Changeset 11537 for NEMO/trunk/doc/latex/NEMO/subfiles/chap_TRA.tex
- Timestamp:
- 2019-09-12T10:24:48+02:00 (5 years ago)
- File:
-
- 1 edited
-
NEMO/trunk/doc/latex/NEMO/subfiles/chap_TRA.tex (modified) (36 diffs)
Legend:
- Unmodified
- Added
- Removed
-
NEMO/trunk/doc/latex/NEMO/subfiles/chap_TRA.tex
r11524 r11537 55 55 56 56 The user has the option of extracting each tendency term on the RHS of the tracer equation for output 57 (\np{ln\_tra\_trd} or \np{ln\_tra\_mxl}\forcode{ =.true.}), as described in \autoref{chap:DIA}.57 (\np{ln\_tra\_trd} or \np{ln\_tra\_mxl}\forcode{=.true.}), as described in \autoref{chap:DIA}. 58 58 59 59 % ================================================================ … … 82 82 Indeed, it is obtained by using the following equality: $\nabla \cdot (\vect U \, T) = \vect U \cdot \nabla T$ which 83 83 results from the use of the continuity equation, $\partial_t e_3 + e_3 \; \nabla \cdot \vect U = 0$ 84 (which reduces to $\nabla \cdot \vect U = 0$ in linear free surface, \ie\ \np{ln\_linssh}\forcode{ =.true.}).84 (which reduces to $\nabla \cdot \vect U = 0$ in linear free surface, \ie\ \np{ln\_linssh}\forcode{=.true.}). 85 85 Therefore it is of paramount importance to design the discrete analogue of the advection tendency so that 86 86 it is consistent with the continuity equation in order to enforce the conservation properties of 87 87 the continuous equations. 88 In other words, by setting $\tau =1$ in (\autoref{eq:tra_adv}) we recover the discrete form of88 In other words, by setting $\tau=1$ in (\autoref{eq:tra_adv}) we recover the discrete form of 89 89 the continuity equation which is used to calculate the vertical velocity. 90 90 %>>>>>>>>>>>>>>>>>>>>>>>>>>>> … … 120 120 \begin{description} 121 121 \item[linear free surface:] 122 (\np{ln\_linssh}\forcode{ =.true.})122 (\np{ln\_linssh}\forcode{=.true.}) 123 123 the first level thickness is constant in time: 124 124 the vertical boundary condition is applied at the fixed surface $z = 0$ rather than on … … 128 128 the first level tracer value. 129 129 \item[non-linear free surface:] 130 (\np{ln\_linssh}\forcode{ =.false.})130 (\np{ln\_linssh}\forcode{=.false.}) 131 131 convergence/divergence in the first ocean level moves the free surface up/down. 132 132 There is no tracer advection through it so that the advective fluxes through the surface are also zero. … … 184 184 % 2nd and 4th order centred schemes 185 185 % ------------------------------------------------------------------------------------------------------------- 186 \subsection[CEN: Centred scheme (\forcode{ln_traadv_cen =.true.})]187 {CEN: Centred scheme (\protect\np{ln\_traadv\_cen}\forcode{ =.true.})}186 \subsection[CEN: Centred scheme (\forcode{ln_traadv_cen=.true.})] 187 {CEN: Centred scheme (\protect\np{ln\_traadv\_cen}\forcode{=.true.})} 188 188 \label{subsec:TRA_adv_cen} 189 189 190 190 % 2nd order centred scheme 191 191 192 The centred advection scheme (CEN) is used when \np{ln\_traadv\_cen}\forcode{ =.true.}.192 The centred advection scheme (CEN) is used when \np{ln\_traadv\_cen}\forcode{=.true.}. 193 193 Its order ($2^{nd}$ or $4^{th}$) can be chosen independently on horizontal (iso-level) and vertical direction by 194 194 setting \np{nn\_cen\_h} and \np{nn\_cen\_v} to $2$ or $4$. … … 222 222 \tau_u^{cen4} = \overline{T - \frac{1}{6} \, \delta_i \Big[ \delta_{i + 1/2}[T] \, \Big]}^{\,i + 1/2} 223 223 \end{equation} 224 In the vertical direction (\np{nn\_cen\_v}\forcode{ =4}),224 In the vertical direction (\np{nn\_cen\_v}\forcode{=4}), 225 225 a $4^{th}$ COMPACT interpolation has been prefered \citep{demange_phd14}. 226 226 In the COMPACT scheme, both the field and its derivative are interpolated, which leads, after a matrix inversion, … … 252 252 % FCT scheme 253 253 % ------------------------------------------------------------------------------------------------------------- 254 \subsection[FCT: Flux Corrected Transport scheme (\forcode{ln_traadv_fct =.true.})]255 {FCT: Flux Corrected Transport scheme (\protect\np{ln\_traadv\_fct}\forcode{ =.true.})}254 \subsection[FCT: Flux Corrected Transport scheme (\forcode{ln_traadv_fct=.true.})] 255 {FCT: Flux Corrected Transport scheme (\protect\np{ln\_traadv\_fct}\forcode{=.true.})} 256 256 \label{subsec:TRA_adv_tvd} 257 257 258 The Flux Corrected Transport schemes (FCT) is used when \np{ln\_traadv\_fct}\forcode{ =.true.}.258 The Flux Corrected Transport schemes (FCT) is used when \np{ln\_traadv\_fct}\forcode{=.true.}. 259 259 Its order ($2^{nd}$ or $4^{th}$) can be chosen independently on horizontal (iso-level) and vertical direction by 260 260 setting \np{nn\_fct\_h} and \np{nn\_fct\_v} to $2$ or $4$. … … 296 296 % MUSCL scheme 297 297 % ------------------------------------------------------------------------------------------------------------- 298 \subsection[MUSCL: Monotone Upstream Scheme for Conservative Laws (\forcode{ln_traadv_mus =.true.})]299 {MUSCL: Monotone Upstream Scheme for Conservative Laws (\protect\np{ln\_traadv\_mus}\forcode{ =.true.})}298 \subsection[MUSCL: Monotone Upstream Scheme for Conservative Laws (\forcode{ln_traadv_mus=.true.})] 299 {MUSCL: Monotone Upstream Scheme for Conservative Laws (\protect\np{ln\_traadv\_mus}\forcode{=.true.})} 300 300 \label{subsec:TRA_adv_mus} 301 301 302 The Monotone Upstream Scheme for Conservative Laws (MUSCL) is used when \np{ln\_traadv\_mus}\forcode{ =.true.}.302 The Monotone Upstream Scheme for Conservative Laws (MUSCL) is used when \np{ln\_traadv\_mus}\forcode{=.true.}. 303 303 MUSCL implementation can be found in the \mdl{traadv\_mus} module. 304 304 … … 328 328 This choice ensure the \textit{positive} character of the scheme. 329 329 In addition, fluxes round a grid-point where a runoff is applied can optionally be computed using upstream fluxes 330 (\np{ln\_mus\_ups}\forcode{ =.true.}).330 (\np{ln\_mus\_ups}\forcode{=.true.}). 331 331 332 332 % ------------------------------------------------------------------------------------------------------------- 333 333 % UBS scheme 334 334 % ------------------------------------------------------------------------------------------------------------- 335 \subsection[UBS a.k.a. UP3: Upstream-Biased Scheme (\forcode{ln_traadv_ubs =.true.})]336 {UBS a.k.a. UP3: Upstream-Biased Scheme (\protect\np{ln\_traadv\_ubs}\forcode{ =.true.})}335 \subsection[UBS a.k.a. UP3: Upstream-Biased Scheme (\forcode{ln_traadv_ubs=.true.})] 336 {UBS a.k.a. UP3: Upstream-Biased Scheme (\protect\np{ln\_traadv\_ubs}\forcode{=.true.})} 337 337 \label{subsec:TRA_adv_ubs} 338 338 339 The Upstream-Biased Scheme (UBS) is used when \np{ln\_traadv\_ubs}\forcode{ =.true.}.339 The Upstream-Biased Scheme (UBS) is used when \np{ln\_traadv\_ubs}\forcode{=.true.}. 340 340 UBS implementation can be found in the \mdl{traadv\_mus} module. 341 341 … … 367 367 \citep{shchepetkin.mcwilliams_OM05, demange_phd14}. 368 368 Therefore the vertical flux is evaluated using either a $2^nd$ order FCT scheme or a $4^th$ order COMPACT scheme 369 (\np{nn\_ubs\_v}\forcode{ =2 or 4}).369 (\np{nn\_ubs\_v}\forcode{=2 or 4}). 370 370 371 371 For stability reasons (see \autoref{chap:STP}), the first term in \autoref{eq:tra_adv_ubs} … … 406 406 % QCK scheme 407 407 % ------------------------------------------------------------------------------------------------------------- 408 \subsection[QCK: QuiCKest scheme (\forcode{ln_traadv_qck =.true.})]409 {QCK: QuiCKest scheme (\protect\np{ln\_traadv\_qck}\forcode{ =.true.})}408 \subsection[QCK: QuiCKest scheme (\forcode{ln_traadv_qck=.true.})] 409 {QCK: QuiCKest scheme (\protect\np{ln\_traadv\_qck}\forcode{=.true.})} 410 410 \label{subsec:TRA_adv_qck} 411 411 412 412 The Quadratic Upstream Interpolation for Convective Kinematics with Estimated Streaming Terms (QUICKEST) scheme 413 proposed by \citet{leonard_CMAME79} is used when \np{ln\_traadv\_qck}\forcode{ =.true.}.413 proposed by \citet{leonard_CMAME79} is used when \np{ln\_traadv\_qck}\forcode{=.true.}. 414 414 QUICKEST implementation can be found in the \mdl{traadv\_qck} module. 415 415 … … 453 453 except for the pure vertical component that appears when a rotation tensor is used. 454 454 This latter component is solved implicitly together with the vertical diffusion term (see \autoref{chap:STP}). 455 When \np{ln\_traldf\_msc}\forcode{ =.true.}, a Method of Stabilizing Correction is used in which455 When \np{ln\_traldf\_msc}\forcode{=.true.}, a Method of Stabilizing Correction is used in which 456 456 the pure vertical component is split into an explicit and an implicit part \citep{lemarie.debreu.ea_OM12}. 457 457 … … 466 466 467 467 \begin{description} 468 \item[\np{ln\_traldf\_OFF}\forcode{ =.true.}:]468 \item[\np{ln\_traldf\_OFF}\forcode{=.true.}:] 469 469 no operator selected, the lateral diffusive tendency will not be applied to the tracer equation. 470 470 This option can be used when the selected advection scheme is diffusive enough (MUSCL scheme for example). 471 \item[\np{ln\_traldf\_lap}\forcode{ =.true.}:]471 \item[\np{ln\_traldf\_lap}\forcode{=.true.}:] 472 472 a laplacian operator is selected. 473 473 This harmonic operator takes the following expression: $\mathcal{L}(T) = \nabla \cdot A_{ht} \; \nabla T $, 474 474 where the gradient operates along the selected direction (see \autoref{subsec:TRA_ldf_dir}), 475 475 and $A_{ht}$ is the eddy diffusivity coefficient expressed in $m^2/s$ (see \autoref{chap:LDF}). 476 \item[\np{ln\_traldf\_blp}\forcode{ =.true.}]:476 \item[\np{ln\_traldf\_blp}\forcode{=.true.}]: 477 477 a bilaplacian operator is selected. 478 478 This biharmonic operator takes the following expression: … … 500 500 The choice of a direction of action determines the form of operator used. 501 501 The operator is a simple (re-entrant) laplacian acting in the (\textbf{i},\textbf{j}) plane when 502 iso-level option is used (\np{ln\_traldf\_lev}\forcode{ =.true.}) or502 iso-level option is used (\np{ln\_traldf\_lev}\forcode{=.true.}) or 503 503 when a horizontal (\ie\ geopotential) operator is demanded in \textit{z}-coordinate 504 (\np{ln\_traldf\_hor} and \np{ln\_zco} equal \forcode{.true.}).504 (\np{ln\_traldf\_hor} and \np{ln\_zco}\forcode{=.true.}). 505 505 The associated code can be found in the \mdl{traldf\_lap\_blp} module. 506 506 The operator is a rotated (re-entrant) laplacian when 507 507 the direction along which it acts does not coincide with the iso-level surfaces, 508 508 that is when standard or triad iso-neutral option is used 509 (\np{ln\_traldf\_iso} or \np{ln\_traldf\_triad} equals\forcode{.true.},509 (\np{ln\_traldf\_iso} or \np{ln\_traldf\_triad} = \forcode{.true.}, 510 510 see \mdl{traldf\_iso} or \mdl{traldf\_triad} module, resp.), or 511 511 when a horizontal (\ie\ geopotential) operator is demanded in \textit{s}-coordinate 512 (\np{ln\_traldf\_hor} and \np{ln\_sco} equal\forcode{.true.})512 (\np{ln\_traldf\_hor} and \np{ln\_sco} = \forcode{.true.}) 513 513 \footnote{In this case, the standard iso-neutral operator will be automatically selected}. 514 514 In that case, a rotation is applied to the gradient(s) that appears in the operator so that … … 540 540 It is a \textit{horizontal} operator (\ie acting along geopotential surfaces) in 541 541 the $z$-coordinate with or without partial steps, but is simply an iso-level operator in the $s$-coordinate. 542 It is thus used when, in addition to \np{ln\_traldf\_lap} or \np{ln\_traldf\_blp}\forcode{ =.true.},543 we have \np{ln\_traldf\_lev}\forcode{ = .true.} or \np{ln\_traldf\_hor}~=~\np{ln\_zco}\forcode{ =.true.}.542 It is thus used when, in addition to \np{ln\_traldf\_lap} or \np{ln\_traldf\_blp}\forcode{=.true.}, 543 we have \np{ln\_traldf\_lev}\forcode{=.true.} or \np{ln\_traldf\_hor}~=~\np{ln\_zco}\forcode{=.true.}. 544 544 In both cases, it significantly contributes to diapycnal mixing. 545 545 It is therefore never recommended, even when using it in the bilaplacian case. 546 546 547 Note that in the partial step $z$-coordinate (\np{ln\_zps}\forcode{ =.true.}),547 Note that in the partial step $z$-coordinate (\np{ln\_zps}\forcode{=.true.}), 548 548 tracers in horizontally adjacent cells are located at different depths in the vicinity of the bottom. 549 549 In this case, horizontal derivatives in (\autoref{eq:tra_ldf_lap}) at the bottom level require a specific treatment. … … 578 578 $r_1$ and $r_2$ are the slopes between the surface of computation ($z$- or $s$-surfaces) and 579 579 the surface along which the diffusion operator acts (\ie\ horizontal or iso-neutral surfaces). 580 It is thus used when, in addition to \np{ln\_traldf\_lap}\forcode{ =.true.},581 we have \np{ln\_traldf\_iso}\forcode{ =.true.},582 or both \np{ln\_traldf\_hor}\forcode{ = .true.} and \np{ln\_zco}\forcode{ =.true.}.580 It is thus used when, in addition to \np{ln\_traldf\_lap}\forcode{=.true.}, 581 we have \np{ln\_traldf\_iso}\forcode{=.true.}, 582 or both \np{ln\_traldf\_hor}\forcode{=.true.} and \np{ln\_zco}\forcode{=.true.}. 583 583 The way these slopes are evaluated is given in \autoref{sec:LDF_slp}. 584 584 At the surface, bottom and lateral boundaries, the turbulent fluxes of heat and salt are set to zero using … … 596 596 any additional background horizontal diffusion \citep{guilyardi.madec.ea_CD01}. 597 597 598 Note that in the partial step $z$-coordinate (\np{ln\_zps}\forcode{ =.true.}),598 Note that in the partial step $z$-coordinate (\np{ln\_zps}\forcode{=.true.}), 599 599 the horizontal derivatives at the bottom level in \autoref{eq:tra_ldf_iso} require a specific treatment. 600 600 They are calculated in module zpshde, described in \autoref{sec:TRA_zpshde}. … … 607 607 608 608 An alternative scheme developed by \cite{griffies.gnanadesikan.ea_JPO98} which ensures tracer variance decreases 609 is also available in \NEMO\ (\np{ln\_traldf\_triad}\forcode{ =.true.}).609 is also available in \NEMO\ (\np{ln\_traldf\_triad}\forcode{=.true.}). 610 610 A complete description of the algorithm is given in \autoref{apdx:triad}. 611 611 … … 655 655 respectively. 656 656 Generally, $A_w^{vT} = A_w^{vS}$ except when double diffusive mixing is parameterised 657 (\ie\ \np{ln\_zdfddm} equals \forcode{.true.},).657 (\ie\ \np{ln\_zdfddm}\forcode{=.true.},). 658 658 The way these coefficients are evaluated is given in \autoref{chap:ZDF} (ZDF). 659 659 Furthermore, when iso-neutral mixing is used, both mixing coefficients are increased by … … 731 731 Such time averaging prevents the divergence of odd and even time step (see \autoref{chap:STP}). 732 732 733 In the linear free surface case (\np{ln\_linssh}\forcode{ =.true.}), an additional term has to be added on733 In the linear free surface case (\np{ln\_linssh}\forcode{=.true.}), an additional term has to be added on 734 734 both temperature and salinity. 735 735 On temperature, this term remove the heat content associated with mass exchange that has been added to $Q_{ns}$. … … 763 763 764 764 Options are defined through the \nam{tra\_qsr} namelist variables. 765 When the penetrative solar radiation option is used (\np{ln\_traqsr}\forcode{ =.true.}),765 When the penetrative solar radiation option is used (\np{ln\_traqsr}\forcode{=.true.}), 766 766 the solar radiation penetrates the top few tens of meters of the ocean. 767 If it is not used (\np{ln\_traqsr}\forcode{ =.false.}) all the heat flux is absorbed in the first ocean level.767 If it is not used (\np{ln\_traqsr}\forcode{=.false.}) all the heat flux is absorbed in the first ocean level. 768 768 Thus, in the former case a term is added to the time evolution equation of temperature \autoref{eq:PE_tra_T} and 769 769 the surface boundary condition is modified to take into account only the non-penetrative part of the surface … … 794 794 larger depths where it contributes to local heating. 795 795 The way this second part of the solar energy penetrates into the ocean depends on which formulation is chosen. 796 In the simple 2-waveband light penetration scheme (\np{ln\_qsr\_2bd}\forcode{ =.true.})796 In the simple 2-waveband light penetration scheme (\np{ln\_qsr\_2bd}\forcode{=.true.}) 797 797 a chlorophyll-independent monochromatic formulation is chosen for the shorter wavelengths, 798 798 leading to the following expression \citep{paulson.simpson_JPO77}: … … 822 822 The 2-bands formulation does not reproduce the full model very well. 823 823 824 The RGB formulation is used when \np{ln\_qsr\_rgb}\forcode{ =.true.}.824 The RGB formulation is used when \np{ln\_qsr\_rgb}\forcode{=.true.}. 825 825 The RGB attenuation coefficients (\ie\ the inverses of the extinction length scales) are tabulated over 826 826 61 nonuniform chlorophyll classes ranging from 0.01 to 10 g.Chl/L … … 829 829 830 830 \begin{description} 831 \item[\np{nn\_chldta}\forcode{ =0}]831 \item[\np{nn\_chldta}\forcode{=0}] 832 832 a constant 0.05 g.Chl/L value everywhere ; 833 \item[\np{nn\_chldta}\forcode{ =1}]833 \item[\np{nn\_chldta}\forcode{=1}] 834 834 an observed time varying chlorophyll deduced from satellite surface ocean color measurement spread uniformly in 835 835 the vertical direction; 836 \item[\np{nn\_chldta}\forcode{ =2}]836 \item[\np{nn\_chldta}\forcode{=2}] 837 837 same as previous case except that a vertical profile of chlorophyl is used. 838 838 Following \cite{morel.berthon_LO89}, the profile is computed from the local surface chlorophyll value; 839 \item[\np{ln\_qsr\_bio}\forcode{ =.true.}]839 \item[\np{ln\_qsr\_bio}\forcode{=.true.}] 840 840 simulated time varying chlorophyll by TOP biogeochemical model. 841 841 In this case, the RGB formulation is used to calculate both the phytoplankton light limitation in … … 876 876 % Bottom Boundary Condition 877 877 % ------------------------------------------------------------------------------------------------------------- 878 \subsection[Bottom boundary condition (\textit{trabbc.F90}) - \forcode{ln_trabbc =.true.})]878 \subsection[Bottom boundary condition (\textit{trabbc.F90}) - \forcode{ln_trabbc=.true.})] 879 879 {Bottom boundary condition (\protect\mdl{trabbc})} 880 880 \label{subsec:TRA_bbc} … … 915 915 % Bottom Boundary Layer 916 916 % ================================================================ 917 \section[Bottom boundary layer (\textit{trabbl.F90} - \forcode{ln_trabbl =.true.})]918 {Bottom boundary layer (\protect\mdl{trabbl} - \protect\np{ln\_trabbl}\forcode{ =.true.})}917 \section[Bottom boundary layer (\textit{trabbl.F90} - \forcode{ln_trabbl=.true.})] 918 {Bottom boundary layer (\protect\mdl{trabbl} - \protect\np{ln\_trabbl}\forcode{=.true.})} 919 919 \label{sec:TRA_bbl} 920 920 %--------------------------------------------nambbl--------------------------------------------------------- … … 948 948 % Diffusive BBL 949 949 % ------------------------------------------------------------------------------------------------------------- 950 \subsection[Diffusive bottom boundary layer (\forcode{nn_bbl_ldf =1})]951 {Diffusive bottom boundary layer (\protect\np{nn\_bbl\_ldf}\forcode{ =1})}950 \subsection[Diffusive bottom boundary layer (\forcode{nn_bbl_ldf=1})] 951 {Diffusive bottom boundary layer (\protect\np{nn\_bbl\_ldf}\forcode{=1})} 952 952 \label{subsec:TRA_bbl_diff} 953 953 954 When applying sigma-diffusion (\np{ln\_trabbl}\forcode{ =.true.} and \np{nn\_bbl\_ldf} set to 1),954 When applying sigma-diffusion (\np{ln\_trabbl}\forcode{=.true.} and \np{nn\_bbl\_ldf} set to 1), 955 955 the diffusive flux between two adjacent cells at the ocean floor is given by 956 956 \[ … … 988 988 % Advective BBL 989 989 % ------------------------------------------------------------------------------------------------------------- 990 \subsection[Advective bottom boundary layer (\forcode{nn_bbl_adv =[12]})]991 {Advective bottom boundary layer (\protect\np{nn\_bbl\_adv}\forcode{ =[12]})}990 \subsection[Advective bottom boundary layer (\forcode{nn_bbl_adv=[12]})] 991 {Advective bottom boundary layer (\protect\np{nn\_bbl\_adv}\forcode{=[12]})} 992 992 \label{subsec:TRA_bbl_adv} 993 993 … … 1020 1020 %%%gmcomment : this section has to be really written 1021 1021 1022 When applying an advective BBL (\np{nn\_bbl\_adv}\forcode{ =1..2}), an overturning circulation is added which1022 When applying an advective BBL (\np{nn\_bbl\_adv}\forcode{=1..2}), an overturning circulation is added which 1023 1023 connects two adjacent bottom grid-points only if dense water overlies less dense water on the slope. 1024 1024 The density difference causes dense water to move down the slope. 1025 1025 1026 \np{nn\_bbl\_adv}\forcode{ =1}:1026 \np{nn\_bbl\_adv}\forcode{=1}: 1027 1027 the downslope velocity is chosen to be the Eulerian ocean velocity just above the topographic step 1028 1028 (see black arrow in \autoref{fig:bbl}) \citep{beckmann.doscher_JPO97}. … … 1031 1031 if the velocity is directed towards greater depth (\ie\ $\vect U \cdot \nabla H > 0$). 1032 1032 1033 \np{nn\_bbl\_adv}\forcode{ =2}:1033 \np{nn\_bbl\_adv}\forcode{=2}: 1034 1034 the downslope velocity is chosen to be proportional to $\Delta \rho$, 1035 1035 the density difference between the higher cell and lower cell densities \citep{campin.goosse_T99}. … … 1159 1159 (\ie\ fluxes plus content in mass exchanges). 1160 1160 $\gamma$ is initialized as \np{rn\_atfp} (\textbf{namelist} parameter). 1161 Its default value is \np{rn\_atfp}\forcode{ =10.e-3}.1161 Its default value is \np{rn\_atfp}\forcode{=10.e-3}. 1162 1162 Note that the forcing correction term in the filter is not applied in linear free surface 1163 (\jp{ln\_linssh}\forcode{ =.true.}) (see \autoref{subsec:TRA_sbc}).1163 (\jp{ln\_linssh}\forcode{=.true.}) (see \autoref{subsec:TRA_sbc}). 1164 1164 Not also that in constant volume case, the time stepping is performed on $T$, not on its content, $e_{3t}T$. 1165 1165 … … 1220 1220 1221 1221 \begin{description} 1222 \item[\np{ln\_teos10}\forcode{ =.true.}]1222 \item[\np{ln\_teos10}\forcode{=.true.}] 1223 1223 the polyTEOS10-bsq equation of seawater \citep{roquet.madec.ea_OM15} is used. 1224 1224 The accuracy of this approximation is comparable to the TEOS-10 rational function approximation, … … 1239 1239 either computing the air-sea and ice-sea fluxes (forced mode) or 1240 1240 sending the SST field to the atmosphere (coupled mode). 1241 \item[\np{ln\_eos80}\forcode{ =.true.}]1241 \item[\np{ln\_eos80}\forcode{=.true.}] 1242 1242 the polyEOS80-bsq equation of seawater is used. 1243 1243 It takes the same polynomial form as the polyTEOS10, but the coefficients have been optimized to … … 1251 1251 Nevertheless, a severe assumption is made in order to have a heat content ($C_p T_p$) which 1252 1252 is conserved by the model: $C_p$ is set to a constant value, the TEOS10 value. 1253 \item[\np{ln\_seos}\forcode{ =.true.}]1253 \item[\np{ln\_seos}\forcode{=.true.}] 1254 1254 a simplified EOS (S-EOS) inspired by \citet{vallis_bk06} is chosen, 1255 1255 the coefficients of which has been optimized to fit the behavior of TEOS10 … … 1376 1376 I've changed "derivative" to "difference" and "mean" to "average"} 1377 1377 1378 With partial cells (\np{ln\_zps}\forcode{ = .true.}) at bottom and top (\np{ln\_isfcav}\forcode{ =.true.}),1378 With partial cells (\np{ln\_zps}\forcode{=.true.}) at bottom and top (\np{ln\_isfcav}\forcode{=.true.}), 1379 1379 in general, tracers in horizontally adjacent cells live at different depths. 1380 1380 Horizontal gradients of tracers are needed for horizontal diffusion (\mdl{traldf} module) and 1381 1381 the hydrostatic pressure gradient calculations (\mdl{dynhpg} module). 1382 The partial cell properties at the top (\np{ln\_isfcav}\forcode{ =.true.}) are computed in the same way as1382 The partial cell properties at the top (\np{ln\_isfcav}\forcode{=.true.}) are computed in the same way as 1383 1383 for the bottom. 1384 1384 So, only the bottom interpolation is explained below. … … 1396 1396 \protect\label{fig:Partial_step_scheme} 1397 1397 Discretisation of the horizontal difference and average of tracers in the $z$-partial step coordinate 1398 (\protect\np{ln\_zps}\forcode{ =.true.}) in the case $(e3w_k^{i + 1} - e3w_k^i) > 0$.1398 (\protect\np{ln\_zps}\forcode{=.true.}) in the case $(e3w_k^{i + 1} - e3w_k^i) > 0$. 1399 1399 A linear interpolation is used to estimate $\widetilde T_k^{i + 1}$, 1400 1400 the tracer value at the depth of the shallower tracer point of the two adjacent bottom $T$-points.
Note: See TracChangeset
for help on using the changeset viewer.
