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NEMO/branches/2019/fix_vvl_ticket1791/doc/latex/NEMO/subfiles/chap_TRA.tex
r10544 r11422 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 % ================================================================ 60 60 % Tracer Advection 61 61 % ================================================================ 62 \section{Tracer advection (\protect\mdl{traadv})} 62 \section[Tracer advection (\textit{traadv.F90})] 63 {Tracer advection (\protect\mdl{traadv})} 63 64 \label{sec:TRA_adv} 64 65 %------------------------------------------namtra_adv----------------------------------------------------- … … 81 82 Indeed, it is obtained by using the following equality: $\nabla \cdot (\vect U \, T) = \vect U \cdot \nabla T$ which 82 83 results from the use of the continuity equation, $\partial_t e_3 + e_3 \; \nabla \cdot \vect U = 0$ 83 (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.}). 84 85 Therefore it is of paramount importance to design the discrete analogue of the advection tendency so that 85 86 it is consistent with the continuity equation in order to enforce the conservation properties of … … 90 91 \begin{figure}[!t] 91 92 \begin{center} 92 \includegraphics[ ]{Fig_adv_scheme}93 \includegraphics[width=\textwidth]{Fig_adv_scheme} 93 94 \caption{ 94 95 \protect\label{fig:adv_scheme} … … 119 120 \begin{description} 120 121 \item[linear free surface:] 121 (\np{ln\_linssh} ~\forcode{= .true.})122 (\np{ln\_linssh}\forcode{ = .true.}) 122 123 the first level thickness is constant in time: 123 124 the vertical boundary condition is applied at the fixed surface $z = 0$ rather than on … … 127 128 the first level tracer value. 128 129 \item[non-linear free surface:] 129 (\np{ln\_linssh} ~\forcode{= .false.})130 (\np{ln\_linssh}\forcode{ = .false.}) 130 131 convergence/divergence in the first ocean level moves the free surface up/down. 131 132 There is no tracer advection through it so that the advective fluxes through the surface are also zero. … … 136 137 Nevertheless, in the latter case, it is achieved to a good approximation since 137 138 the non-conservative term is the product of the time derivative of the tracer and the free surface height, 138 two quantities that are not correlated \citep{ Roullet_Madec_JGR00, Griffies_al_MWR01, Campin2004}.139 140 The velocity field that appears in (\autoref{eq:tra_adv} and \autoref{eq:tra_adv_zco }) is139 two quantities that are not correlated \citep{roullet.madec_JGR00, griffies.pacanowski.ea_MWR01, campin.adcroft.ea_OM04}. 140 141 The velocity field that appears in (\autoref{eq:tra_adv} and \autoref{eq:tra_adv_zco?}) is 141 142 the centred (\textit{now}) \textit{effective} ocean velocity, \ie the \textit{eulerian} velocity 142 143 (see \autoref{chap:DYN}) plus the eddy induced velocity (\textit{eiv}) and/or … … 183 184 % 2nd and 4th order centred schemes 184 185 % ------------------------------------------------------------------------------------------------------------- 185 \subsection{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.})} 186 188 \label{subsec:TRA_adv_cen} 187 189 188 190 % 2nd order centred scheme 189 191 190 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.}. 191 193 Its order ($2^{nd}$ or $4^{th}$) can be chosen independently on horizontal (iso-level) and vertical direction by 192 194 setting \np{nn\_cen\_h} and \np{nn\_cen\_v} to $2$ or $4$. … … 220 222 \tau_u^{cen4} = \overline{T - \frac{1}{6} \, \delta_i \Big[ \delta_{i + 1/2}[T] \, \Big]}^{\,i + 1/2} 221 223 \end{equation} 222 In the vertical direction (\np{nn\_cen\_v} ~\forcode{= 4}),223 a $4^{th}$ COMPACT interpolation has been prefered \citep{ Demange_PhD2014}.224 In the vertical direction (\np{nn\_cen\_v}\forcode{ = 4}), 225 a $4^{th}$ COMPACT interpolation has been prefered \citep{demange_phd14}. 224 226 In the COMPACT scheme, both the field and its derivative are interpolated, which leads, after a matrix inversion, 225 spectral characteristics similar to schemes of higher order \citep{ Lele_JCP1992}.227 spectral characteristics similar to schemes of higher order \citep{lele_JCP92}. 226 228 227 229 Strictly speaking, the CEN4 scheme is not a $4^{th}$ order advection scheme but … … 250 252 % FCT scheme 251 253 % ------------------------------------------------------------------------------------------------------------- 252 \subsection{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.})} 253 256 \label{subsec:TRA_adv_tvd} 254 257 255 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.}. 256 259 Its order ($2^{nd}$ or $4^{th}$) can be chosen independently on horizontal (iso-level) and vertical direction by 257 260 setting \np{nn\_fct\_h} and \np{nn\_fct\_v} to $2$ or $4$. … … 277 280 (\ie it depends on the setting of \np{nn\_fct\_h} and \np{nn\_fct\_v}). 278 281 There exist many ways to define $c_u$, each corresponding to a different FCT scheme. 279 The one chosen in \NEMO is described in \citet{ Zalesak_JCP79}.282 The one chosen in \NEMO is described in \citet{zalesak_JCP79}. 280 283 $c_u$ only departs from $1$ when the advective term produces a local extremum in the tracer field. 281 284 The resulting scheme is quite expensive but \textit{positive}. 282 285 It can be used on both active and passive tracers. 283 A comparison of FCT-2 with MUSCL and a MPDATA scheme can be found in \citet{ Levy_al_GRL01}.286 A comparison of FCT-2 with MUSCL and a MPDATA scheme can be found in \citet{levy.estublier.ea_GRL01}. 284 287 285 288 An additional option has been added controlled by \np{nn\_fct\_zts}. … … 287 290 a $2^{nd}$ order FCT scheme is used on both horizontal and vertical direction, but on the latter, 288 291 a split-explicit time stepping is used, with a number of sub-timestep equals to \np{nn\_fct\_zts}. 289 This option can be useful when the size of the timestep is limited by vertical advection \citep{ Lemarie_OM2015}.292 This option can be useful when the size of the timestep is limited by vertical advection \citep{lemarie.debreu.ea_OM15}. 290 293 Note that in this case, a similar split-explicit time stepping should be used on vertical advection of momentum to 291 294 insure a better stability (see \autoref{subsec:DYN_zad}). … … 300 303 % MUSCL scheme 301 304 % ------------------------------------------------------------------------------------------------------------- 302 \subsection{MUSCL: Monotone Upstream Scheme for Conservative Laws (\protect\np{ln\_traadv\_mus}~\forcode{= .true.})} 305 \subsection[MUSCL: Monotone Upstream Scheme for Conservative Laws (\forcode{ln_traadv_mus = .true.})] 306 {MUSCL: Monotone Upstream Scheme for Conservative Laws (\protect\np{ln\_traadv\_mus}\forcode{ = .true.})} 303 307 \label{subsec:TRA_adv_mus} 304 308 305 The Monotone Upstream Scheme for Conservative Laws (MUSCL) is used when \np{ln\_traadv\_mus} ~\forcode{= .true.}.309 The Monotone Upstream Scheme for Conservative Laws (MUSCL) is used when \np{ln\_traadv\_mus}\forcode{ = .true.}. 306 310 MUSCL implementation can be found in the \mdl{traadv\_mus} module. 307 311 308 MUSCL has been first implemented in \NEMO by \citet{ Levy_al_GRL01}.312 MUSCL has been first implemented in \NEMO by \citet{levy.estublier.ea_GRL01}. 309 313 In its formulation, the tracer at velocity points is evaluated assuming a linear tracer variation between 310 314 two $T$-points (\autoref{fig:adv_scheme}). … … 331 335 This choice ensure the \textit{positive} character of the scheme. 332 336 In addition, fluxes round a grid-point where a runoff is applied can optionally be computed using upstream fluxes 333 (\np{ln\_mus\_ups} ~\forcode{= .true.}).337 (\np{ln\_mus\_ups}\forcode{ = .true.}). 334 338 335 339 % ------------------------------------------------------------------------------------------------------------- 336 340 % UBS scheme 337 341 % ------------------------------------------------------------------------------------------------------------- 338 \subsection{UBS a.k.a. UP3: Upstream-Biased Scheme (\protect\np{ln\_traadv\_ubs}~\forcode{= .true.})} 342 \subsection[UBS a.k.a. UP3: Upstream-Biased Scheme (\forcode{ln_traadv_ubs = .true.})] 343 {UBS a.k.a. UP3: Upstream-Biased Scheme (\protect\np{ln\_traadv\_ubs}\forcode{ = .true.})} 339 344 \label{subsec:TRA_adv_ubs} 340 345 341 The Upstream-Biased Scheme (UBS) is used when \np{ln\_traadv\_ubs} ~\forcode{= .true.}.346 The Upstream-Biased Scheme (UBS) is used when \np{ln\_traadv\_ubs}\forcode{ = .true.}. 342 347 UBS implementation can be found in the \mdl{traadv\_mus} module. 343 348 … … 358 363 359 364 This results in a dissipatively dominant (i.e. hyper-diffusive) truncation error 360 \citep{ Shchepetkin_McWilliams_OM05}.361 The overall performance of the advection scheme is similar to that reported in \cite{ Farrow1995}.365 \citep{shchepetkin.mcwilliams_OM05}. 366 The overall performance of the advection scheme is similar to that reported in \cite{farrow.stevens_JPO95}. 362 367 It is a relatively good compromise between accuracy and smoothness. 363 368 Nevertheless the scheme is not \textit{positive}, meaning that false extrema are permitted, … … 367 372 The intrinsic diffusion of UBS makes its use risky in the vertical direction where 368 373 the control of artificial diapycnal fluxes is of paramount importance 369 \citep{ Shchepetkin_McWilliams_OM05, Demange_PhD2014}.374 \citep{shchepetkin.mcwilliams_OM05, demange_phd14}. 370 375 Therefore the vertical flux is evaluated using either a $2^nd$ order FCT scheme or a $4^th$ order COMPACT scheme 371 (\np{nn\_cen\_v} ~\forcode{= 2 or 4}).376 (\np{nn\_cen\_v}\forcode{ = 2 or 4}). 372 377 373 378 For stability reasons (see \autoref{chap:STP}), the first term in \autoref{eq:tra_adv_ubs} … … 376 381 (which is the diffusive part of the scheme), 377 382 is evaluated using the \textit{before} tracer (forward in time). 378 This choice is discussed by \citet{ Webb_al_JAOT98} in the context of the QUICK advection scheme.383 This choice is discussed by \citet{webb.de-cuevas.ea_JAOT98} in the context of the QUICK advection scheme. 379 384 UBS and QUICK schemes only differ by one coefficient. 380 Replacing 1/6 with 1/8 in \autoref{eq:tra_adv_ubs} leads to the QUICK advection scheme \citep{ Webb_al_JAOT98}.385 Replacing 1/6 with 1/8 in \autoref{eq:tra_adv_ubs} leads to the QUICK advection scheme \citep{webb.de-cuevas.ea_JAOT98}. 381 386 This option is not available through a namelist parameter, since the 1/6 coefficient is hard coded. 382 387 Nevertheless it is quite easy to make the substitution in the \mdl{traadv\_ubs} module and obtain a QUICK scheme. … … 408 413 % QCK scheme 409 414 % ------------------------------------------------------------------------------------------------------------- 410 \subsection{QCK: QuiCKest scheme (\protect\np{ln\_traadv\_qck}~\forcode{= .true.})} 415 \subsection[QCK: QuiCKest scheme (\forcode{ln_traadv_qck = .true.})] 416 {QCK: QuiCKest scheme (\protect\np{ln\_traadv\_qck}\forcode{ = .true.})} 411 417 \label{subsec:TRA_adv_qck} 412 418 413 419 The Quadratic Upstream Interpolation for Convective Kinematics with Estimated Streaming Terms (QUICKEST) scheme 414 proposed by \citet{ Leonard1979} is used when \np{ln\_traadv\_qck}~\forcode{= .true.}.420 proposed by \citet{leonard_CMAME79} is used when \np{ln\_traadv\_qck}\forcode{ = .true.}. 415 421 QUICKEST implementation can be found in the \mdl{traadv\_qck} module. 416 422 417 423 QUICKEST is the third order Godunov scheme which is associated with the ULTIMATE QUICKEST limiter 418 \citep{ Leonard1991}.424 \citep{leonard_CMAME91}. 419 425 It has been implemented in NEMO by G. Reffray (MERCATOR-ocean) and can be found in the \mdl{traadv\_qck} module. 420 426 The resulting scheme is quite expensive but \textit{positive}. … … 431 437 % Tracer Lateral Diffusion 432 438 % ================================================================ 433 \section{Tracer lateral diffusion (\protect\mdl{traldf})} 439 \section[Tracer lateral diffusion (\textit{traldf.F90})] 440 {Tracer lateral diffusion (\protect\mdl{traldf})} 434 441 \label{sec:TRA_ldf} 435 442 %-----------------------------------------nam_traldf------------------------------------------------------ … … 453 460 except for the pure vertical component that appears when a rotation tensor is used. 454 461 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 which456 the pure vertical component is split into an explicit and an implicit part \citep{ Lemarie_OM2012}.462 When \np{ln\_traldf\_msc}\forcode{ = .true.}, a Method of Stabilizing Correction is used in which 463 the pure vertical component is split into an explicit and an implicit part \citep{lemarie.debreu.ea_OM12}. 457 464 458 465 % ------------------------------------------------------------------------------------------------------------- 459 466 % Type of operator 460 467 % ------------------------------------------------------------------------------------------------------------- 461 \subsection[Type of operator (\protect\np{ln\_traldf}\{\_NONE,\_lap,\_blp\}\})]{Type of operator (\protect\np{ln\_traldf\_NONE}, \protect\np{ln\_traldf\_lap}, or \protect\np{ln\_traldf\_blp}) } 468 \subsection[Type of operator (\texttt{ln\_traldf}\{\texttt{\_NONE,\_lap,\_blp}\})] 469 {Type of operator (\protect\np{ln\_traldf\_NONE}, \protect\np{ln\_traldf\_lap}, or \protect\np{ln\_traldf\_blp}) } 462 470 \label{subsec:TRA_ldf_op} 463 471 … … 465 473 466 474 \begin{description} 467 \item[\np{ln\_traldf\_NONE} ~\forcode{= .true.}:]475 \item[\np{ln\_traldf\_NONE}\forcode{ = .true.}:] 468 476 no operator selected, the lateral diffusive tendency will not be applied to the tracer equation. 469 477 This option can be used when the selected advection scheme is diffusive enough (MUSCL scheme for example). 470 \item[\np{ln\_traldf\_lap} ~\forcode{= .true.}:]478 \item[\np{ln\_traldf\_lap}\forcode{ = .true.}:] 471 479 a laplacian operator is selected. 472 480 This harmonic operator takes the following expression: $\mathpzc{L}(T) = \nabla \cdot A_{ht} \; \nabla T $, 473 481 where the gradient operates along the selected direction (see \autoref{subsec:TRA_ldf_dir}), 474 482 and $A_{ht}$ is the eddy diffusivity coefficient expressed in $m^2/s$ (see \autoref{chap:LDF}). 475 \item[\np{ln\_traldf\_blp} ~\forcode{= .true.}]:483 \item[\np{ln\_traldf\_blp}\forcode{ = .true.}]: 476 484 a bilaplacian operator is selected. 477 485 This biharmonic operator takes the following expression: … … 493 501 % Direction of action 494 502 % ------------------------------------------------------------------------------------------------------------- 495 \subsection[Action direction (\protect\np{ln\_traldf}\{\_lev,\_hor,\_iso,\_triad\})]{Direction of action (\protect\np{ln\_traldf\_lev}, \protect\np{ln\_traldf\_hor}, \protect\np{ln\_traldf\_iso}, or \protect\np{ln\_traldf\_triad}) } 503 \subsection[Action direction (\texttt{ln\_traldf}\{\texttt{\_lev,\_hor,\_iso,\_triad}\})] 504 {Direction of action (\protect\np{ln\_traldf\_lev}, \protect\np{ln\_traldf\_hor}, \protect\np{ln\_traldf\_iso}, or \protect\np{ln\_traldf\_triad}) } 496 505 \label{subsec:TRA_ldf_dir} 497 506 498 507 The choice of a direction of action determines the form of operator used. 499 508 The operator is a simple (re-entrant) laplacian acting in the (\textbf{i},\textbf{j}) plane when 500 iso-level option is used (\np{ln\_traldf\_lev} ~\forcode{= .true.}) or509 iso-level option is used (\np{ln\_traldf\_lev}\forcode{ = .true.}) or 501 510 when a horizontal (\ie geopotential) operator is demanded in \textit{z}-coordinate 502 511 (\np{ln\_traldf\_hor} and \np{ln\_zco} equal \forcode{.true.}). … … 519 528 % iso-level operator 520 529 % ------------------------------------------------------------------------------------------------------------- 521 \subsection{Iso-level (bi -)laplacian operator ( \protect\np{ln\_traldf\_iso}) } 530 \subsection[Iso-level (bi-)laplacian operator (\texttt{ln\_traldf\_iso})] 531 {Iso-level (bi-)laplacian operator ( \protect\np{ln\_traldf\_iso})} 522 532 \label{subsec:TRA_ldf_lev} 523 533 … … 537 547 It is a \textit{horizontal} operator (\ie acting along geopotential surfaces) in 538 548 the $z$-coordinate with or without partial steps, but is simply an iso-level operator in the $s$-coordinate. 539 It is thus used when, in addition to \np{ln\_traldf\_lap} or \np{ln\_traldf\_blp} ~\forcode{= .true.},540 we have \np{ln\_traldf\_lev} ~\forcode{= .true.} or \np{ln\_traldf\_hor}~=~\np{ln\_zco}~\forcode{= .true.}.549 It is thus used when, in addition to \np{ln\_traldf\_lap} or \np{ln\_traldf\_blp}\forcode{ = .true.}, 550 we have \np{ln\_traldf\_lev}\forcode{ = .true.} or \np{ln\_traldf\_hor}~=~\np{ln\_zco}\forcode{ = .true.}. 541 551 In both cases, it significantly contributes to diapycnal mixing. 542 552 It is therefore never recommended, even when using it in the bilaplacian case. 543 553 544 Note that in the partial step $z$-coordinate (\np{ln\_zps} ~\forcode{= .true.}),554 Note that in the partial step $z$-coordinate (\np{ln\_zps}\forcode{ = .true.}), 545 555 tracers in horizontally adjacent cells are located at different depths in the vicinity of the bottom. 546 556 In this case, horizontal derivatives in (\autoref{eq:tra_ldf_lap}) at the bottom level require a specific treatment. … … 550 560 % Rotated laplacian operator 551 561 % ------------------------------------------------------------------------------------------------------------- 552 \subsection{Standard and triad (bi 562 \subsection{Standard and triad (bi-)laplacian operator} 553 563 \label{subsec:TRA_ldf_iso_triad} 554 564 555 %&& Standard rotated (bi 565 %&& Standard rotated (bi-)laplacian operator 556 566 %&& ---------------------------------------------- 557 \subsubsection{Standard rotated (bi -)laplacian operator (\protect\mdl{traldf\_iso})} 567 \subsubsection[Standard rotated (bi-)laplacian operator (\textit{traldf\_iso.F90})] 568 {Standard rotated (bi-)laplacian operator (\protect\mdl{traldf\_iso})} 558 569 \label{subsec:TRA_ldf_iso} 559 570 The general form of the second order lateral tracer subgrid scale physics (\autoref{eq:PE_zdf}) … … 574 585 $r_1$ and $r_2$ are the slopes between the surface of computation ($z$- or $s$-surfaces) and 575 586 the surface along which the diffusion operator acts (\ie horizontal or iso-neutral surfaces). 576 It is thus used when, in addition to \np{ln\_traldf\_lap} ~\forcode{= .true.},577 we have \np{ln\_traldf\_iso} ~\forcode{= .true.},578 or both \np{ln\_traldf\_hor} ~\forcode{= .true.} and \np{ln\_zco}~\forcode{= .true.}.587 It is thus used when, in addition to \np{ln\_traldf\_lap}\forcode{ = .true.}, 588 we have \np{ln\_traldf\_iso}\forcode{ = .true.}, 589 or both \np{ln\_traldf\_hor}\forcode{ = .true.} and \np{ln\_zco}\forcode{ = .true.}. 579 590 The way these slopes are evaluated is given in \autoref{sec:LDF_slp}. 580 591 At the surface, bottom and lateral boundaries, the turbulent fluxes of heat and salt are set to zero using … … 590 601 This formulation conserves the tracer but does not ensure the decrease of the tracer variance. 591 602 Nevertheless the treatment performed on the slopes (see \autoref{chap:LDF}) allows the model to run safely without 592 any additional background horizontal diffusion \citep{ Guilyardi_al_CD01}.593 594 Note that in the partial step $z$-coordinate (\np{ln\_zps} ~\forcode{= .true.}),603 any additional background horizontal diffusion \citep{guilyardi.madec.ea_CD01}. 604 605 Note that in the partial step $z$-coordinate (\np{ln\_zps}\forcode{ = .true.}), 595 606 the horizontal derivatives at the bottom level in \autoref{eq:tra_ldf_iso} require a specific treatment. 596 607 They are calculated in module zpshde, described in \autoref{sec:TRA_zpshde}. 597 608 598 %&& Triad rotated (bi 609 %&& Triad rotated (bi-)laplacian operator 599 610 %&& ------------------------------------------- 600 \subsubsection{Triad rotated (bi -)laplacian operator (\protect\np{ln\_traldf\_triad})} 611 \subsubsection[Triad rotated (bi-)laplacian operator (\textit{ln\_traldf\_triad})] 612 {Triad rotated (bi-)laplacian operator (\protect\np{ln\_traldf\_triad})} 601 613 \label{subsec:TRA_ldf_triad} 602 614 603 If the Griffies triad scheme is employed (\np{ln\_traldf\_triad} ~\forcode{= .true.}; see \autoref{apdx:triad})604 605 An alternative scheme developed by \cite{ Griffies_al_JPO98} which ensures tracer variance decreases606 is also available in \NEMO (\np{ln\_traldf\_grif} ~\forcode{= .true.}).615 If the Griffies triad scheme is employed (\np{ln\_traldf\_triad}\forcode{ = .true.}; see \autoref{apdx:triad}) 616 617 An alternative scheme developed by \cite{griffies.gnanadesikan.ea_JPO98} which ensures tracer variance decreases 618 is also available in \NEMO (\np{ln\_traldf\_grif}\forcode{ = .true.}). 607 619 A complete description of the algorithm is given in \autoref{apdx:triad}. 608 620 … … 632 644 % Tracer Vertical Diffusion 633 645 % ================================================================ 634 \section{Tracer vertical diffusion (\protect\mdl{trazdf})} 646 \section[Tracer vertical diffusion (\textit{trazdf.F90})] 647 {Tracer vertical diffusion (\protect\mdl{trazdf})} 635 648 \label{sec:TRA_zdf} 636 649 %--------------------------------------------namzdf--------------------------------------------------------- … … 663 676 664 677 The large eddy coefficient found in the mixed layer together with high vertical resolution implies that 665 in the case of explicit time stepping (\np{ln\_zdfexp} ~\forcode{= .true.})678 in the case of explicit time stepping (\np{ln\_zdfexp}\forcode{ = .true.}) 666 679 there would be too restrictive a constraint on the time step. 667 680 Therefore, the default implicit time stepping is preferred for the vertical diffusion since 668 681 it overcomes the stability constraint. 669 A forward time differencing scheme (\np{ln\_zdfexp} ~\forcode{= .true.}) using682 A forward time differencing scheme (\np{ln\_zdfexp}\forcode{ = .true.}) using 670 683 a time splitting technique (\np{nn\_zdfexp} $> 1$) is provided as an alternative. 671 684 Namelist variables \np{ln\_zdfexp} and \np{nn\_zdfexp} apply to both tracers and dynamics. … … 680 693 % surface boundary condition 681 694 % ------------------------------------------------------------------------------------------------------------- 682 \subsection{Surface boundary condition (\protect\mdl{trasbc})} 695 \subsection[Surface boundary condition (\textit{trasbc.F90})] 696 {Surface boundary condition (\protect\mdl{trasbc})} 683 697 \label{subsec:TRA_sbc} 684 698 … … 730 744 Such time averaging prevents the divergence of odd and even time step (see \autoref{chap:STP}). 731 745 732 In the linear free surface case (\np{ln\_linssh} ~\forcode{= .true.}), an additional term has to be added on746 In the linear free surface case (\np{ln\_linssh}\forcode{ = .true.}), an additional term has to be added on 733 747 both temperature and salinity. 734 748 On temperature, this term remove the heat content associated with mass exchange that has been added to $Q_{ns}$. … … 747 761 Note that an exact conservation of heat and salt content is only achieved with non-linear free surface. 748 762 In the linear free surface case, there is a small imbalance. 749 The imbalance is larger than the imbalance associated with the Asselin time filter \citep{ Leclair_Madec_OM09}.763 The imbalance is larger than the imbalance associated with the Asselin time filter \citep{leclair.madec_OM09}. 750 764 This is the reason why the modified filter is not applied in the linear free surface case (see \autoref{chap:STP}). 751 765 … … 753 767 % Solar Radiation Penetration 754 768 % ------------------------------------------------------------------------------------------------------------- 755 \subsection{Solar radiation penetration (\protect\mdl{traqsr})} 769 \subsection[Solar radiation penetration (\textit{traqsr.F90})] 770 {Solar radiation penetration (\protect\mdl{traqsr})} 756 771 \label{subsec:TRA_qsr} 757 772 %--------------------------------------------namqsr-------------------------------------------------------- … … 761 776 762 777 Options are defined through the \ngn{namtra\_qsr} namelist variables. 763 When the penetrative solar radiation option is used (\np{ln\_flxqsr} ~\forcode{= .true.}),778 When the penetrative solar radiation option is used (\np{ln\_flxqsr}\forcode{ = .true.}), 764 779 the solar radiation penetrates the top few tens of meters of the ocean. 765 If it is not used (\np{ln\_flxqsr} ~\forcode{= .false.}) all the heat flux is absorbed in the first ocean level.780 If it is not used (\np{ln\_flxqsr}\forcode{ = .false.}) all the heat flux is absorbed in the first ocean level. 766 781 Thus, in the former case a term is added to the time evolution equation of temperature \autoref{eq:PE_tra_T} and 767 782 the surface boundary condition is modified to take into account only the non-penetrative part of the surface … … 792 807 larger depths where it contributes to local heating. 793 808 The way this second part of the solar energy penetrates into the ocean depends on which formulation is chosen. 794 In the simple 2-waveband light penetration scheme (\np{ln\_qsr\_2bd} ~\forcode{= .true.})809 In the simple 2-waveband light penetration scheme (\np{ln\_qsr\_2bd}\forcode{ = .true.}) 795 810 a chlorophyll-independent monochromatic formulation is chosen for the shorter wavelengths, 796 leading to the following expression \citep{ Paulson1977}:811 leading to the following expression \citep{paulson.simpson_JPO77}: 797 812 \[ 798 813 % \label{eq:traqsr_iradiance} … … 805 820 806 821 Such assumptions have been shown to provide a very crude and simplistic representation of 807 observed light penetration profiles (\cite{ Morel_JGR88}, see also \autoref{fig:traqsr_irradiance}).822 observed light penetration profiles (\cite{morel_JGR88}, see also \autoref{fig:traqsr_irradiance}). 808 823 Light absorption in the ocean depends on particle concentration and is spectrally selective. 809 \cite{ Morel_JGR88} has shown that an accurate representation of light penetration can be provided by824 \cite{morel_JGR88} has shown that an accurate representation of light penetration can be provided by 810 825 a 61 waveband formulation. 811 826 Unfortunately, such a model is very computationally expensive. 812 Thus, \cite{ Lengaigne_al_CD07} have constructed a simplified version of this formulation in which827 Thus, \cite{lengaigne.menkes.ea_CD07} have constructed a simplified version of this formulation in which 813 828 visible light is split into three wavebands: blue (400-500 nm), green (500-600 nm) and red (600-700nm). 814 829 For each wave-band, the chlorophyll-dependent attenuation coefficient is fitted to the coefficients computed from 815 the full spectral model of \cite{ Morel_JGR88} (as modified by \cite{Morel_Maritorena_JGR01}),830 the full spectral model of \cite{morel_JGR88} (as modified by \cite{morel.maritorena_JGR01}), 816 831 assuming the same power-law relationship. 817 832 As shown in \autoref{fig:traqsr_irradiance}, this formulation, called RGB (Red-Green-Blue), … … 820 835 The 2-bands formulation does not reproduce the full model very well. 821 836 822 The RGB formulation is used when \np{ln\_qsr\_rgb} ~\forcode{= .true.}.837 The RGB formulation is used when \np{ln\_qsr\_rgb}\forcode{ = .true.}. 823 838 The RGB attenuation coefficients (\ie the inverses of the extinction length scales) are tabulated over 824 839 61 nonuniform chlorophyll classes ranging from 0.01 to 10 g.Chl/L … … 827 842 828 843 \begin{description} 829 \item[\np{nn\_chdta} ~\forcode{= 0}]844 \item[\np{nn\_chdta}\forcode{ = 0}] 830 845 a constant 0.05 g.Chl/L value everywhere ; 831 \item[\np{nn\_chdta} ~\forcode{= 1}]846 \item[\np{nn\_chdta}\forcode{ = 1}] 832 847 an observed time varying chlorophyll deduced from satellite surface ocean color measurement spread uniformly in 833 848 the vertical direction; 834 \item[\np{nn\_chdta} ~\forcode{= 2}]849 \item[\np{nn\_chdta}\forcode{ = 2}] 835 850 same as previous case except that a vertical profile of chlorophyl is used. 836 Following \cite{ Morel_Berthon_LO89}, the profile is computed from the local surface chlorophyll value;837 \item[\np{ln\_qsr\_bio} ~\forcode{= .true.}]851 Following \cite{morel.berthon_LO89}, the profile is computed from the local surface chlorophyll value; 852 \item[\np{ln\_qsr\_bio}\forcode{ = .true.}] 838 853 simulated time varying chlorophyll by TOP biogeochemical model. 839 854 In this case, the RGB formulation is used to calculate both the phytoplankton light limitation in … … 856 871 \begin{figure}[!t] 857 872 \begin{center} 858 \includegraphics[ ]{Fig_TRA_Irradiance}873 \includegraphics[width=\textwidth]{Fig_TRA_Irradiance} 859 874 \caption{ 860 875 \protect\label{fig:traqsr_irradiance} … … 865 880 61 waveband Morel (1988) formulation (black) for a chlorophyll concentration of 866 881 (a) Chl=0.05 mg/m$^3$ and (b) Chl=0.5 mg/m$^3$. 867 From \citet{ Lengaigne_al_CD07}.882 From \citet{lengaigne.menkes.ea_CD07}. 868 883 } 869 884 \end{center} … … 874 889 % Bottom Boundary Condition 875 890 % ------------------------------------------------------------------------------------------------------------- 876 \subsection{Bottom boundary condition (\protect\mdl{trabbc})} 891 \subsection[Bottom boundary condition (\textit{trabbc.F90})] 892 {Bottom boundary condition (\protect\mdl{trabbc})} 877 893 \label{subsec:TRA_bbc} 878 894 %--------------------------------------------nambbc-------------------------------------------------------- … … 883 899 \begin{figure}[!t] 884 900 \begin{center} 885 \includegraphics[ ]{Fig_TRA_geoth}901 \includegraphics[width=\textwidth]{Fig_TRA_geoth} 886 902 \caption{ 887 903 \protect\label{fig:geothermal} 888 Geothermal Heat flux (in $mW.m^{-2}$) used by \cite{ Emile-Geay_Madec_OS09}.889 It is inferred from the age of the sea floor and the formulae of \citet{ Stein_Stein_Nat92}.904 Geothermal Heat flux (in $mW.m^{-2}$) used by \cite{emile-geay.madec_OS09}. 905 It is inferred from the age of the sea floor and the formulae of \citet{stein.stein_N92}. 890 906 } 891 907 \end{center} … … 897 913 This is the default option in \NEMO, and it is implemented using the masking technique. 898 914 However, there is a non-zero heat flux across the seafloor that is associated with solid earth cooling. 899 This flux is weak compared to surface fluxes (a mean global value of $\sim 0.1 \, W/m^2$ \citep{ Stein_Stein_Nat92}),915 This flux is weak compared to surface fluxes (a mean global value of $\sim 0.1 \, W/m^2$ \citep{stein.stein_N92}), 900 916 but it warms systematically the ocean and acts on the densest water masses. 901 917 Taking this flux into account in a global ocean model increases the deepest overturning cell 902 (\ie the one associated with the Antarctic Bottom Water) by a few Sverdrups \citep{ Emile-Geay_Madec_OS09}.918 (\ie the one associated with the Antarctic Bottom Water) by a few Sverdrups \citep{emile-geay.madec_OS09}. 903 919 904 920 Options are defined through the \ngn{namtra\_bbc} namelist variables. … … 907 923 the \np{nn\_geoflx\_cst}, which is also a namelist parameter. 908 924 When \np{nn\_geoflx} is set to 2, a spatially varying geothermal heat flux is introduced which is provided in 909 the \ifile{geothermal\_heating} NetCDF file (\autoref{fig:geothermal}) \citep{ Emile-Geay_Madec_OS09}.925 the \ifile{geothermal\_heating} NetCDF file (\autoref{fig:geothermal}) \citep{emile-geay.madec_OS09}. 910 926 911 927 % ================================================================ 912 928 % Bottom Boundary Layer 913 929 % ================================================================ 914 \section{Bottom boundary layer (\protect\mdl{trabbl} - \protect\key{trabbl})} 930 \section[Bottom boundary layer (\textit{trabbl.F90} - \texttt{\textbf{key\_trabbl}})] 931 {Bottom boundary layer (\protect\mdl{trabbl} - \protect\key{trabbl})} 915 932 \label{sec:TRA_bbl} 916 933 %--------------------------------------------nambbl--------------------------------------------------------- … … 931 948 sometimes over a thickness much larger than the thickness of the observed gravity plume. 932 949 A similar problem occurs in the $s$-coordinate when the thickness of the bottom level varies rapidly downstream of 933 a sill \citep{ Willebrand_al_PO01}, and the thickness of the plume is not resolved.934 935 The idea of the bottom boundary layer (BBL) parameterisation, first introduced by \citet{ Beckmann_Doscher1997},950 a sill \citep{willebrand.barnier.ea_PO01}, and the thickness of the plume is not resolved. 951 952 The idea of the bottom boundary layer (BBL) parameterisation, first introduced by \citet{beckmann.doscher_JPO97}, 936 953 is to allow a direct communication between two adjacent bottom cells at different levels, 937 954 whenever the densest water is located above the less dense water. … … 939 956 In the current implementation of the BBL, only the tracers are modified, not the velocities. 940 957 Furthermore, it only connects ocean bottom cells, and therefore does not include all the improvements introduced by 941 \citet{ Campin_Goosse_Tel99}.958 \citet{campin.goosse_T99}. 942 959 943 960 % ------------------------------------------------------------------------------------------------------------- 944 961 % Diffusive BBL 945 962 % ------------------------------------------------------------------------------------------------------------- 946 \subsection{Diffusive bottom boundary layer (\protect\np{nn\_bbl\_ldf}~\forcode{= 1})} 963 \subsection[Diffusive bottom boundary layer (\forcode{nn_bbl_ldf = 1})] 964 {Diffusive bottom boundary layer (\protect\np{nn\_bbl\_ldf}\forcode{ = 1})} 947 965 \label{subsec:TRA_bbl_diff} 948 966 … … 955 973 with $\nabla_\sigma$ the lateral gradient operator taken between bottom cells, and 956 974 $A_l^\sigma$ the lateral diffusivity in the BBL. 957 Following \citet{ Beckmann_Doscher1997}, the latter is prescribed with a spatial dependence,975 Following \citet{beckmann.doscher_JPO97}, the latter is prescribed with a spatial dependence, 958 976 \ie in the conditional form 959 977 \begin{equation} … … 983 1001 % Advective BBL 984 1002 % ------------------------------------------------------------------------------------------------------------- 985 \subsection{Advective bottom boundary layer (\protect\np{nn\_bbl\_adv}~\forcode{= 1..2})} 1003 \subsection[Advective bottom boundary layer (\forcode{nn_bbl_adv = [12]})] 1004 {Advective bottom boundary layer (\protect\np{nn\_bbl\_adv}\forcode{ = [12]})} 986 1005 \label{subsec:TRA_bbl_adv} 987 1006 … … 994 1013 \begin{figure}[!t] 995 1014 \begin{center} 996 \includegraphics[ ]{Fig_BBL_adv}1015 \includegraphics[width=\textwidth]{Fig_BBL_adv} 997 1016 \caption{ 998 1017 \protect\label{fig:bbl} … … 1014 1033 %%%gmcomment : this section has to be really written 1015 1034 1016 When applying an advective BBL (\np{nn\_bbl\_adv} ~\forcode{= 1..2}), an overturning circulation is added which1035 When applying an advective BBL (\np{nn\_bbl\_adv}\forcode{ = 1..2}), an overturning circulation is added which 1017 1036 connects two adjacent bottom grid-points only if dense water overlies less dense water on the slope. 1018 1037 The density difference causes dense water to move down the slope. 1019 1038 1020 \np{nn\_bbl\_adv} ~\forcode{= 1}:1039 \np{nn\_bbl\_adv}\forcode{ = 1}: 1021 1040 the downslope velocity is chosen to be the Eulerian ocean velocity just above the topographic step 1022 (see black arrow in \autoref{fig:bbl}) \citep{ Beckmann_Doscher1997}.1041 (see black arrow in \autoref{fig:bbl}) \citep{beckmann.doscher_JPO97}. 1023 1042 It is a \textit{conditional advection}, that is, advection is allowed only 1024 1043 if dense water overlies less dense water on the slope (\ie $\nabla_\sigma \rho \cdot \nabla H < 0$) and 1025 1044 if the velocity is directed towards greater depth (\ie $\vect U \cdot \nabla H > 0$). 1026 1045 1027 \np{nn\_bbl\_adv} ~\forcode{= 2}:1046 \np{nn\_bbl\_adv}\forcode{ = 2}: 1028 1047 the downslope velocity is chosen to be proportional to $\Delta \rho$, 1029 the density difference between the higher cell and lower cell densities \citep{ Campin_Goosse_Tel99}.1048 the density difference between the higher cell and lower cell densities \citep{campin.goosse_T99}. 1030 1049 The advection is allowed only if dense water overlies less dense water on the slope 1031 1050 (\ie $\nabla_\sigma \rho \cdot \nabla H < 0$). … … 1041 1060 The parameter $\gamma$ should take a different value for each bathymetric step, but for simplicity, 1042 1061 and because no direct estimation of this parameter is available, a uniform value has been assumed. 1043 The possible values for $\gamma$ range between 1 and $10~s$ \citep{ Campin_Goosse_Tel99}.1062 The possible values for $\gamma$ range between 1 and $10~s$ \citep{campin.goosse_T99}. 1044 1063 1045 1064 Scalar properties are advected by this additional transport $(u^{tr}_{bbl},v^{tr}_{bbl})$ using the upwind scheme. … … 1074 1093 % Tracer damping 1075 1094 % ================================================================ 1076 \section{Tracer damping (\protect\mdl{tradmp})} 1095 \section[Tracer damping (\textit{tradmp.F90})] 1096 {Tracer damping (\protect\mdl{tradmp})} 1077 1097 \label{sec:TRA_dmp} 1078 1098 %--------------------------------------------namtra_dmp------------------------------------------------- … … 1109 1129 In the vicinity of these walls, $\gamma$ takes large values (equivalent to a time scale of a few days) whereas 1110 1130 it is zero in the interior of the model domain. 1111 The second case corresponds to the use of the robust diagnostic method \citep{ Sarmiento1982}.1131 The second case corresponds to the use of the robust diagnostic method \citep{sarmiento.bryan_JGR82}. 1112 1132 It allows us to find the velocity field consistent with the model dynamics whilst 1113 1133 having a $T$, $S$ field close to a given climatological field ($T_o$, $S_o$). … … 1121 1141 only below the mixed layer (defined either on a density or $S_o$ criterion). 1122 1142 It is common to set the damping to zero in the mixed layer as the adjustment time scale is short here 1123 \citep{ Madec_al_JPO96}.1143 \citep{madec.delecluse.ea_JPO96}. 1124 1144 1125 1145 For generating \ifile{resto}, see the documentation for the DMP tool provided with the source code under … … 1129 1149 % Tracer time evolution 1130 1150 % ================================================================ 1131 \section{Tracer time evolution (\protect\mdl{tranxt})} 1151 \section[Tracer time evolution (\textit{tranxt.F90})] 1152 {Tracer time evolution (\protect\mdl{tranxt})} 1132 1153 \label{sec:TRA_nxt} 1133 1154 %--------------------------------------------namdom----------------------------------------------------- … … 1137 1158 1138 1159 Options are defined through the \ngn{namdom} namelist variables. 1139 The general framework for tracer time stepping is a modified leap-frog scheme \citep{ Leclair_Madec_OM09},1160 The general framework for tracer time stepping is a modified leap-frog scheme \citep{leclair.madec_OM09}, 1140 1161 \ie a three level centred time scheme associated with a Asselin time filter (cf. \autoref{sec:STP_mLF}): 1141 1162 \begin{equation} … … 1151 1172 (\ie fluxes plus content in mass exchanges). 1152 1173 $\gamma$ is initialized as \np{rn\_atfp} (\textbf{namelist} parameter). 1153 Its default value is \np{rn\_atfp} ~\forcode{= 10.e-3}.1174 Its default value is \np{rn\_atfp}\forcode{ = 10.e-3}. 1154 1175 Note that the forcing correction term in the filter is not applied in linear free surface 1155 (\jp{lk\_vvl} ~\forcode{= .false.}) (see \autoref{subsec:TRA_sbc}).1176 (\jp{lk\_vvl}\forcode{ = .false.}) (see \autoref{subsec:TRA_sbc}). 1156 1177 Not also that in constant volume case, the time stepping is performed on $T$, not on its content, $e_{3t}T$. 1157 1178 … … 1166 1187 % Equation of State (eosbn2) 1167 1188 % ================================================================ 1168 \section{Equation of state (\protect\mdl{eosbn2}) } 1189 \section[Equation of state (\textit{eosbn2.F90})] 1190 {Equation of state (\protect\mdl{eosbn2})} 1169 1191 \label{sec:TRA_eosbn2} 1170 1192 %--------------------------------------------nameos----------------------------------------------------- … … 1176 1198 % Equation of State 1177 1199 % ------------------------------------------------------------------------------------------------------------- 1178 \subsection{Equation of seawater (\protect\np{nn\_eos}~\forcode{= -1..1})} 1200 \subsection[Equation of seawater (\forcode{nn_eos = {-1,1}})] 1201 {Equation of seawater (\protect\np{nn\_eos}\forcode{ = {-1,1}})} 1179 1202 \label{subsec:TRA_eos} 1180 1203 … … 1186 1209 Nonlinearities of the EOS are of major importance, in particular influencing the circulation through 1187 1210 determination of the static stability below the mixed layer, 1188 thus controlling rates of exchange between the atmosphere and the ocean interior \citep{ Roquet_JPO2015}.1189 Therefore an accurate EOS based on either the 1980 equation of state (EOS-80, \cite{ UNESCO1983}) or1190 TEOS-10 \citep{ TEOS10} standards should be used anytime a simulation of the real ocean circulation is attempted1191 \citep{ Roquet_JPO2015}.1211 thus controlling rates of exchange between the atmosphere and the ocean interior \citep{roquet.madec.ea_JPO15}. 1212 Therefore an accurate EOS based on either the 1980 equation of state (EOS-80, \cite{fofonoff.millard_bk83}) or 1213 TEOS-10 \citep{ioc.iapso_bk10} standards should be used anytime a simulation of the real ocean circulation is attempted 1214 \citep{roquet.madec.ea_JPO15}. 1192 1215 The use of TEOS-10 is highly recommended because 1193 1216 \textit{(i)} it is the new official EOS, … … 1195 1218 \textit{(iii)} it uses Conservative Temperature and Absolute Salinity (instead of potential temperature and 1196 1219 practical salinity for EOS-980, both variables being more suitable for use as model variables 1197 \citep{ TEOS10, Graham_McDougall_JPO13}.1220 \citep{ioc.iapso_bk10, graham.mcdougall_JPO13}. 1198 1221 EOS-80 is an obsolescent feature of the NEMO system, kept only for backward compatibility. 1199 1222 For process studies, it is often convenient to use an approximation of the EOS. 1200 To that purposed, a simplified EOS (S-EOS) inspired by \citet{ Vallis06} is also available.1223 To that purposed, a simplified EOS (S-EOS) inspired by \citet{vallis_bk06} is also available. 1201 1224 1202 1225 In the computer code, a density anomaly, $d_a = \rho / \rho_o - 1$, is computed, with $\rho_o$ a reference density. … … 1204 1227 This is a sensible choice for the reference density used in a Boussinesq ocean climate model, as, 1205 1228 with the exception of only a small percentage of the ocean, 1206 density in the World Ocean varies by no more than 2$\%$ from that value \citep{ Gill1982}.1229 density in the World Ocean varies by no more than 2$\%$ from that value \citep{gill_bk82}. 1207 1230 1208 1231 Options are defined through the \ngn{nameos} namelist variables, and in particular \np{nn\_eos} which … … 1210 1233 1211 1234 \begin{description} 1212 \item[\np{nn\_eos} ~\forcode{= -1}]1213 the polyTEOS10-bsq equation of seawater \citep{ Roquet_OM2015} is used.1235 \item[\np{nn\_eos}\forcode{ = -1}] 1236 the polyTEOS10-bsq equation of seawater \citep{roquet.madec.ea_OM15} is used. 1214 1237 The accuracy of this approximation is comparable to the TEOS-10 rational function approximation, 1215 1238 but it is optimized for a boussinesq fluid and the polynomial expressions have simpler and … … 1217 1240 use in ocean models. 1218 1241 Note that a slightly higher precision polynomial form is now used replacement of 1219 the TEOS-10 rational function approximation for hydrographic data analysis \citep{ TEOS10}.1242 the TEOS-10 rational function approximation for hydrographic data analysis \citep{ioc.iapso_bk10}. 1220 1243 A key point is that conservative state variables are used: 1221 1244 Absolute Salinity (unit: g/kg, notation: $S_A$) and Conservative Temperature (unit: \deg{C}, notation: $\Theta$). 1222 1245 The pressure in decibars is approximated by the depth in meters. 1223 1246 With TEOS10, the specific heat capacity of sea water, $C_p$, is a constant. 1224 It is set to $C_p = 3991.86795711963~J\,Kg^{-1}\,^{\circ}K^{-1}$, according to \citet{ TEOS10}.1247 It is set to $C_p = 3991.86795711963~J\,Kg^{-1}\,^{\circ}K^{-1}$, according to \citet{ioc.iapso_bk10}. 1225 1248 Choosing polyTEOS10-bsq implies that the state variables used by the model are $\Theta$ and $S_A$. 1226 1249 In particular, the initial state deined by the user have to be given as \textit{Conservative} Temperature and … … 1229 1252 either computing the air-sea and ice-sea fluxes (forced mode) or 1230 1253 sending the SST field to the atmosphere (coupled mode). 1231 \item[\np{nn\_eos} ~\forcode{= 0}]1254 \item[\np{nn\_eos}\forcode{ = 0}] 1232 1255 the polyEOS80-bsq equation of seawater is used. 1233 1256 It takes the same polynomial form as the polyTEOS10, but the coefficients have been optimized to … … 1238 1261 The pressure in decibars is approximated by the depth in meters. 1239 1262 With thsi EOS, the specific heat capacity of sea water, $C_p$, is a function of temperature, salinity and 1240 pressure \citep{ UNESCO1983}.1263 pressure \citep{fofonoff.millard_bk83}. 1241 1264 Nevertheless, a severe assumption is made in order to have a heat content ($C_p T_p$) which 1242 1265 is conserved by the model: $C_p$ is set to a constant value, the TEOS10 value. 1243 \item[\np{nn\_eos} ~\forcode{= 1}]1244 a simplified EOS (S-EOS) inspired by \citet{ Vallis06} is chosen,1266 \item[\np{nn\_eos}\forcode{ = 1}] 1267 a simplified EOS (S-EOS) inspired by \citet{vallis_bk06} is chosen, 1245 1268 the coefficients of which has been optimized to fit the behavior of TEOS10 1246 (Roquet, personal comm.) (see also \citet{ Roquet_JPO2015}).1269 (Roquet, personal comm.) (see also \citet{roquet.madec.ea_JPO15}). 1247 1270 It provides a simplistic linear representation of both cabbeling and thermobaricity effects which 1248 is enough for a proper treatment of the EOS in theoretical studies \citep{ Roquet_JPO2015}.1271 is enough for a proper treatment of the EOS in theoretical studies \citep{roquet.madec.ea_JPO15}. 1249 1272 With such an equation of state there is no longer a distinction between 1250 1273 \textit{conservative} and \textit{potential} temperature, … … 1303 1326 % Brunt-V\"{a}is\"{a}l\"{a} Frequency 1304 1327 % ------------------------------------------------------------------------------------------------------------- 1305 \subsection{Brunt-V\"{a}is\"{a}l\"{a} frequency (\protect\np{nn\_eos}~\forcode{= 0..2})} 1328 \subsection[Brunt-V\"{a}is\"{a}l\"{a} frequency (\forcode{nn_eos = [0-2]})] 1329 {Brunt-V\"{a}is\"{a}l\"{a} frequency (\protect\np{nn\_eos}\forcode{ = [0-2]})} 1306 1330 \label{subsec:TRA_bn2} 1307 1331 … … 1329 1353 \label{subsec:TRA_fzp} 1330 1354 1331 The freezing point of seawater is a function of salinity and pressure \citep{ UNESCO1983}:1355 The freezing point of seawater is a function of salinity and pressure \citep{fofonoff.millard_bk83}: 1332 1356 \begin{equation} 1333 1357 \label{eq:tra_eos_fzp} … … 1357 1381 % Horizontal Derivative in zps-coordinate 1358 1382 % ================================================================ 1359 \section{Horizontal derivative in \textit{zps}-coordinate (\protect\mdl{zpshde})} 1383 \section[Horizontal derivative in \textit{zps}-coordinate (\textit{zpshde.F90})] 1384 {Horizontal derivative in \textit{zps}-coordinate (\protect\mdl{zpshde})} 1360 1385 \label{sec:TRA_zpshde} 1361 1386 … … 1363 1388 I've changed "derivative" to "difference" and "mean" to "average"} 1364 1389 1365 With partial cells (\np{ln\_zps} ~\forcode{= .true.}) at bottom and top (\np{ln\_isfcav}~\forcode{= .true.}),1390 With partial cells (\np{ln\_zps}\forcode{ = .true.}) at bottom and top (\np{ln\_isfcav}\forcode{ = .true.}), 1366 1391 in general, tracers in horizontally adjacent cells live at different depths. 1367 1392 Horizontal gradients of tracers are needed for horizontal diffusion (\mdl{traldf} module) and 1368 1393 the hydrostatic pressure gradient calculations (\mdl{dynhpg} module). 1369 The partial cell properties at the top (\np{ln\_isfcav} ~\forcode{= .true.}) are computed in the same way as1394 The partial cell properties at the top (\np{ln\_isfcav}\forcode{ = .true.}) are computed in the same way as 1370 1395 for the bottom. 1371 1396 So, only the bottom interpolation is explained below. … … 1379 1404 \begin{figure}[!p] 1380 1405 \begin{center} 1381 \includegraphics[ ]{Fig_partial_step_scheme}1406 \includegraphics[width=\textwidth]{Fig_partial_step_scheme} 1382 1407 \caption{ 1383 1408 \protect\label{fig:Partial_step_scheme} 1384 1409 Discretisation of the horizontal difference and average of tracers in the $z$-partial step coordinate 1385 (\protect\np{ln\_zps} ~\forcode{= .true.}) in the case $(e3w_k^{i + 1} - e3w_k^i) > 0$.1410 (\protect\np{ln\_zps}\forcode{ = .true.}) in the case $(e3w_k^{i + 1} - e3w_k^i) > 0$. 1386 1411 A linear interpolation is used to estimate $\widetilde T_k^{i + 1}$, 1387 1412 the tracer value at the depth of the shallower tracer point of the two adjacent bottom $T$-points.
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