From bcb551e67061ef1183c49e6b7bc7b6fd73c3c5eb Mon Sep 17 00:00:00 2001
From: Pierre Mathiot <pierre.mathiot@univ-grenoble-alpes.fr>
Date: Wed, 18 Dec 2024 14:44:49 +0000
Subject: [PATCH] Resolve "Modification across chapters for ISF/ICB"
---
latex/NEMO/main/chapters.tex | 2 +-
latex/NEMO/subfiles/chap_D2D.tex | 12 +++++-------
latex/NEMO/subfiles/chap_DOM.tex | 11 ++++++-----
latex/NEMO/subfiles/chap_DYN.tex | 21 +++------------------
latex/NEMO/subfiles/chap_LIO.tex | 15 ++++++++-------
latex/NEMO/subfiles/chap_SBC.tex | 29 +++++++++++++++--------------
latex/NEMO/subfiles/chap_TRA.tex | 18 +++++++++---------
7 files changed, 47 insertions(+), 61 deletions(-)
diff --git a/latex/NEMO/main/chapters.tex b/latex/NEMO/main/chapters.tex
index 48bdb75..d56b30d 100644
--- a/latex/NEMO/main/chapters.tex
+++ b/latex/NEMO/main/chapters.tex
@@ -5,9 +5,9 @@
\subfile{../subfiles/chap_model_basics} %% Continuous equations and assumptions
\subfile{../subfiles/chap_time_domain} %% Time discretisation (time stepping strategy)
\subfile{../subfiles/chap_DOM} %% Space discretisation
-\subfile{../subfiles/chap_TRA} %% Tracer advection/diffusion equation
\subfile{../subfiles/chap_D2D} %% Dynamics : 2D Barotropic equations
\subfile{../subfiles/chap_DYN} %% Dynamics : momentum equation
+\subfile{../subfiles/chap_TRA} %% Tracer advection/diffusion equation
\subfile{../subfiles/chap_SBC} %% Surface Boundary Conditions
\subfile{../subfiles/chap_LIO} %% Land Ice interaction chapter
\subfile{../subfiles/chap_LBC} %% Lateral Boundary Conditions
diff --git a/latex/NEMO/subfiles/chap_D2D.tex b/latex/NEMO/subfiles/chap_D2D.tex
index 10061bf..8438dda 100644
--- a/latex/NEMO/subfiles/chap_D2D.tex
+++ b/latex/NEMO/subfiles/chap_D2D.tex
@@ -243,19 +243,17 @@ the following options:
(1) When \np[=.true.]{ln_rnf}{ln\_rnf} (see \autoref{sec:SBC_rnf}),
river runoff is taken into account when computing the net freshwater flux.
-(2) When \np[=.true.]{ln_isf}{ln\_isf} (see \autoref{sec:SBC_isf}), explicit or
+(2) When \np[=.true.]{ln_isf}{ln\_isf} (see \autoref{sec:LIO_isf}), explicit or
parameterised contributions from ice-shelf cavities are taken into account when computing
-the net freshwater flux.
+the net freshwater flux. Furthermore, if \np[=.true.]{ln_isfcpl_cons}{ln\_isfcpl\_cons},
+the corrective increment flux applied to ensure the mass conservation when NEMO is coupled
+to an ice sheet model is also taken into account (see \autoref{subsec:ISF_iscpl} for details).
(3) When \np[=.true.]{ln_sdw}{ln\_sdw} (see \autoref{subsec:SBC_wave_sdw}), the contribution from
divergence due to Stoke's drift is taken into account when computing the net freshwater
flux.
-(4) When \np[=.true.]{ln_isf .AND. ln_isfcpl}{ln\_isf .AND. ln\_isfcpl} (see
-\autoref{sec:SBC_isf}), the contribution from coupled ice-sheets is taken into account when
-computing the net freshwater flux.
-
-(5) When \np[=.true.]{lk_asminc .AND. ln_sshinc .AND. ln_asmiau}{lk\_asminc .AND.
+(4) When \np[=.true.]{lk_asminc .AND. ln_sshinc .AND. ln_asmiau}{lk\_asminc .AND.
ln\_sshinc .AND. ln\_asmiau} (see \autoref{sec:ASM_IAU}), the contribution from IAU
weighted ssh increments is taken into account when computing the net freshwater flux.
diff --git a/latex/NEMO/subfiles/chap_DOM.tex b/latex/NEMO/subfiles/chap_DOM.tex
index 90ef47c..97ba989 100644
--- a/latex/NEMO/subfiles/chap_DOM.tex
+++ b/latex/NEMO/subfiles/chap_DOM.tex
@@ -476,7 +476,7 @@ Where $r3t(i,j,t) = \frac{\eta(i,j,t)}{\mathrm{ht\_0}(i,j)}$,
the ratio of sea surface height to reference water column height,
is updated at every time step by \rou{domqco\_r3c} and where
\forcode{e3t_0}, \forcode{ht_0} and \forcode{tmask} are the $T$-point variants of the reference vertical scale
-factor, the reference water height, and the land-sea mask, respectively.
+factor, the reference water column height, and the land-sea mask, respectively.
Similar expressions are applied to the scale factors at $u$/$v$/$f$-points using appropriate interpolation of $\eta$.
In the expressions for the scale factors at $w$-levels, grid point depths and water heights,
the ratio is instead unmasked.
@@ -580,7 +580,7 @@ $s-z$ or $s-zps$ coordinates (\autoref{fig:DOM_z_zps_s_sps}d and \autoref{fig:DO
\label{subsec:DOM_zps}
In $zps$-coordinates reference levels are based on the same spatially uniform levels as in $z$-coordinates.
-At the bottom (and at the surface) a partial cell volume varies in order to to take into account
+At the bottom (and at the top) a partial cell volume varies in order to to take into account
solid boundaries \ie\ the bathymetry (and the ice-shelf cavities) more accurately.
In \NEMO\ v4.2 and previous versions, partial cells were vertically shrunk, causing the mass center and the $T$-point location to shift,
@@ -594,6 +594,7 @@ Unlike in the previous approach, the height of the $T$-points remains unchanged.
This representation is described in \citep{kevlahan_GMD15}, it is
based on Brinkman penalization where a control parameter \ie\ the porosity modifies fluxes though penalized lateral surfaces.
This parameter is encapsulated within vertical scale factors ($e3t^0$, $e3u^0$, $e3v^0$) as illustrated in \autoref{fig:DOM_partial_step_scheme}.
+In case of ocean cavities, partial cells are also applied at the top interface using the same method as for the bottom interface but upside-down.
\begin{figure}
\centering
@@ -612,7 +613,7 @@ This parameter is encapsulated within vertical scale factors ($e3t^0$, $e3u^0$,
The \forcode{bottom_level} and \forcode{top_level} variables define
the bottom and top wet levels in each grid column.
-The values of \forcode{top_level} depend on whether ice shelf cavities are used (\autoref{subsec:DOM_zgr_space}):
+The values of \forcode{top_level} depend on whether ice shelf cavities are used (\autoref{subsec:ISF_dom}):
without ice cavities, \forcode{top_level} is essentially a land mask (0 on land; 1 everywhere else);
with ice cavities, in locations below an overlying ice shelf \forcode{top_level} determines the topmost wet point instead.
@@ -639,8 +640,8 @@ Based on variables \forcode{top_level} and \forcode{bottom_level}, the mask vari
Note that, without ice shelves cavities,
masks at $T$- and $w$-points are identical with the numerical indexing used
(see \autoref{subsec:DOM_Num_Index}).
-Nevertheless,
-$wmask$ are required with ocean cavities to deal with the top boundary (ice shelf/ocean interface)
+Nevertheless, with ocean cavities,
+$wmask$ are required to deal with the top boundary (ice shelf/ocean interface)
in exactly the same way as for the bottom boundary.
%% The specification of closed lateral boundaries requires that at least
diff --git a/latex/NEMO/subfiles/chap_DYN.tex b/latex/NEMO/subfiles/chap_DYN.tex
index b060ef5..ed32911 100644
--- a/latex/NEMO/subfiles/chap_DYN.tex
+++ b/latex/NEMO/subfiles/chap_DYN.tex
@@ -662,7 +662,9 @@ with the non-linear free surface (\np[=.false.]{ln_linssh}{ln\_linssh} and \key{
\item
\textbf{Traditional coding with adaptation for ice shelf cavities} (\np[=.true.]{ln_hpg_isf}{ln\_hpg\_isf}):
-this scheme must be used when ice shelf cavities are activated (\np[=.true.]{ln_isfcav}{ln\_isfcav} and the inclusion of \key{isf}).
+In the presence of ice shelves, the traditional coding has been adapted to accommodate the load provided by the ice shelves.
+This scheme must be used when ice shelf cavities are activated (\np[=.true.]{ln_isfcav}{ln\_isfcav} and the inclusion of \key{isf}.
+All the details on the modification are provided in \autoref{subsec:ISF_hpg}.
\item
\textbf{Pressure Jacobian scheme} (\np[=.true.]{ln_hpg_prj}{ln\_hpg\_prj}):
@@ -696,23 +698,6 @@ The true in situ density $\rho= \rho_0 (1 + r_0(z) + rhd )$ where $r_0(z)$ accou
with depth for water with a potential temperature of $4^{\circ}$C and salinity of $35.16504$g/kg
(see (13) and (14) of \citet{roquet.madec.ea_OM15}).
-%% =================================================================================================
-\subsection{Ice shelf cavity}
-\label{subsec:DYN_hpg_isf}
-
-Beneath an ice shelf, the total pressure gradient is the sum of the pressure gradient due to the ice shelf load and
-the pressure gradient due to the ocean load (\np[=.true.]{ln_hpg_isf}{ln\_hpg\_isf} with the inclusion of \key{isf}).\\
-
-The main hypothesis to compute the ice shelf load is that the ice shelf is in an isostatic equilibrium.
-The top pressure is computed integrating from surface to the base of the ice shelf a reference density profile
-(prescribed as density of a water at 34.4 PSU and -1.9\deg{C}) and
-corresponds to the water replaced by the ice shelf.
-This top pressure is constant over time.
-A detailed description of this method is described in \citet{losch_JGR08}.\\
-
-The pressure gradient due to ocean load is computed using the expression \autoref{eq:DYN_hpg_sco} described in
-\autoref{subsec:DYN_hpg_sco}.
-
%% =================================================================================================
%% \subsection[Time-scheme (\forcode{ln_dynhpg_imp})]{Time-scheme (\protect\np{ln_dynhpg_imp}{ln\_dynhpg\_imp})}
%% \label{subsec:DYN_hpg_imp}
diff --git a/latex/NEMO/subfiles/chap_LIO.tex b/latex/NEMO/subfiles/chap_LIO.tex
index 59c612a..989d96e 100644
--- a/latex/NEMO/subfiles/chap_LIO.tex
+++ b/latex/NEMO/subfiles/chap_LIO.tex
@@ -188,13 +188,13 @@ The outcomes of the ISF module are the fresh water flux and the associated heat
This formulation has not been extensively tested in NEMO (and is thus not recommended).
\end{description}
- In the formulation presented above, the transfert coeficient $\Gamma^{T}$ and $\Gamma^{S}$ are respectively defined by \np{rn_gammat0}{rn\_gammat0} and \np{rn_gammas0}{rn\_gammas0}. The definition of the exchange velocities $\gamma^{T,S}$ is done in the \mdl{isfcavgam} module.
+ In the formulation presented above, the transfert coeficient $\Gamma^{T}$ and $\Gamma^{S}$ are respectively defined by \np{rn_gammat0}{rn\_gammat0} and \np{rn_gammas0}{rn\_gammas0}. The definition of the exchange velocities $\gamma^{T,S}$ is done in the \mdl{isfcavgam} module.\\
The ice shelf fresh water fluxes are implemented as a volume flux, same as for the runoff.
-The fwf addition due to the ice shelf melting is, at each relevant depth level, added to
-the horizontal divergence (\textit{hdivn}) in the subroutine \rou{isf\_hdiv}, called from \mdl{divhor}.
+The fresh water flux addition due to the ice shelf melting is distributed uniformly over the top boundary layer and added to
+the horizontal divergence (\textit{hdivn}) at each relevant depth level in the subroutine \rou{isf\_hdiv}, called from \mdl{divhor}.
+As for the volume flux, the associated heat fluxes (latent heat and heat content) are distributed uniformly vertically over the top boundary layer in \mdl{traisf}.
See the runoff section \autoref{sec:SBC_rnf} for all the details about the divergence correction.\\
-
\subsection[Ocean/Ice shelf fluxes in parametrised cavities (\textit{isfpar.F90})]{Ocean/Ice shelf fluxes in parametrised cavities (\protect\mdl{isfpar})}
For a low resolution model, many ice shelves are too small to be explicitly represented.
@@ -215,7 +215,7 @@ See the runoff section \autoref{sec:SBC_rnf} for all the details about the diver
\item[\np{cn_isfpar_mlt}{cn\_isfpar\_mlt}\forcode{ = 'spe'}]:
The fwf ($q$) is read from \np{sn_isfpar_fwf}{sn\_isfpar\_fwf} and distributed along the ice shelf front between
the average grounding line (GL) depth (\np{sn_isfpar_zmax}{sn\_isfpar\_zmax}) and
- the depth of the base of the ice shelf at the front edge (\np{sn_isfpar_zmin}{sn\_isfpar\_min}). Convention of the input file is positive toward the ocean (i.e. positive for melting and negative for freezing).
+ the depth of the base of the ice shelf at the front edge (\np{sn_isfpar_zmin}{sn\_isfpar\_zmin}). Convention of the input file is positive toward the ocean (i.e. positive for melting and negative for freezing).
The heat flux ($Q_h$) is computed as $Q_h = q \times L_f$.
\item[\np{cn_isfpar_mlt}{cn\_isfpar\_mlt}\forcode{ = 'oasis'}]:
@@ -224,7 +224,8 @@ See the runoff section \autoref{sec:SBC_rnf} for all the details about the diver
\end{description}
-As for the open cavity case, the ice shelf fresh water fluxes are implemented as a volume flux.\\
+As for the open cavity case, the ice shelf fresh water fluxes are implemented as a volume flux.
+In this case the volume and heat fluxes are uniformly distributed between \np{sn_isfpar_zmin}{sn\_isfpar\_zmin} and \np{sn_isfpar_zmax}{sn\_isfpar\_zmax}.\\
To conclude these two sections on ice shelf melt, it is worth noting the following:
\begin{description}
@@ -339,7 +340,7 @@ The corrective increment is applied into the cells themselves (if it is a wet ce
\label{subsec:ISF_hpg}
Ice shelf impose a load on the ocean. The main hypothesis to compute the ice shelf load is that the ice shelf is in an hydrostatic equilibrium. Therefore, beneath an ice shelf, the total pressure is the sum of the pressure due to the ice shelf load and
-the pressure due to the ocean load. The ice shelf pressure is computed by integrating a reference density profile $\rho_{isf}$ from the surface to the base of the ice shelf. THe local ocean pressure can thenThis can be formulated like this:
+the pressure due to the ocean load. The ice shelf pressure is computed by integrating a reference density profile $\rho_{isf}$ from the surface to the base of the ice shelf. The local ocean pressure can thenThis can be formulated like this:
\begin{equation}
\label{eq:ISF_hpg_isf_1}
diff --git a/latex/NEMO/subfiles/chap_SBC.tex b/latex/NEMO/subfiles/chap_SBC.tex
index 4fc1a9c..3f5e9a9 100644
--- a/latex/NEMO/subfiles/chap_SBC.tex
+++ b/latex/NEMO/subfiles/chap_SBC.tex
@@ -74,6 +74,7 @@ These options control:
\item the modification of fluxes below ice-covered areas (using climatological ice-cover or a sea-ice model)
(\autoref{subsec:SBC_ice-cover}),
\item the addition of river runoffs as surface freshwater fluxes or lateral inflow (\autoref{sec:SBC_rnf}),
+\item the addition of iceberg melting as surface freshwater flux and latent heat flux (\autoref{sec:LIO_icb}),
\item the addition of a freshwater flux adjustment in order to avoid a mean sea-level drift
(\autoref{subsec:SBC_fwb}),
\item the transformation of the solar radiation (if provided as daily mean) into an analytical diurnal cycle
@@ -116,12 +117,12 @@ The way the light penetrates inside the water column is generally a sum of decre
The surface freshwater budget is provided by the \textit{emp} field.
It represents the mass flux exchanged with the atmosphere (evaporation minus precipitation) and
-possibly with the sea-ice and ice shelves (freezing minus melting of ice).
+possibly with the sea-ice and icebergs (freezing minus melting of ice).
It affects the ocean in two different ways:
$(i)$ it changes the volume of the ocean, and therefore appears in the sea surface height equation as %GS: autoref ssh equation to be added
a volume flux, and
$(ii)$ it changes the surface temperature and salinity through the heat and salt contents of
-the mass exchanged with atmosphere, sea-ice and ice shelves.
+the mass exchanged with atmosphere, sea-ice and icebergs.
%\colorbox{yellow}{Miss: }
%A extensive description of all namsbc namelist (parameter that have to be
@@ -1260,10 +1261,10 @@ The heat and salt content of the river runoff is not included in this step,
and so the tracer concentrations are diluted as water of ocean temperature and salinity is moved upward out of
the box and replaced by the same volume of river water with no corresponding heat and salt addition. \\
-For the tracers, by default (\np{ln_rnf_sal}{ln\_rnf\_sal} and
-\np{ln_rnf_tem}{ln\_rnf\_tem} set to false), the runoff is assumed to be at the river point sst and with 0 salinity (fresh).
-If set to true, the user needs to provide a runoff temperature and/or salinity field (\np{sn_t_rnf}{sn\_t\_rnf} and/or (\np{sn_s_rnf}{sn\_s\_rnf}) respectively). It is worth noting that location with a temperature value of -999 is considered as missing data and the river temperature is taken to
-be the surface temperature at the river point. Furthermore, the forcing iceberg melt flux (and associated latent heat flux) can be added as runoff by activating \np{ln_rnf_icb}{ln\_rnf\_icb} instead of using the lagrangian iceberg model (ICB, \autoref{subsec:ICB}) to simulate it.
+For the tracers, by default (\np{ln_rnf_tem}{ln\_rnf\_tem} and \np{ln_rnf_sal}{ln\_rnf\_sal}
+ set to \textit{false}), the runoff is assumed to be at the river point \textit{sst} and with salinity 0 g/kg.
+If set to true, the user needs to provide a runoff temperature and/or salinity field (\np{sn_t_rnf}{sn\_t\_rnf} and/or \np{sn_s_rnf}{sn\_s\_rnf} respectively). It is worth noting that location with a temperature value of -999 is considered as missing data and the river temperature is taken to
+be the surface temperature at the river point. Furthermore, the iceberg melt flux forcing (and the associated latent heat flux) can be added as runoff by activating \np{ln_rnf_icb}{ln\_rnf\_icb} instead of using the lagrangian iceberg model (ICB, \autoref{sec:LIO_icb}) to simulate it.
In this case, the user simply need to specify a map of iceberg melt rate in the file \np{sn_i_rnf}{sn\_i\_rnf}.
In this case, the iceberg fresh water flux is added to the runoff fluxes and the latent heat flux directly to the non solar heat fluxes.
@@ -1280,7 +1281,7 @@ As such the volume of water does not change, but the water is diluted.
For the non-linear free surface case, no flux is allowed through the surface.
Instead in the surface box (as well as water moving up from the boxes below) a volume of runoff water is added with
-the corresponding heat and salt (runoff temperature at surface temperature and 0 salinity by default) and so as happens in the lower boxes there is a dilution effect.
+the corresponding heat and salt (runoff temperature at surface temperature and salinity 0 g/kg by default) and so as happens in the lower boxes there is a dilution effect.
(The runoff addition to the top box along with the water being moved up through
boxes below means the surface box has a large increase in volume, whilst all other boxes remain the same size).
@@ -1669,11 +1670,11 @@ The presence at the sea surface of an ice covered area modifies all the fluxes t
There are several way to handle sea-ice in the system depending on
the value of the \np{nn_ice}{nn\_ice} namelist parameter found in \nam{sbc}{sbc} namelist.
\begin{description}
-\item [nn\_ice = 0] there will never be sea-ice in the computational domain.
+\item [{\np[=0]{nn_ice}{nn\_ice}}:] there will never be sea-ice in the computational domain.
This is a typical namelist value used for tropical ocean domain.
The surface fluxes are simply specified for an ice-free ocean.
No specific things is done for sea-ice.
-\item [nn\_ice = 1] sea-ice can exist in the computational domain, but no sea-ice model is used.
+\item [{\np[=1]{nn_ice}{nn\_ice}}:] sea-ice can exist in the computational domain, but no sea-ice model is used.
An observed ice covered area is read in a file.
Below this area, the SST is restored to the freezing point and
the heat fluxes are set to $-4~W/m^2$ ($-2~W/m^2$) in the northern (southern) hemisphere.
@@ -1684,7 +1685,7 @@ the value of the \np{nn_ice}{nn\_ice} namelist parameter found in \nam{sbc}{sbc}
This manner of managing sea-ice area, just by using a IF case,
is usually referred as the \textit{ice-if} model.
It can be found in the \mdl{sbcice\_if} module.
-\item [nn\_ice = 2 or more] A full sea ice model is used.
+\item [{\np[=2]{nn_ice}{nn\_ice}}:] A full sea ice model is used.
This model computes the ice-ocean fluxes,
that are combined with the air-sea fluxes using the ice fraction of each model cell to
provide the surface averaged ocean fluxes.
@@ -1728,11 +1729,11 @@ controlling the freshwater budget are proposed:
If \np{nn_fwb}{nn\_fwb} is set > 0, \nam{sbc_fwb}{sbc\_fwb} block must be filled accordingly:
\begin{description}
- \item [rn\_fwb0 :] if {\np[=2]{nn_fwb}{nn\_fwb}}, it defines the initial freshwater adjustment flux.
- \item [nn\_fwb\_voltype :] it refers to the variable considered as the global value of volume (in equivalent liquid height in m) to be conserved by the adjustment process.
- \item [nn\_fwb\_voltype :] if set to 1, the total ocean+equivalent liquid sea ice volume water budget is controled, or if set to 0, only the ocean volume is controled.
+ \item [{\np{rn_fwb0}{rn\_fwb0}}:] if {\np[=2]{nn_fwb}{nn\_fwb}}, it defines the initial freshwater adjustment flux.
+ \item [{\np{nn_fwb_voltype}{nn\_fwb\_voltype}} :] it refers to the variable considered as the global value of volume (in equivalent liquid height in m) to be conserved by the adjustment process.
+ \item [{\np{nn_fwb_voltype}{nn\_fwb\_voltype}} :] if set to 1, the total ocean+equivalent liquid sea ice volume water budget is controled, or if set to 0, only the ocean volume is controled.
The former is now the default and recommended, being obviously more accurate on a physical point of view.
- \item [ln\_hvolg\_var :] if set to .true., an analytical variation of the global liquid height can be specified by the user.
+ \item [{\np{ln_hvolg_var}{ln\_hvolg\_var}} :] if set to .true., an analytical variation of the global liquid height can be specified by the user.
It is defined as the sum of an annual harmonic signal (with a peak to peak amplitude \np{rn_hvolg_amp}{rn\_hvolg\_amp} in m,
and a zero crossing at the beginning of month \np{nn_hvolg_mth}{nn\_hvolg\_mth}) and a linear trend given by \np{rn_hvolg_trd}{rn\_hvolg\_trd} (in m/s).
\end{description}
diff --git a/latex/NEMO/subfiles/chap_TRA.tex b/latex/NEMO/subfiles/chap_TRA.tex
index 01fcc9c..dfdb2f6 100644
--- a/latex/NEMO/subfiles/chap_TRA.tex
+++ b/latex/NEMO/subfiles/chap_TRA.tex
@@ -37,7 +37,7 @@ The two active tracers are potential temperature and salinity.
Their prognostic equations can be summarized as follows:
\[
\text{NXT} = \text{ADV} + \text{LDF} + \text{ZDF} + \text{SBC}
- + \{\text{QSR}, \text{BBC}, \text{BBL}, \text{DMP}\}
+ + \{\text{QSR}, \text{BBC}, \text{BBL}, \text{DMP}, \text{ISF}\}
\]
NXT stands for next, referring to the time-stepping.
@@ -45,13 +45,13 @@ From left to right, the terms on the rhs of the tracer equations are the advecti
the lateral diffusion (LDF), the vertical diffusion (ZDF),
the contributions from the external forcings (SBC: Surface Boundary Condition,
QSR: penetrative Solar Radiation, and BBC: Bottom Boundary Condition),
-the contribution from the bottom boundary Layer (BBL) parametrisation,
-and an internal damping (DMP) term.
-The terms QSR, BBC, BBL and DMP are optional.
+the contribution from the bottom boundary Layer (BBL) parametrisation, an internal damping (DMP) and
+the contribution from the floating ice shelves (ISF) term.
+The terms QSR, BBC, BBL, DMP and ISF are optional.
The external forcings and parameterisations require complex inputs and complex calculations
(\eg\ bulk formulae, estimation of mixing coefficients) that are carried out in the SBC,
-LDF and ZDF modules and described in \autoref{chap:SBC}, \autoref{chap:LDF} and
-\autoref{chap:ZDF}, respectively.
+LDF, ZDF and ISF modules and described in \autoref{chap:SBC}, \autoref{chap:LDF},
+\autoref{chap:ZDF} and \autoref{chap:LIO}, respectively.
Note that \mdl{tranpc}, the non-penetrative convection module,
is located in the \path{./src/OCE/TRA} directory because it directly modifies the tracer fields.
However, it is described alongside the model's vertical physics (ZDF), together with other available
@@ -735,7 +735,7 @@ Because the vertical mixing is always solved implicitly, the update of the trace
\label{sec:TRA_sbc_qsr_bbc}
Changes in the heat and salt content of the ocean's surface layer result from
-water mass exchanges between the ocean and the atmosphere, land surfaces,
+water mass exchanges between the ocean and the atmosphere, land surfaces, icebergs
or sea ice (\mdl{trasbc}).
Runoff related fluxes are distributed vertically.
The assimilation module integrates the ocean model with observational data.
@@ -782,7 +782,7 @@ The surface module (\mdl{sbcmod}, see \autoref{chap:SBC}) provides the following
\item [\textit{sfx}] The salt flux resulting from ice-ocean mass exchange
(freezing, melting, ridging...)
\item [\textit{emp}] The mass flux exchanged with the atmosphere (evaporation minus precipitation) and
- possibly with the sea-ice and ice-shelves.
+ possibly with the sea-ice and icebergs.
\item [\textit{rnf}] The mass flux associated with runoff
(see \autoref{sec:SBC_rnf} for further detail of how it acts on temperature and salinity tendencies)
\end{labeling}
@@ -793,7 +793,7 @@ The surface module (\mdl{sbcmod}, see \autoref{chap:SBC}) provides the following
estimating advection, Coriolis, and pressure gradient terms.
The absence of vertical diffusion terms during these initial integrations justifies
the exclusion of salt and heat forcing. Indeed, it saves two calls of \rou{traqsr}
-which is computationnally expensive.
+which is computationally expensive.
However, for compatibility with the continuity equation, it is necessary to account
for mass flux forcing (\textit{emp}) at the surface.
This change of mass at the first level should not impact the salt and temperature,
--
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