Changeset 12928 for NEMO/branches/2019/dev_r11078_OSMOSIS_IMMERSE_Nurser/doc/latex/NEMO/subfiles/chap_SBC.tex

Timestamp:

2020-05-14T21:46:00+02:00 (4 years ago)

Author:

smueller

Message:

Synchronizing with ^{/NEMO/trunk@12925 (ticket #2170)}

Location:

NEMO/branches/2019/dev_r11078_OSMOSIS_IMMERSE_Nurser

Files:

• . (modified) (1 prop)
• doc/latex/NEMO/subfiles/chap_SBC.tex (modified) (14 diffs)

NEMO/branches/2019/dev_r11078_OSMOSIS_IMMERSE_Nurser

@@ -6 +6 @@
 ^/vendors/FCM@HEAD            ext/FCM
 ^/vendors/IOIPSL@HEAD         ext/IOIPSL
+
+# SETTE
+^/utils/CI/sette@HEAD         sette

@@ -6 +6 @@
 ^/vendors/FCM@HEAD            ext/FCM
 ^/vendors/IOIPSL@HEAD         ext/IOIPSL
+
+# SETTE
+^/utils/CI/sette@HEAD         sette

NEMO/branches/2019/dev_r11078_OSMOSIS_IMMERSE_Nurser/doc/latex/NEMO/subfiles/chap_SBC.tex

@@ -1 +1 @@
 \documentclass[../main/NEMO_manual]{subfiles}
+\usepackage{fontspec}
+\usepackage{fontawesome}
 
 \begin{document}
@@ -45 +47 @@
 
 \begin{itemize}
-\item a bulk formulation (\np[=.true.]{ln_blk}{ln\_blk} with four possible bulk algorithms),
+\item a bulk formulation (\np[=.true.]{ln_blk}{ln\_blk}), featuring a selection of four bulk parameterization algorithms,
 \item a flux formulation (\np[=.true.]{ln_flx}{ln\_flx}),
 \item a coupled or mixed forced/coupled formulation (exchanges with a atmospheric model via the OASIS coupler),
@@ -504 +506 @@
 \label{sec:SBC_flx}
 
+% Laurent: DO NOT mix up ``bulk formulae'' (the classic equation) and the ``bulk
+% parameterization'' (i.e NCAR, COARE, ECMWF...)
+
 \begin{listing}
   \nlst{namsbc_flx}
@@ -520 +525 @@
 See \autoref{subsec:SBC_ssr} for its specification.
 
-%% =================================================================================================
+
+
+
+
+
+
+%% =================================================================================================
+\pagebreak
+\newpage
 \section[Bulk formulation (\textit{sbcblk.F90})]{Bulk formulation (\protect\mdl{sbcblk})}
 \label{sec:SBC_blk}
+
+% L. Brodeau, December 2019... %
 
 \begin{listing}
@@ -530 +545 @@
 \end{listing}
 
-In the bulk formulation, the surface boundary condition fields are computed with bulk formulae using atmospheric fields
-and ocean (and sea-ice) variables averaged over \np{nn_fsbc}{nn\_fsbc} time-step.
-
-The atmospheric fields used depend on the bulk formulae used.
-In forced mode, when a sea-ice model is used, a specific bulk formulation is used.
-Therefore, different bulk formulae are used for the turbulent fluxes computation
-over the ocean and over sea-ice surface.
-For the ocean, four bulk formulations are available thanks to the \href{https://brodeau.github.io/aerobulk/}{Aerobulk} package (\citet{brodeau.barnier.ea_JPO16}):
-the NCAR (formerly named CORE), COARE 3.0, COARE 3.5 and ECMWF bulk formulae.
-The choice is made by setting to true one of the following namelist variable:
- \np{ln_NCAR}{ln\_NCAR}, \np{ln_COARE_3p0}{ln\_COARE\_3p0},  \np{ln_COARE_3p5}{ln\_COARE\_3p5} and  \np{ln_ECMWF}{ln\_ECMWF}.
-For sea-ice, three possibilities can be selected:
-a constant transfer coefficient (1.4e-3; default value), \citet{lupkes.gryanik.ea_JGR12} (\np{ln_Cd_L12}{ln\_Cd\_L12}), and \citet{lupkes.gryanik_JGR15} (\np{ln_Cd_L15}{ln\_Cd\_L15}) parameterizations
+If the bulk formulation is selected (\np[=.true.]{ln_blk}{ln\_blk}), the air-sea
+fluxes associated with surface boundary conditions are estimated by means of the
+traditional \emph{bulk formulae}. As input, bulk formulae rely on a prescribed
+near-surface atmosphere state (typically extracted from a weather reanalysis)
+and the prognostic sea (-ice) surface state averaged over \np{nn_fsbc}{nn\_fsbc}
+time-step(s).
+
+% Turbulent air-sea fluxes are computed using the sea surface properties and
+% atmospheric SSVs at height $z$ above the sea surface, with the traditional
+% aerodynamic bulk formulae:
+
+Note: all the NEMO Fortran routines involved in the present section have been
+ initially developed (and are still developed in parallel) in
+ the \href{https://brodeau.github.io/aerobulk/}{\texttt{AeroBulk}} open-source project
+\citep{brodeau.barnier.ea_JPO17}.
+
+%%% Bulk formulae are this:
+\subsection{Bulk formulae}\label{subsec:SBC_blkform}
+%
+In NEMO, the set of equations that relate each component of the surface fluxes
+to the near-surface atmosphere and sea surface states writes
+%
+\begin{subequations}\label{eq_bulk}
+  \label{eq:SBC_bulk_form}
+  \begin{eqnarray}
+    \mathbf{\tau} &=& \rho~ C_D ~ \mathbf{U}_z  ~ U_B \\
+    Q_H           &=& \rho~C_H~C_P~\big[ \theta_z - T_s \big] ~ U_B \\
+    E             &=& \rho~C_E    ~\big[    q_s   - q_z \big] ~ U_B \\
+    Q_L           &=& -L_v \, E \\
+    %
+    Q_{sr}        &=& (1 - a) Q_{sw\downarrow} \\
+    Q_{ir}        &=& \delta (Q_{lw\downarrow} -\sigma T_s^4)
+  \end{eqnarray}
+\end{subequations}
+%
+with
+   \[ \theta_z \simeq T_z+\gamma z \]
+   \[  q_s \simeq 0.98\,q_{sat}(T_s,p_a ) \]
+%
+from which, the the non-solar heat flux is \[ Q_{ns} = Q_L + Q_H + Q_{ir} \]
+%
+where $\mathbf{\tau}$ is the wind stress vector, $Q_H$ the sensible heat flux,
+$E$ the evaporation, $Q_L$ the latent heat flux, and $Q_{ir}$ the net longwave
+flux.
+%
+$Q_{sw\downarrow}$ and $Q_{lw\downarrow}$ are the surface downwelling shortwave
+and longwave radiative fluxes, respectively.
+%
+Note: a positive sign for $\mathbf{\tau}$, $Q_H$, $Q_L$, $Q_{sr}$ or $Q_{ir}$
+implies a gain of the relevant quantity for the ocean, while a positive $E$
+implies a freshwater loss for the ocean.
+%
+$\rho$ is the density of air. $C_D$, $C_H$ and $C_E$ are the bulk transfer
+coefficients for momentum, sensible heat, and moisture, respectively.
+%
+$C_P$ is the heat capacity of moist air, and $L_v$ is the latent heat of
+vaporization of water.
+%
+$\theta_z$, $T_z$ and $q_z$ are the potential temperature, absolute temperature,
+and specific humidity of air at height $z$ above the sea surface,
+respectively. $\gamma z$ is a temperature correction term which accounts for the
+adiabatic lapse rate and approximates the potential temperature at height
+$z$ \citep{josey.gulev.ea_2013}.
+%
+$\mathbf{U}_z$ is the wind speed vector at height $z$ above the sea surface
+(possibly referenced to the surface current $\mathbf{u_0}$,
+section \ref{s_res1}.\ref{ss_current}).
+%
+The bulk scalar wind speed, namely $U_B$, is the scalar wind speed,
+$|\mathbf{U}_z|$, with the potential inclusion of a gustiness contribution.
+%
+$a$ and $\delta$ are the albedo and emissivity of the sea surface, respectively.\\
+%
+%$p_a$ is the mean sea-level pressure (SLP).
+%
+$T_s$ is the sea surface temperature. $q_s$ is the saturation specific humidity
+of air at temperature $T_s$; it includes a 2\% reduction to account for the
+presence of salt in seawater \citep{sverdrup.johnson.ea_1942,kraus.businger_QJRMS96}.
+Depending on the bulk parametrization used, $T_s$ can either be the temperature
+at the air-sea interface (skin temperature, hereafter SSST) or at typically a
+few tens of centimeters below the surface (bulk sea surface temperature,
+hereafter SST).
+%
+The SSST differs from the SST due to the contributions of two effects of
+opposite sign, the \emph{cool skin} and \emph{warm layer} (hereafter CS and WL,
+respectively, see section\,\ref{subsec:SBC_skin}).
+%
+Technically, when the ECMWF or COARE* bulk parametrizations are selected
+(\np[=.true.]{ln_ECMWF}{ln\_ECMWF} or \np[=.true.]{ln_COARE*}{ln\_COARE\*}),
+$T_s$ is the SSST, as opposed to the NCAR bulk parametrization
+(\np[=.true.]{ln_NCAR}{ln\_NCAR}) for which $T_s$ is the bulk SST (\ie~temperature
+at first T-point level).
+
+For more details on all these aspects the reader is invited to refer
+to \citet{brodeau.barnier.ea_JPO17}.
+
+
+
+\subsection{Bulk parametrizations}\label{subsec:SBC_blk_ocean}
+%%%\label{subsec:SBC_param}
+
+Accuracy of the estimate of surface turbulent fluxes by means of bulk formulae
+strongly relies on that of the bulk transfer coefficients: $C_D$, $C_H$ and
+$C_E$. They are estimated with what we refer to as a \emph{bulk
+parametrization} algorithm. When relevant, these algorithms also perform the
+height adjustment of humidity and temperature to the wind reference measurement
+height (from \np{rn_zqt}{rn\_zqt} to \np{rn_zu}{rn\_zu}).
+
+
+
+For the open ocean, four bulk parametrization algorithms are available in NEMO:
+\begin{itemize}
+\item NCAR, formerly known as CORE, \citep{large.yeager_rpt04,large.yeager_CD09}
+\item COARE 3.0 \citep{fairall.bradley.ea_JC03}
+\item COARE 3.6 \citep{edson.jampana.ea_JPO13}
+\item ECMWF (IFS documentation, cy45)
+\end{itemize}
+
+
+With respect to version 3, the principal advances in version 3.6 of the COARE
+bulk parametrization are built around improvements in the representation of the
+effects of waves on
+fluxes \citep{edson.jampana.ea_JPO13,brodeau.barnier.ea_JPO17}. This includes
+improved relationships of surface roughness, and whitecap fraction on wave
+parameters. It is therefore recommended to chose version 3.6 over 3.
+
+
+
+
+\subsection{Cool-skin and warm-layer parametrizations}\label{subsec:SBC_skin}
+%\subsection[Cool-skin and warm-layer parameterizations
+%(\forcode{ln_skin_cs} \& \forcode{ln_skin_wl})]{Cool-skin and warm-layer parameterizations (\protect\np{ln_skin_cs}{ln\_skin\_cs} \& \np{ln_skin_wl}{ln\_skin\_wl})}
+%\label{subsec:SBC_skin}
+%
+As opposed to the NCAR bulk parametrization, more advanced bulk
+parametrizations such as COARE3.x and ECMWF are meant to be used with the skin
+temperature $T_s$ rather than the bulk SST (which, in NEMO is the temperature at
+the first T-point level, see section\,\ref{subsec:SBC_blkform}).
+%
+As such, the relevant cool-skin and warm-layer parametrization must be
+activated through \np[=T]{ln_skin_cs}{ln\_skin\_cs}
+and \np[=T]{ln_skin_wl}{ln\_skin\_wl} to use COARE3.x or ECMWF in a consistent
+way.
+
+\texttt{\#LB: ADD BLBLA ABOUT THE TWO CS/WL PARAMETRIZATIONS (ECMWF and COARE) !!!}
+
+For the cool-skin scheme parametrization COARE and ECMWF algorithms share the same
+basis: \citet{fairall.bradley.ea_JGR96}. With some minor updates based
+on \citet{zeng.beljaars_GRL05} for ECMWF, and \citet{fairall.ea_19} for COARE
+3.6.
+
+For the warm-layer scheme, ECMWF is based on \citet{zeng.beljaars_GRL05} with a
+recent update from \citet{takaya.bidlot.ea_JGR10} (consideration of the
+turbulence input from Langmuir circulation).
+
+Importantly, COARE warm-layer scheme \citep{fairall.ea_19} includes a prognostic
+equation for the thickness of the warm-layer, while it is considered as constant
+in the ECWMF algorithm.
+
+
+\subsection{Appropriate use of each bulk parametrization}
+
+\subsubsection{NCAR}
+
+NCAR bulk parametrizations (formerly known as CORE) is meant to be used with the
+CORE II atmospheric forcing \citep{large.yeager_CD09}. The expected sea surface
+temperature is the bulk SST. Hence the following namelist parameters must be
+set:
+%
+\begin{verbatim}
+  ...
+  ln_NCAR    = .true.
+  ...
+  rn_zqt     = 10.     ! Air temperature & humidity reference height (m)
+  rn_zu      = 10.     ! Wind vector reference height (m)
+  ...
+  ln_skin_cs = .false. ! use the cool-skin parameterization
+  ln_skin_wl = .false. ! use the warm-layer parameterization
+  ...
+  ln_humi_sph = .true. ! humidity "sn_humi" is specific humidity  [kg/kg]
+\end{verbatim}
+
+
+\subsubsection{ECMWF}
+%
+With an atmospheric forcing based on a reanalysis of the ECMWF, such as the
+Drakkar Forcing Set \citep{brodeau.barnier.ea_OM10}, we strongly recommend to
+use the ECMWF bulk parametrizations with the cool-skin and warm-layer
+parametrizations activated. In ECMWF reanalyzes, since air temperature and
+humidity are provided at the 2\,m height, and given that the humidity is
+distributed as the dew-point temperature, the namelist must be tuned as follows:
+%
+\begin{verbatim}
+  ...
+  ln_ECMWF   = .true.
+  ...     
+  rn_zqt     =  2.     ! Air temperature & humidity reference height (m)
+  rn_zu      = 10.     ! Wind vector reference height (m)
+  ...
+  ln_skin_cs = .true. ! use the cool-skin parameterization
+  ln_skin_wl = .true. ! use the warm-layer parameterization
+  ...
+  ln_humi_dpt = .true. !  humidity "sn_humi" is dew-point temperature [K]
+  ...
+\end{verbatim}
+%
+Note: when \np{ln_ECMWF}{ln\_ECMWF} is selected, the selection
+of \np{ln_skin_cs}{ln\_skin\_cs} and \np{ln_skin_wl}{ln\_skin\_wl} implicitly
+triggers the use of the ECMWF cool-skin and warm-layer parametrizations,
+respectively (found in \textit{sbcblk\_skin\_ecmwf.F90}).
+
+
+\subsubsection{COARE 3.x}
+%
+Since the ECMWF parametrization is largely based on the COARE* parametrization,
+the two algorithms are very similar in terms of structure and closure
+approach. As such, the namelist tuning for COARE 3.x is identical to that of
+ECMWF:
+%
+\begin{verbatim}
+  ...
+  ln_COARE3p6 = .true.
+  ...     
+  ln_skin_cs = .true. ! use the cool-skin parameterization
+  ln_skin_wl = .true. ! use the warm-layer parameterization
+  ...
+\end{verbatim}
+
+Note: when \np[=T]{ln_COARE3p0}{ln\_COARE3p0} is selected, the selection
+of \np{ln_skin_cs}{ln\_skin\_cs} and \np{ln_skin_wl}{ln\_skin\_wl} implicitly
+triggers the use of the COARE cool-skin and warm-layer parametrizations,
+respectively (found in \textit{sbcblk\_skin\_coare.F90}).
+
+
+%lulu
+
+
+
+% In a typical bulk algorithm, the BTCs under neutral stability conditions are
+% defined using \emph{in-situ} flux measurements while their dependence on the
+% stability is accounted through the \emph{Monin-Obukhov Similarity Theory} and
+% the \emph{flux-profile} relationships \citep[\eg{}][]{Paulson_1970}. BTCs are
+% functions of the wind speed and the near-surface stability of the atmospheric
+% surface layer (hereafter ASL), and hence, depend on $U_B$, $T_s$, $T_z$, $q_s$
+% and $q_z$.
+
+
+
+\subsection{Prescribed near-surface atmospheric state}
+
+The atmospheric fields used depend on the bulk formulae used.  In forced mode,
+when a sea-ice model is used, a specific bulk formulation is used.  Therefore,
+different bulk formulae are used for the turbulent fluxes computation over the
+ocean and over sea-ice surface.
+%
+
+%The choice is made by setting to true one of the following namelist
+%variable: \np{ln_NCAR}{ln\_NCAR}, \np{ln_COARE_3p0}{ln\_COARE\_3p0}, \np{ln_COARE_3p6}{ln\_COARE\_3p6}
+%and \np{ln_ECMWF}{ln\_ECMWF}. 
 
 Common options are defined through the \nam{sbc_blk}{sbc\_blk} namelist variables.
@@ -553 +814 @@
     Variable description                 & Model variable & Units              & point \\
     \hline
-    i-component of the 10m air velocity  & utau           & $m.s^{-1}$         & T     \\
+    i-component of the 10m air velocity  & wndi           & $m.s^{-1}$         & T     \\
     \hline
-    j-component of the 10m air velocity  & vtau           & $m.s^{-1}$         & T     \\
+    j-component of the 10m air velocity  & wndj           & $m.s^{-1}$         & T     \\
     \hline
-    10m air temperature                  & tair           & \r{}$K$            & T     \\
+    10m air temperature                  & tair           & $K$               & T     \\
     \hline
-    Specific humidity                    & humi           & \%                 & T     \\
+    Specific humidity                    & humi           & $-$               & T     \\
+    Relative humidity                    & ~              & $\%$              & T     \\
+    Dew-point temperature                & ~              & $K$               & T     \\    
     \hline
-    Incoming long wave radiation         & qlw            & $W.m^{-2}$         & T     \\
+    Downwelling longwave radiation       & qlw            & $W.m^{-2}$         & T     \\
     \hline
-    Incoming short wave radiation        & qsr            & $W.m^{-2}$         & T     \\
+    Downwelling shortwave radiation      & qsr            & $W.m^{-2}$         & T     \\
     \hline
     Total precipitation (liquid + solid) & precip         & $Kg.m^{-2}.s^{-1}$ & T     \\
@@ -584 +847 @@
 
 \np{cn_dir}{cn\_dir} is the directory of location of bulk files
-\np{ln_taudif}{ln\_taudif} is the flag to specify if we use Hight Frequency (HF) tau information (.true.) or not (.false.)
+%\np{ln_taudif}{ln\_taudif} is the flag to specify if we use High Frequency (HF) tau information (.true.) or not (.false.)
 \np{rn_zqt}{rn\_zqt}: is the height of humidity and temperature measurements (m)
 \np{rn_zu}{rn\_zu}: is the height of wind measurements (m)
@@ -595 +858 @@
 Its range must be between zero and one, and it is recommended to set it to 0 at low-resolution (ORCA2 configuration).
 
-As for the flux formulation, information about the input data required by the model is provided in
+As for the flux parametrization, information about the input data required by the model is provided in
 the namsbc\_blk namelist (see \autoref{subsec:SBC_fldread}).
 
-%% =================================================================================================
-\subsection[Ocean-Atmosphere Bulk formulae (\textit{sbcblk\_algo\_coare.F90, sbcblk\_algo\_coare3p5.F90, sbcblk\_algo\_ecmwf.F90, sbcblk\_algo\_ncar.F90})]{Ocean-Atmosphere Bulk formulae (\mdl{sbcblk\_algo\_coare}, \mdl{sbcblk\_algo\_coare3p5}, \mdl{sbcblk\_algo\_ecmwf}, \mdl{sbcblk\_algo\_ncar})}
-\label{subsec:SBC_blk_ocean}
-
-Four different bulk algorithms are available to compute surface turbulent momentum and heat fluxes over the ocean.
-COARE 3.0, COARE 3.5 and ECMWF schemes mainly differ by their roughness lenghts computation and consequently
-their neutral transfer coefficients relationships with neutral wind.
-\begin{itemize}
-\item NCAR (\np[=.true.]{ln_NCAR}{ln\_NCAR}): The NCAR bulk formulae have been developed by \citet{large.yeager_rpt04}.
-  They have been designed to handle the NCAR forcing, a mixture of NCEP reanalysis and satellite data.
-  They use an inertial dissipative method to compute the turbulent transfer coefficients
-  (momentum, sensible heat and evaporation) from the 10m wind speed, air temperature and specific humidity.
-  This \citet{large.yeager_rpt04} dataset is available through
-  the \href{http://nomads.gfdl.noaa.gov/nomads/forms/mom4/NCAR.html}{GFDL web site}.
-  Note that substituting ERA40 to NCEP reanalysis fields does not require changes in the bulk formulea themself.
-  This is the so-called DRAKKAR Forcing Set (DFS) \citep{brodeau.barnier.ea_OM10}.
-\item COARE 3.0 (\np[=.true.]{ln_COARE_3p0}{ln\_COARE\_3p0}): See \citet{fairall.bradley.ea_JC03} for more details
-\item COARE 3.5 (\np[=.true.]{ln_COARE_3p5}{ln\_COARE\_3p5}): See \citet{edson.jampana.ea_JPO13} for more details
-\item ECMWF (\np[=.true.]{ln_ECMWF}{ln\_ECMWF}): Based on \href{https://www.ecmwf.int/node/9221}{IFS (Cy31)} implementation and documentation.
-  Surface roughness lengths needed for the Obukhov length are computed following \citet{beljaars_QJRMS95}.
-\end{itemize}
+
+\subsubsection{Air humidity}
+
+Air humidity can be provided as three different parameters: specific humidity
+[kg/kg], relative humidity [\%], or dew-point temperature [K] (LINK to namelist
+parameters)...
+
+
+~\\
+
+
+
+
+
+
+
+
+
+
+%% =================================================================================================
+%\subsection[Ocean-Atmosphere Bulk formulae (\textit{sbcblk\_algo\_coare3p0.F90, sbcblk\_algo\_coare3p6.F90, %sbcblk\_algo\_ecmwf.F90, sbcblk\_algo\_ncar.F90})]{Ocean-Atmosphere Bulk formulae (\mdl{sbcblk\_algo\_coare3p0}, %\mdl{sbcblk\_algo\_coare3p6}, \mdl{sbcblk\_algo\_ecmwf}, \mdl{sbcblk\_algo\_ncar})}
+%\label{subsec:SBC_blk_ocean}
+
+%Four different bulk algorithms are available to compute surface turbulent momentum and heat fluxes over the ocean.
+%COARE 3.0, COARE 3.6 and ECMWF schemes mainly differ by their roughness lenghts computation and consequently
+%their neutral transfer coefficients relationships with neutral wind.
+%\begin{itemize}
+%\item NCAR (\np[=.true.]{ln_NCAR}{ln\_NCAR}): The NCAR bulk formulae have been developed by \citet{large.yeager_rpt04}.
+%  They have been designed to handle the NCAR forcing, a mixture of NCEP reanalysis and satellite data.
+%  They use an inertial dissipative method to compute the turbulent transfer coefficients
+%  (momentum, sensible heat and evaporation) from the 10m wind speed, air temperature and specific humidity.
+%  This \citet{large.yeager_rpt04} dataset is available through
+%  the \href{http://nomads.gfdl.noaa.gov/nomads/forms/mom4/NCAR.html}{GFDL web site}.
+%  Note that substituting ERA40 to NCEP reanalysis fields does not require changes in the bulk formulea themself.
+%  This is the so-called DRAKKAR Forcing Set (DFS) \citep{brodeau.barnier.ea_OM10}.
+%\item COARE 3.0 (\np[=.true.]{ln_COARE_3p0}{ln\_COARE\_3p0}): See \citet{fairall.bradley.ea_JC03} for more details
+%\item COARE 3.6 (\np[=.true.]{ln_COARE_3p6}{ln\_COARE\_3p6}): See \citet{edson.jampana.ea_JPO13} for more details
+%\item ECMWF (\np[=.true.]{ln_ECMWF}{ln\_ECMWF}): Based on \href{https://www.ecmwf.int/node/9204}{IFS (Cy40r1)} %implementation and documentation.
+%  Surface roughness lengths needed for the Obukhov length are computed
+%  following \citet{beljaars_QJRMS95}.
+%\end{itemize}
 
 %% =================================================================================================
 \subsection{Ice-Atmosphere Bulk formulae}
 \label{subsec:SBC_blk_ice}
+
+
+\texttt{\#out\_of\_place:}
+ For sea-ice, three possibilities can be selected:
+a constant transfer coefficient (1.4e-3; default
+value), \citet{lupkes.gryanik.ea_JGR12} (\np{ln_Cd_L12}{ln\_Cd\_L12}),
+and \citet{lupkes.gryanik_JGR15} (\np{ln_Cd_L15}{ln\_Cd\_L15}) parameterizations
+\texttt{\#out\_of\_place.}
+
+
+
 
 Surface turbulent fluxes between sea-ice and the atmosphere can be computed in three different ways:
@@ -880 +1174 @@
 %ENDIF
 
-%\gmcomment{  word doc of runoffs:
-%In the current \NEMO\ setup river runoff is added to emp fluxes, these are then applied at just the sea surface as a volume change (in the variable volume case this is a literal volume change, and in the linear free surface case the free surface is moved) and a salt flux due to the concentration/dilution effect.  There is also an option to increase vertical mixing near river mouths; this gives the effect of having a 3d river.  All river runoff and emp fluxes are assumed to be fresh water (zero salinity) and at the same temperature as the sea surface.
-%Our aim was to code the option to specify the temperature and salinity of river runoff, (as well as the amount), along with the depth that the river water will affect.  This would make it possible to model low salinity outflow, such as the Baltic, and would allow the ocean temperature to be affected by river runoff.
-
-%The depth option makes it possible to have the river water affecting just the surface layer, throughout depth, or some specified point in between.
-
-%To do this we need to treat evaporation/precipitation fluxes and river runoff differently in the tra_sbc module.  We decided to separate them throughout the code, so that the variable emp represented solely evaporation minus precipitation fluxes, and a new 2d variable rnf was added which represents the volume flux of river runoff (in kg/m2s to remain consistent with emp).  This meant many uses of emp and emps needed to be changed, a list of all modules which use emp or emps and the changes made are below:
+\cmtgm{  word doc of runoffs:
+In the current \NEMO\ setup river runoff is added to emp fluxes,
+these are then applied at just the sea surface as a volume change (in the variable volume case
+this is a literal volume change, and in the linear free surface case the free surface is moved)
+and a salt flux due to the concentration/dilution effect.
+There is also an option to increase vertical mixing near river mouths;
+this gives the effect of having a 3d river.
+All river runoff and emp fluxes are assumed to be fresh water (zero salinity) and
+at the same temperature as the sea surface.
+Our aim was to code the option to specify the temperature and salinity of river runoff,
+(as well as the amount), along with the depth that the river water will affect.
+This would make it possible to model low salinity outflow, such as the Baltic,
+and would allow the ocean temperature to be affected by river runoff.
+
+The depth option makes it possible to have the river water affecting just the surface layer,
+throughout depth, or some specified point in between.
+
+To do this we need to treat evaporation/precipitation fluxes and river runoff differently in
+the \mdl{tra_sbc} module.
+We decided to separate them throughout the code,
+so that the variable emp represented solely evaporation minus precipitation fluxes,
+and a new 2d variable rnf was added which represents the volume flux of river runoff
+(in $kg/m^2s$ to remain consistent with $emp$).
+This meant many uses of emp and emps needed to be changed,
+a list of all modules which use $emp$ or $emps$ and the changes made are below:}
 
 %% =================================================================================================
@@ -908 +1220 @@
   Two different bulk formulae are available:
 
-   \begin{description}
-   \item [{\np[=1]{nn_isfblk}{nn\_isfblk}}]: The melt rate is based on a balance between the upward ocean heat flux and
-     the latent heat flux at the ice shelf base. A complete description is available in \citet{hunter_rpt06}.
-   \item [{\np[=2]{nn_isfblk}{nn\_isfblk}}]: The melt rate and the heat flux are based on a 3 equations formulation
-     (a heat flux budget at the ice base, a salt flux budget at the ice base and a linearised freezing point temperature equation).
-     A complete description is available in \citet{jenkins_JGR91}.
-   \end{description}
-
-     Temperature and salinity used to compute the melt are the average temperature in the top boundary layer \citet{losch_JGR08}.
-     Its thickness is defined by \np{rn_hisf_tbl}{rn\_hisf\_tbl}.
-     The fluxes and friction velocity are computed using the mean temperature, salinity and velocity in the the first \np{rn_hisf_tbl}{rn\_hisf\_tbl} m.
-     Then, the fluxes are spread over the same thickness (ie over one or several cells).
-     If \np{rn_hisf_tbl}{rn\_hisf\_tbl} larger than top $e_{3}t$, there is no more feedback between the freezing point at the interface and the the top cell temperature.
-     This can lead to super-cool temperature in the top cell under melting condition.
-     If \np{rn_hisf_tbl}{rn\_hisf\_tbl} smaller than top $e_{3}t$, the top boundary layer thickness is set to the top cell thickness.\\
-
-     Each melt bulk formula depends on a exchange coeficient ($\Gamma^{T,S}$) between the ocean and the ice.
-     There are 3 different ways to compute the exchange coeficient:
-   \begin{description}
-        \item [{\np[=0]{nn_gammablk}{nn\_gammablk}}]: The salt and heat exchange coefficients are constant and defined by \np{rn_gammas0}{rn\_gammas0} and \np{rn_gammat0}{rn\_gammat0}.
-     \begin{gather*}
+  \begin{description}
+  \item [{\np[=1]{nn_isfblk}{nn\_isfblk}}]: The melt rate is based on a balance between the upward ocean heat flux and
+    the latent heat flux at the ice shelf base. A complete description is available in \citet{hunter_rpt06}.
+  \item [{\np[=2]{nn_isfblk}{nn\_isfblk}}]: The melt rate and the heat flux are based on a 3 equations formulation
+    (a heat flux budget at the ice base, a salt flux budget at the ice base and a linearised freezing point temperature equation).
+    A complete description is available in \citet{jenkins_JGR91}.
+  \end{description}
+
+  Temperature and salinity used to compute the melt are the average temperature in the top boundary layer \citet{losch_JGR08}.
+  Its thickness is defined by \np{rn_hisf_tbl}{rn\_hisf\_tbl}.
+  The fluxes and friction velocity are computed using the mean temperature, salinity and velocity in the the first \np{rn_hisf_tbl}{rn\_hisf\_tbl} m.
+  Then, the fluxes are spread over the same thickness (ie over one or several cells).
+  If \np{rn_hisf_tbl}{rn\_hisf\_tbl} larger than top $e_{3}t$, there is no more feedback between the freezing point at the interface and the the top cell temperature.
+  This can lead to super-cool temperature in the top cell under melting condition.
+  If \np{rn_hisf_tbl}{rn\_hisf\_tbl} smaller than top $e_{3}t$, the top boundary layer thickness is set to the top cell thickness.\\
+
+  Each melt bulk formula depends on a exchange coeficient ($\Gamma^{T,S}$) between the ocean and the ice.
+  There are 3 different ways to compute the exchange coeficient:
+  \begin{description}
+  \item [{\np[=0]{nn_gammablk}{nn\_gammablk}}]: The salt and heat exchange coefficients are constant and defined by \np{rn_gammas0}{rn\_gammas0} and \np{rn_gammat0}{rn\_gammat0}.
+    \begin{gather*}
        % \label{eq:SBC_isf_gamma_iso}
-       \gamma^{T} = rn\_gammat0 \\
-       \gamma^{S} = rn\_gammas0
-     \end{gather*}
-     This is the recommended formulation for ISOMIP.
-   \item [{\np[=1]{nn_gammablk}{nn\_gammablk}}]: The salt and heat exchange coefficients are velocity dependent and defined as
-     \begin{gather*}
-       \gamma^{T} = rn\_gammat0 \times u_{*} \\
-       \gamma^{S} = rn\_gammas0 \times u_{*}
-     \end{gather*}
-     where $u_{*}$ is the friction velocity in the top boundary layer (ie first \np{rn_hisf_tbl}{rn\_hisf\_tbl} meters).
-     See \citet{jenkins.nicholls.ea_JPO10} for all the details on this formulation. It is the recommended formulation for realistic application.
-   \item [{\np[=2]{nn_gammablk}{nn\_gammablk}}]: The salt and heat exchange coefficients are velocity and stability dependent and defined as:
-\[
-\gamma^{T,S} = \frac{u_{*}}{\Gamma_{Turb} + \Gamma^{T,S}_{Mole}}
-\]
-     where $u_{*}$ is the friction velocity in the top boundary layer (ie first \np{rn_hisf_tbl}{rn\_hisf\_tbl} meters),
-     $\Gamma_{Turb}$ the contribution of the ocean stability and
-     $\Gamma^{T,S}_{Mole}$ the contribution of the molecular diffusion.
-     See \citet{holland.jenkins_JPO99} for all the details on this formulation.
-     This formulation has not been extensively tested in \NEMO\ (not recommended).
-   \end{description}
-  \item [{\np[=2]{nn_isf}{nn\_isf}}]: The ice shelf cavity is not represented.
-   The fwf and heat flux are computed using the \citet{beckmann.goosse_OM03} parameterisation of isf melting.
-   The fluxes are distributed along the ice shelf edge between the depth of the average grounding line (GL)
-   (\np{sn_depmax_isf}{sn\_depmax\_isf}) and the base of the ice shelf along the calving front
-   (\np{sn_depmin_isf}{sn\_depmin\_isf}) as in (\np[=3]{nn_isf}{nn\_isf}).
-   The effective melting length (\np{sn_Leff_isf}{sn\_Leff\_isf}) is read from a file.
-  \item [{\np[=3]{nn_isf}{nn\_isf}}]: The ice shelf cavity is not represented.
-   The fwf (\np{sn_rnfisf}{sn\_rnfisf}) is prescribed and distributed along the ice shelf edge between
-   the depth of the average grounding line (GL) (\np{sn_depmax_isf}{sn\_depmax\_isf}) and
-   the base of the ice shelf along the calving front (\np{sn_depmin_isf}{sn\_depmin\_isf}).
-   The heat flux ($Q_h$) is computed as $Q_h = fwf \times L_f$.
-  \item [{\np[=4]{nn_isf}{nn\_isf}}]: The ice shelf cavity is opened (\np[=.true.]{ln_isfcav}{ln\_isfcav} needed).
-   However, the fwf is not computed but specified from file \np{sn_fwfisf}{sn\_fwfisf}).
-   The heat flux ($Q_h$) is computed as $Q_h = fwf \times L_f$.
-   As in \np[=1]{nn_isf}{nn\_isf}, the fluxes are spread over the top boundary layer thickness (\np{rn_hisf_tbl}{rn\_hisf\_tbl})\\
+      \gamma^{T} = rn\_gammat0 \\
+      \gamma^{S} = rn\_gammas0
+    \end{gather*}
+    This is the recommended formulation for ISOMIP.
+  \item [{\np[=1]{nn_gammablk}{nn\_gammablk}}]: The salt and heat exchange coefficients are velocity dependent and defined as
+    \begin{gather*}
+      \gamma^{T} = rn\_gammat0 \times u_{*} \\
+      \gamma^{S} = rn\_gammas0 \times u_{*}
+    \end{gather*}
+    where $u_{*}$ is the friction velocity in the top boundary layer (ie first \np{rn_hisf_tbl}{rn\_hisf\_tbl} meters).
+    See \citet{jenkins.nicholls.ea_JPO10} for all the details on this formulation. It is the recommended formulation for realistic application.
+  \item [{\np[=2]{nn_gammablk}{nn\_gammablk}}]: The salt and heat exchange coefficients are velocity and stability dependent and defined as:
+    \[
+      \gamma^{T,S} = \frac{u_{*}}{\Gamma_{Turb} + \Gamma^{T,S}_{Mole}}
+    \]
+    where $u_{*}$ is the friction velocity in the top boundary layer (ie first \np{rn_hisf_tbl}{rn\_hisf\_tbl} meters),
+    $\Gamma_{Turb}$ the contribution of the ocean stability and
+    $\Gamma^{T,S}_{Mole}$ the contribution of the molecular diffusion.
+    See \citet{holland.jenkins_JPO99} for all the details on this formulation.
+    This formulation has not been extensively tested in \NEMO\ (not recommended).
+  \end{description}
+\item [{\np[=2]{nn_isf}{nn\_isf}}]: The ice shelf cavity is not represented.
+  The fwf and heat flux are computed using the \citet{beckmann.goosse_OM03} parameterisation of isf melting.
+  The fluxes are distributed along the ice shelf edge between the depth of the average grounding line (GL)
+  (\np{sn_depmax_isf}{sn\_depmax\_isf}) and the base of the ice shelf along the calving front
+  (\np{sn_depmin_isf}{sn\_depmin\_isf}) as in (\np[=3]{nn_isf}{nn\_isf}).
+  The effective melting length (\np{sn_Leff_isf}{sn\_Leff\_isf}) is read from a file.
+\item [{\np[=3]{nn_isf}{nn\_isf}}]: The ice shelf cavity is not represented.
+  The fwf (\np{sn_rnfisf}{sn\_rnfisf}) is prescribed and distributed along the ice shelf edge between
+  the depth of the average grounding line (GL) (\np{sn_depmax_isf}{sn\_depmax\_isf}) and
+  the base of the ice shelf along the calving front (\np{sn_depmin_isf}{sn\_depmin\_isf}).
+  The heat flux ($Q_h$) is computed as $Q_h = fwf \times L_f$.
+\item [{\np[=4]{nn_isf}{nn\_isf}}]: The ice shelf cavity is opened (\np[=.true.]{ln_isfcav}{ln\_isfcav} needed).
+  However, the fwf is not computed but specified from file \np{sn_fwfisf}{sn\_fwfisf}).
+  The heat flux ($Q_h$) is computed as $Q_h = fwf \times L_f$.
+  As in \np[=1]{nn_isf}{nn\_isf}, the fluxes are spread over the top boundary layer thickness (\np{rn_hisf_tbl}{rn\_hisf\_tbl})
 \end{description}
 
@@ -986 +1298 @@
 \begin{figure}[!t]
   \centering
-  \includegraphics[width=0.66\textwidth]{Fig_SBC_isf}
+  \includegraphics[width=0.66\textwidth]{SBC_isf}
   \caption[Ice shelf location and fresh water flux definition]{
     Illustration of the location where the fwf is injected and
@@ -1307 +1619 @@
 \begin{figure}[!t]
   \centering
-  \includegraphics[width=0.66\textwidth]{Fig_SBC_diurnal}
+  \includegraphics[width=0.66\textwidth]{SBC_diurnal}
   \caption[Reconstruction of the diurnal cycle variation of short wave flux]{
     Example of reconstruction of the diurnal cycle variation of short wave flux from
@@ -1341 +1653 @@
 \begin{figure}[!t]
   \centering
-  \includegraphics[width=0.66\textwidth]{Fig_SBC_dcy}
+  \includegraphics[width=0.66\textwidth]{SBC_dcy}
   \caption[Reconstruction of the diurnal cycle variation of short wave flux on an ORCA2 grid]{
     Example of reconstruction of the diurnal cycle variation of short wave flux from
@@ -1521 +1833 @@
 % in ocean-ice models.
 
-\onlyinsubfile{\input{../../global/epilogue}}
+\subinc{\input{../../global/epilogue}}
 
 \end{document}

@@ -6 +6 @@
 ^/vendors/FCM@HEAD            ext/FCM
 ^/vendors/IOIPSL@HEAD         ext/IOIPSL
+
+# SETTE
+^/utils/CI/sette@HEAD         sette