of subgrid-scale eddies is represented by horizontal diffusion, with a uniform diffusivity in both layers. Then, the mean wind-driven circulation is computed by calculating
the Ekman mass fluxes in the surface layer from the surface wind stress and taking an opposite return flow at depth. These mass fluxes are then used to advect the ocean temperature horizontally. In the case of divergent horizontal mass fluxes, the upwelling or downwelling mass flux is obtained by continuity. This simplified model reproduces the global meridional oceanic heat transport quite closely compared to a full GCM, both for actual Earth and for a simulated global ocean case [Marshall et al., 2007].

The oceanic model also computes the formation of oceanic ice. Sea ice forms when the ocean temperature falls below –1.8°C and melts when its temperature rises above freezing. The changes in ice extent and thickness are computed based on energy conservation, keeping the ocean temperature at –1.8°C as long as ice is present. A layer of snow can be present above the ice. The surface albedo is then that of snow, or for bare ice:
A = A$$^{max}_{ice}$$ – (A$$^{max}_{ice}$$ – A$$^{min}_{ice}$$ ) exp(–h$$_{ice}$$/h$$^0_{ice}$$)
with A the albedo, A$$^{max}_{ice}$$ = 0.65 the maximal albedo, A$$^{min}_{ice}$$ =0.2 the minimal albedo, hice the ice thickness (in m) and h$$^0_{ice}$$ = 0.5 m. The albedo over the ice-free ocean is taken to be equal to 0.07. The value for the maximal sea ice albedo we used (i.e., 0.65) is classical for GCMs.

== Technical aspects ==
In the code the slab ocean model is read by ....
Values of A$$^{max}_{ice}$$ and A$$^{min}_{ice}$$ are fixed in slab_ice_h.F90

Slab ocean model

2022-05-11T08:10:54Z

Bcharnay:

The slab ocean model is from Codron [2012]. This model uses the same horizontal grid as the GCM and is composed of two layers. The first layer (50 m depth) represents the surface mixed layer, where the exchanges with the atmosphere take place. The second layer (150 m depth) represents
the deep ocean. The transport of heat by the ocean circulation is given by two components. First, the impact of subgrid-scale eddies is represented by horizontal diffusion, with a uniform diffusivity in both layers. Then, the mean wind-driven circulation is computed by calculating
the Ekman mass fluxes in the surface layer from the surface wind stress and taking an opposite return flow at depth. These mass fluxes are then used to advect the ocean temperature horizontally. In the case of divergent horizontal mass fluxes, the upwelling or downwelling mass flux is obtained by continuity. This simplified model reproduces the global meridional oceanic heat transport quite closely compared to a full GCM, both for actual Earth and for a simulated global ocean case [Marshall et al., 2007].

The oceanic model also computes the formation of oceanic ice. Sea ice forms when the ocean temperature falls below –1.8°C and melts when its temperature rises above freezing. The changes in ice extent and thickness are computed based on energy conservation, keeping the ocean temperature at –1.8°C as long as ice is present. A layer of snow can be present above the ice. The surface albedo is then that of snow, or for bare ice:
A = A$^max$ice – (Amaxice – Aminice ) exp(–hice/h0ice)
with A the albedo, Amaxice = 0.65 the maximal albedo, Aminice =0.2 the minimal albedo, hice the ice thickness (in m) and h0ice = 0.5 m. The albedo over the ice-free ocean is taken to be equal to 0.07. The value for the maximal sea ice albedo we used (i.e., 0.65) is classical for GCMs.

== Technical aspects ==
In the code the slab ocean model is read by ....

Slab ocean model

2022-05-11T08:09:20Z

Bcharnay:

The slab ocean model is from Codron [2012]. This model uses the same horizontal grid as the GCM and is composed of two layers. The first layer (50 m depth) represents the surface mixed layer, where the exchanges with the atmosphere take place. The second layer (150 m depth) represents
the deep ocean. The transport of heat by the ocean circulation is given by two components. First, the impact of subgrid-scale eddies is represented by horizontal diffusion, with a uniform diffusivity in both layers. Then, the mean wind-driven circulation is computed by calculating
the Ekman mass fluxes in the surface layer from the surface wind stress and taking an opposite return flow at depth. These mass fluxes are then used to advect the ocean temperature horizontally. In the case of divergent horizontal mass fluxes, the upwelling or downwelling mass flux is obtained by continuity. This simplified model reproduces the global meridional oceanic heat transport quite closely compared to a full GCM, both for actual Earth and for a simulated global ocean case [Marshall et al., 2007].

The oceanic model also computes the formation of oceanic ice. Sea ice forms when the ocean temperature falls below –1.8°C and melts when its temperature rises above freezing. The changes in ice extent and thickness are computed based on energy conservation, keeping the ocean temperature at –1.8°C as long as ice is present. A layer of snow can be present above the ice. The surface albedo is then that of snow, or for bare ice:
A = Amaxice – (Amaxice – Aminice ) exp(–hice/h0ice)
with A the albedo, Amaxice = 0.65 the maximal albedo, Aminice =0.2 the minimal albedo, hice the ice thickness (in m) and h0ice = 0.5 m. The albedo over the ice-free ocean is taken to be equal to 0.07. The value for the maximal sea ice albedo we used (i.e., 0.65) is classical for GCMs.

== Technical aspects ==
In the code the slab ocean model is read by ....

Slab ocean model

2022-05-11T08:04:36Z

Bcharnay: Created page with "The slab ocean model is from Codron [2012]. This model uses the same horizontal grid as the GCM and is composed of two layers. The first layer (50 m depth) represents the surf..."

The slab ocean model is from Codron [2012]. This model uses the same horizontal grid as the GCM and is composed of two layers. The first layer (50 m depth) represents the surface mixed layer, where the exchanges with the atmosphere take place. The second layer (150 m depth) represents
the deep ocean. The transport of heat by the ocean circulation is given by two components. First, the impact of subgrid-scale eddies is represented by horizontal diffusion, with a uniform diffusivity in both layers. Then, the mean wind-driven circulation is computed by calculating
the Ekman mass fluxes in the surface layer from the surface wind stress and taking an opposite return flow at depth.
These mass fluxes are then used to advect the ocean temperature horizontally. In the case of divergent horizontal mass
fluxes, the upwelling or downwelling mass flux is obtained by continuity. Other components of the ocean circulation—
density-driven circulations and horizontal gyres—are not present in the model. Although they can play an important
role regionally on the present Earth, they are weaker on global average, and gyres would be absent in the case of a
global ocean. This simplified model reproduces the global meridional oceanic heat transport quite closely compared to
a full GCM, both for actual Earth and for a simulated global ocean case [Marshall et al., 2007].
[37] The oceanic model also computes the formation of oceanic ice. Sea ice forms when the ocean temperature
falls below –1.8ıC and melts when its temperature rises above freezing. The changes in ice extent and thickness are
computed based on energy conservation, keeping the ocean temperature at –1.8ıC as long as ice is present. A layer of
snow can be present above the ice. The surface albedo is then that of snow, or for bare ice:
A = Amax
ice – (Amax
ice – Amin
ice ) exp(–hice/h0
ice) (11)
with A the albedo, Amax
ice = 0.65 the maximal albedo, Amin
ice =
0.2 the minimal albedo, hice the ice thickness (in m) and
h0ice = 0.5 m. The albedo over the ice-free ocean is taken to
be equal to 0.07. The value for the maximal sea ice albedo
we used (i.e., 0.65) is classical for GCMs. It is a pretty high
value for studies of snowball Earth [Abbot et al., 2011],
making our results concerning cold climates pretty robust.
[38] The transport of sea ice is not taken into account. This
has a small impact for the present-day conditions, but it may
be more important for different conditions (e.g., a colder
climate with more sea ice) [Lewis et al., 2003].

== Technical aspects ==
In the code the slab ocean model is read by ....