Changeset 3683 for trunk/DOC/TexFiles/Chapters
- Timestamp:
- 2012-11-27T16:21:24+01:00 (12 years ago)
- Location:
- trunk/DOC/TexFiles/Chapters
- Files:
-
- 6 edited
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trunk/DOC/TexFiles/Chapters/Chap_CFG.tex
r3294 r3683 206 206 % ------------------------------------------------------------------------------------------------------------- 207 207 \section{GYRE family: double gyre basin (\key{gyre})} 208 \label{ MISC_config_gyre}208 \label{CFG_gyre} 209 209 210 210 The GYRE configuration \citep{Levy_al_OM10} have been built to simulated -
trunk/DOC/TexFiles/Chapters/Chap_DIA.tex
r3294 r3683 1018 1018 In addition, a series of diagnostics has been added in the \mdl{diaar5}. 1019 1019 They corresponds to outputs that are required for AR5 simulations 1020 (see Section \ref{ MISC_steric} below for one of them).1020 (see Section \ref{DIA_steric} below for one of them). 1021 1021 Activating those outputs requires to define the \key{diaar5} CPP key. 1022 1022 \\ -
trunk/DOC/TexFiles/Chapters/Chap_DOM.tex
r3294 r3683 499 499 Hybridation of the three main coordinates are available: $s-z$ or $s-zps$ coordinate 500 500 (Fig.~\ref{Fig_z_zps_s_sps}d and \ref{Fig_z_zps_s_sps}e). When using the variable 501 volume option \key{vvl} )($i.e.$ non-linear free surface), the coordinate follow the501 volume option \key{vvl} ($i.e.$ non-linear free surface), the coordinate follow the 502 502 time-variation of the free surface so that the transformation is time dependent: 503 503 $z(i,j,k,t)$ (Fig.~\ref{Fig_z_zps_s_sps}f). This option can be used with full step -
trunk/DOC/TexFiles/Chapters/Chap_DYN.tex
r3294 r3683 127 127 This is of paramount importance. Replacing $T$ by the number $1$ in the tracer equation and summing 128 128 over the water column must lead to the sea surface height equation otherwise tracer content 129 will not be conserved \ ref{Griffies_al_MWR01, LeclairMadec2009}.129 will not be conserved \citep{Griffies_al_MWR01, Leclair_Madec_OM09}. 130 130 131 131 The vertical velocity is computed by an upward integration of the horizontal … … 189 189 the relative vorticity term and horizontal kinetic energy for the planetary vorticity 190 190 term (MIX scheme) ; or conserving both the potential enstrophy of horizontally non-divergent 191 flow and horizontal kinetic energy (EEN scheme) (see Appendix~\ref{Apdx_C_vor _zad}). In the191 flow and horizontal kinetic energy (EEN scheme) (see Appendix~\ref{Apdx_C_vorEEN}). In the 192 192 case of ENS, ENE or MIX schemes the land sea mask may be slightly modified to ensure the 193 193 consistency of vorticity term with analytical equations (\textit{ln\_dynvor\_con}=true). … … 331 331 This EEN scheme in fact combines the conservation properties of the ENS and ENE schemes. 332 332 It conserves both total energy and potential enstrophy in the limit of horizontally 333 nondivergent flow ($i.e.$ $\chi$=$0$) (see Appendix~\ref{Apdx_C_vor _zad}).333 nondivergent flow ($i.e.$ $\chi$=$0$) (see Appendix~\ref{Apdx_C_vorEEN}). 334 334 Applied to a realistic ocean configuration, it has been shown that it leads to a significant 335 335 reduction of the noise in the vertical velocity field \citep{Le_Sommer_al_OM09}. … … 938 938 is the \textit{before} velocity in time, except for the pure vertical component 939 939 that appears when a tensor of rotation is used. This latter term is solved 940 implicitly together with the vertical diffusion term (see \S\ref{ DOM_nxt})940 implicitly together with the vertical diffusion term (see \S\ref{STP}) 941 941 942 942 At the lateral boundaries either free slip, no slip or partial slip boundary … … 1066 1066 scheme (\np{ln\_zdfexp}=true) using a time splitting technique 1067 1067 (\np{nn\_zdfexp} $>$ 1) or $(b)$ a backward (or implicit) time differencing scheme 1068 (\np{ln\_zdfexp}=false) (see \S\ref{ DOM_nxt}). Note that namelist variables1068 (\np{ln\_zdfexp}=false) (see \S\ref{STP}). Note that namelist variables 1069 1069 \np{ln\_zdfexp} and \np{nn\_zdfexp} apply to both tracers and dynamics. 1070 1070 -
trunk/DOC/TexFiles/Chapters/Chap_TRA.tex
r3308 r3683 264 264 transport) rather than TVD. The TVD scheme is implemented in the \mdl{traadv\_tvd} module. 265 265 266 For stability reasons (see \S\ref{ DOM_nxt}),266 For stability reasons (see \S\ref{STP}), 267 267 $\tau _u^{cen2}$ is evaluated in (\ref{Eq_tra_adv_tvd}) using the \textit{now} tracer while $\tau _u^{ups}$ 268 268 is evaluated using the \textit{before} tracer. In other words, the advective part of … … 337 337 \np{ln\_traadv\_ubs}=true. 338 338 339 For stability reasons (see \S\ref{ DOM_nxt}),339 For stability reasons (see \S\ref{STP}), 340 340 the first term in \eqref{Eq_tra_adv_ubs} (which corresponds to a second order centred scheme) 341 341 is evaluated using the \textit{now} tracer (centred in time) while the … … 451 451 except for the pure vertical component that appears when a rotation tensor 452 452 is used. This latter term is solved implicitly together with the 453 vertical diffusion term (see \S\ref{ DOM_nxt}).453 vertical diffusion term (see \S\ref{STP}). 454 454 455 455 % ------------------------------------------------------------------------------------------------------------- -
trunk/DOC/TexFiles/Chapters/Chap_ZDF.tex
r3294 r3683 120 120 \end{equation} 121 121 122 is computed from the wind stress vector $|\tau|$ and the reference den dity $ \rho_o$.122 is computed from the wind stress vector $|\tau|$ and the reference density $ \rho_o$. 123 123 The final $h_{e}$ is further constrained by the adjustable bounds \np{rn\_mldmin} and \np{rn\_mldmax}. 124 124 Once $h_{e}$ is computed, the vertical eddy coefficients within $h_{e}$ are set to … … 1188 1188 \includegraphics[width=0.90\textwidth]{./TexFiles/Figures/Fig_ZDF_M2_K1_tmx.pdf} 1189 1189 \caption{ \label{Fig_ZDF_M2_K1_tmx} 1190 (a) M2 and (b) K 2internal wave drag energy from \citet{Carrere_Lyard_GRL03} ($W/m^2$). }1190 (a) M2 and (b) K1 internal wave drag energy from \citet{Carrere_Lyard_GRL03} ($W/m^2$). } 1191 1191 \end{center} \end{figure} 1192 1192 %>>>>>>>>>>>>>>>>>>>>>>>>>>>> … … 1205 1205 1206 1206 When \np{ln\_tmx\_itf}=true, the two key parameters $q$ and $F(z)$ are adjusted following 1207 the parameterisation developed by \ ref{Koch-Larrouy_al_GRL07}:1207 the parameterisation developed by \citet{Koch-Larrouy_al_GRL07}: 1208 1208 1209 1209 First, the Indonesian archipelago is a complex geographic region … … 1219 1219 Second, the vertical structure function, $F(z)$, is no more associated 1220 1220 with a bottom intensification of the mixing, but with a maximum of 1221 energy available within the thermocline. \ ref{Koch-Larrouy_al_GRL07}1221 energy available within the thermocline. \citet{Koch-Larrouy_al_GRL07} 1222 1222 have suggested that the vertical distribution of the energy dissipation 1223 1223 proportional to $N^2$ below the core of the thermocline and to $N$ above. … … 1236 1236 and vertical distributions of the mixing are adequately prescribed 1237 1237 \citep{Koch-Larrouy_al_GRL07, Koch-Larrouy_al_OD08a, Koch-Larrouy_al_OD08b}. 1238 Note also that such a parameterisation has a s ugnificant impact on the behaviour1238 Note also that such a parameterisation has a significant impact on the behaviour 1239 1239 of global coupled GCMs \citep{Koch-Larrouy_al_CD10}. 1240 1240
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