Changeset 11123 for NEMO/trunk
- Timestamp:
- 2019-06-17T14:22:27+02:00 (5 years ago)
- Location:
- NEMO/trunk/doc/latex/NEMO
- Files:
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- 27 edited
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NEMO/trunk/doc/latex/NEMO/main/NEMO_manual.sty
r11043 r11123 6 6 %% LaTeX packages 7 7 %% ============================================================================== 8 \usepackage{natbib} %% bib9 \usepackage{caption} %% caption10 \usepackage{xcolor} %% color11 \usepackage{times} %% font12 \usepackage{hyperref} %% hyper13 \usepackage{idxlayout} %% index14 \usepackage{enumitem} %% list15 \usepackage {minted}%% listing16 \usepackage{amsmath} %% maths17 \usepackage{fancyhdr} %% page18 \usepackage{minitoc} %% toc19 \usepackage{subfiles} %% subdocs20 \usepackage[utf8]{inputenc} %% input encoding21 \usepackage{draftwatermark} %% watermark22 \usepackage{textcomp} %% Companion fonts8 \usepackage{natbib} %% bib 9 \usepackage{caption} %% caption 10 \usepackage{xcolor} %% color 11 \usepackage{times} %% font 12 \usepackage{hyperref} %% hyper 13 \usepackage{idxlayout} %% index 14 \usepackage{enumitem} %% list 15 \usepackage[outputdir=../build]{minted} %% listing 16 \usepackage{amsmath} %% maths 17 \usepackage{fancyhdr} %% page 18 \usepackage{minitoc} %% toc 19 \usepackage{subfiles} %% subdocs 20 \usepackage[utf8]{inputenc} %% input encoding 21 \usepackage{draftwatermark} %% watermark 22 \usepackage{textcomp} %% Companion fonts 23 23 24 24 %% Extensions in bundle package … … 130 130 \newcommand{\pd}[2][]{\ensuremath{\frac{\partial #1}{\partial #2}}} 131 131 132 %% Shortened DOI in bibliography133 \newcommand{\doi}[1]{\href{http://dx.doi.org/#1}{doi:#1}}134 135 132 %% Namelists inclusion 136 133 \newcommand{\nlst}[1]{\forfile{../../../namelists/#1}} -
NEMO/trunk/doc/latex/NEMO/main/NEMO_manual.tex
r11043 r11123 80 80 %% Chapters 81 81 \subfile{../subfiles/chap_model_basics} 82 \subfile{../subfiles/chap_time_domain} % Time discretisation (time stepping strategy)83 \subfile{../subfiles/chap_DOM} % Space discretisation84 \subfile{../subfiles/chap_TRA} % Tracer advection/diffusion equation85 \subfile{../subfiles/chap_DYN} % Dynamics : momentum equation86 \subfile{../subfiles/chap_SBC} % Surface Boundary Conditions87 \subfile{../subfiles/chap_LBC} % Lateral Boundary Conditions88 \subfile{../subfiles/chap_LDF} % Lateral diffusion89 \subfile{../subfiles/chap_ZDF} % Vertical diffusion90 \subfile{../subfiles/chap_DIA} % Outputs and Diagnostics91 \subfile{../subfiles/chap_OBS} % Observation operator92 \subfile{../subfiles/chap_ASM} % Assimilation increments93 \subfile{../subfiles/chap_STO} % Stochastic param.94 \subfile{../subfiles/chap_misc} % Miscellaneous topics95 \subfile{../subfiles/chap_CONFIG} % Predefined configurations82 \subfile{../subfiles/chap_time_domain} % Time discretisation (time stepping strategy) 83 \subfile{../subfiles/chap_DOM} % Space discretisation 84 \subfile{../subfiles/chap_TRA} % Tracer advection/diffusion equation 85 \subfile{../subfiles/chap_DYN} % Dynamics : momentum equation 86 \subfile{../subfiles/chap_SBC} % Surface Boundary Conditions 87 \subfile{../subfiles/chap_LBC} % Lateral Boundary Conditions 88 \subfile{../subfiles/chap_LDF} % Lateral diffusion 89 \subfile{../subfiles/chap_ZDF} % Vertical diffusion 90 \subfile{../subfiles/chap_DIA} % Outputs and Diagnostics 91 \subfile{../subfiles/chap_OBS} % Observation operator 92 \subfile{../subfiles/chap_ASM} % Assimilation increments 93 \subfile{../subfiles/chap_STO} % Stochastic param. 94 \subfile{../subfiles/chap_misc} % Miscellaneous topics 95 \subfile{../subfiles/chap_CONFIG} % Predefined configurations 96 96 97 97 %% Appendix 98 98 \appendix 99 \subfile{../subfiles/annex_A} 100 \subfile{../subfiles/annex_B} 101 \subfile{../subfiles/annex_C} 102 \subfile{../subfiles/annex_iso} 103 \subfile{../subfiles/annex_D} 99 \subfile{../subfiles/annex_A} % Generalised vertical coordinate 100 \subfile{../subfiles/annex_B} % Diffusive operator 101 \subfile{../subfiles/annex_C} % Discrete invariants of the eqs. 102 \subfile{../subfiles/annex_iso} % Isoneutral diffusion using triads 103 \subfile{../subfiles/annex_D} % Coding rules 104 104 105 105 %% Not included 106 %\subfile{../subfiles/chap_conservation} % 106 %\subfile{../subfiles/chap_model_basics_zstar} 107 %\subfile{../subfiles/chap_DIU} 108 %\subfile{../subfiles/chap_conservation} 107 109 %\subfile{../subfiles/annex_E} % Notes on some on going staff 108 109 110 110 111 %% Backmatter -
NEMO/trunk/doc/latex/NEMO/subfiles
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NEMO/trunk/doc/latex/NEMO/subfiles/annex_A.tex
r10442 r11123 399 399 400 400 As in $z$-coordinate, 401 the horizontal pressure gradient can be split in two parts following \citet{ Marsaleix_al_OM08}.401 the horizontal pressure gradient can be split in two parts following \citet{marsaleix.auclair.ea_OM08}. 402 402 Let defined a density anomaly, $d$, by $d=(\rho - \rho_o)/ \rho_o$, 403 403 and a hydrostatic pressure anomaly, $p_h'$, by $p_h'= g \; \int_z^\eta d \; e_3 \; dk$. -
NEMO/trunk/doc/latex/NEMO/subfiles/annex_B.tex
r10442 r11123 162 162 the ($i$,$j$,$k$) curvilinear coordinate system in which 163 163 the equations of the ocean circulation model are formulated, 164 takes the following form \citep{ Redi_JPO82}:164 takes the following form \citep{redi_JPO82}: 165 165 166 166 \begin{equation} … … 184 184 185 185 In practice, isopycnal slopes are generally less than $10^{-2}$ in the ocean, 186 so $\textbf {A}_{\textbf I}$ can be simplified appreciably \citep{ Cox1987}:186 so $\textbf {A}_{\textbf I}$ can be simplified appreciably \citep{cox_OM87}: 187 187 \begin{subequations} 188 188 \label{apdx:B4} -
NEMO/trunk/doc/latex/NEMO/subfiles/annex_D.tex
r10442 r11123 32 32 33 33 To satisfy part of these aims, \NEMO is written with a coding standard which is close to the ECMWF rules, 34 named DOCTOR \citep{ Gibson_TR86}.34 named DOCTOR \citep{gibson_rpt86}. 35 35 These rules present some advantages like: 36 36 -
NEMO/trunk/doc/latex/NEMO/subfiles/annex_E.tex
r10442 r11123 49 49 50 50 This results in a dissipatively dominant (\ie hyper-diffusive) truncation error 51 \citep{ Shchepetkin_McWilliams_OM05}.52 The overall performance of the advection scheme is similar to that reported in \cite{ Farrow1995}.51 \citep{shchepetkin.mcwilliams_OM05}. 52 The overall performance of the advection scheme is similar to that reported in \cite{farrow.stevens_JPO95}. 53 53 It is a relatively good compromise between accuracy and smoothness. 54 54 It is not a \emph{positive} scheme meaning false extrema are permitted but … … 65 65 the second term which is the diffusive part of the scheme, is evaluated using the \textit{before} velocity 66 66 (forward in time). 67 This is discussed by \citet{ Webb_al_JAOT98} in the context of the Quick advection scheme.67 This is discussed by \citet{webb.de-cuevas.ea_JAOT98} in the context of the Quick advection scheme. 68 68 UBS and QUICK schemes only differ by one coefficient. 69 Substituting 1/6 with 1/8 in (\autoref{eq:tra_adv_ubs}) leads to the QUICK advection scheme \citep{ Webb_al_JAOT98}.69 Substituting 1/6 with 1/8 in (\autoref{eq:tra_adv_ubs}) leads to the QUICK advection scheme \citep{webb.de-cuevas.ea_JAOT98}. 70 70 This option is not available through a namelist parameter, since the 1/6 coefficient is hard coded. 71 71 Nevertheless it is quite easy to make the substitution in \mdl{traadv\_ubs} module and obtain a QUICK scheme. … … 80 80 $\tau_w^{ubs}$ will be evaluated using either \textit{(a)} a centered $2^{nd}$ order scheme, 81 81 or \textit{(b)} a TVD scheme, or \textit{(c)} an interpolation based on conservative parabolic splines following 82 \citet{ Shchepetkin_McWilliams_OM05} implementation of UBS in ROMS, or \textit{(d)} an UBS.82 \citet{shchepetkin.mcwilliams_OM05} implementation of UBS in ROMS, or \textit{(d)} an UBS. 83 83 The $3^{rd}$ case has dispersion properties similar to an eight-order accurate conventional scheme. 84 84 … … 255 255 \subsection{Griffies iso-neutral diffusion operator} 256 256 257 Let try to define a scheme that get its inspiration from the \citet{ Griffies_al_JPO98} scheme,257 Let try to define a scheme that get its inspiration from the \citet{griffies.gnanadesikan.ea_JPO98} scheme, 258 258 but is formulated within the \NEMO framework 259 259 (\ie using scale factors rather than grid-size and having a position of $T$-points that … … 272 272 Nevertheless, this technique works fine for $T$ and $S$ as they are active tracers 273 273 (\ie they enter the computation of density), but it does not work for a passive tracer. 274 \citep{ Griffies_al_JPO98} introduce a different way to discretise the off-diagonal terms that274 \citep{griffies.gnanadesikan.ea_JPO98} introduce a different way to discretise the off-diagonal terms that 275 275 nicely solve the problem. 276 276 The idea is to get rid of combinations of an averaged in one direction combined with … … 508 508 \] 509 509 510 \citep{ Griffies_JPO98} introduces another way to implement the eddy induced advection, the so-called skew form.510 \citep{griffies_JPO98} introduces another way to implement the eddy induced advection, the so-called skew form. 511 511 It is based on a transformation of the advective fluxes using the non-divergent nature of the eddy induced velocity. 512 512 For example in the (\textbf{i},\textbf{k}) plane, the tracer advective fluxes can be transformed as follows: … … 574 574 The horizontal component reduces to the one use for an horizontal laplacian operator and 575 575 the vertical one keeps the same complexity, but not more. 576 This property has been used to reduce the computational time \citep{ Griffies_JPO98},576 This property has been used to reduce the computational time \citep{griffies_JPO98}, 577 577 but it is not of practical use as usually $A \neq A_e$. 578 578 Nevertheless this property can be used to choose a discret form of \autoref{eq:eiv_skew_continuous} which -
NEMO/trunk/doc/latex/NEMO/subfiles/annex_iso.tex
r10442 r11123 52 52 the vertical skew flux is further reduced to ensure no vertical buoyancy flux, 53 53 giving an almost pure horizontal diffusive tracer flux within the mixed layer. 54 This is similar to the tapering suggested by \citet{ Gerdes1991}. See \autoref{subsec:Gerdes-taper}54 This is similar to the tapering suggested by \citet{gerdes.koberle.ea_CD91}. See \autoref{subsec:Gerdes-taper} 55 55 \item[\np{ln\_botmix\_triad}] 56 56 See \autoref{sec:iso_bdry}. … … 71 71 \label{sec:iso} 72 72 73 We have implemented into \NEMO a scheme inspired by \citet{ Griffies_al_JPO98},73 We have implemented into \NEMO a scheme inspired by \citet{griffies.gnanadesikan.ea_JPO98}, 74 74 but formulated within the \NEMO framework, using scale factors rather than grid-sizes. 75 75 … … 194 194 \subsection{Expression of the skew-flux in terms of triad slopes} 195 195 196 \citep{ Griffies_al_JPO98} introduce a different discretization of the off-diagonal terms that196 \citep{griffies.gnanadesikan.ea_JPO98} introduce a different discretization of the off-diagonal terms that 197 197 nicely solves the problem. 198 198 % Instead of multiplying the mean slope calculated at the $u$-point by … … 473 473 474 474 To complete the discretization we now need only specify the triad volumes $_i^k\mathbb{V}_{i_p}^{k_p}$. 475 \citet{ Griffies_al_JPO98} identifies these $_i^k\mathbb{V}_{i_p}^{k_p}$ as the volumes of the quarter cells,475 \citet{griffies.gnanadesikan.ea_JPO98} identifies these $_i^k\mathbb{V}_{i_p}^{k_p}$ as the volumes of the quarter cells, 476 476 defined in terms of the distances between $T$, $u$,$f$ and $w$-points. 477 477 This is the natural discretization of \autoref{eq:cts-var}. … … 685 685 As discussed in \autoref{subsec:LDF_slp_iso}, 686 686 iso-neutral slopes relative to geopotentials must be bounded everywhere, 687 both for consistency with the small-slope approximation and for numerical stability \citep{ Cox1987, Griffies_Bk04}.687 both for consistency with the small-slope approximation and for numerical stability \citep{cox_OM87, griffies_bk04}. 688 688 The bound chosen in \NEMO is applied to each component of the slope separately and 689 689 has a value of $1/100$ in the ocean interior. … … 859 859 \footnote{ 860 860 To ensure good behaviour where horizontal density gradients are weak, 861 we in fact follow \citet{ Gerdes1991} and861 we in fact follow \citet{gerdes.koberle.ea_CD91} and 862 862 set $\rML^*=\mathrm{sgn}(\tilde{r}_i)\min(|\rMLt^2/\tilde{r}_i|,|\tilde{r}_i|)-\sigma_i$. 863 863 } … … 865 865 This approach is similar to multiplying the iso-neutral diffusion coefficient by 866 866 $\tilde{r}_{\mathrm{max}}^{-2}\tilde{r}_i^{-2}$ for steep slopes, 867 as suggested by \citet{ Gerdes1991} (see also \citet{Griffies_Bk04}).867 as suggested by \citet{gerdes.koberle.ea_CD91} (see also \citet{griffies_bk04}). 868 868 Again it is applied separately to each triad $_i^k\mathbb{R}_{i_p}^{k_p}$ 869 869 … … 925 925 926 926 However, when \np{ln\_traldf\_triad} is set true, 927 \NEMO instead implements eddy induced advection according to the so-called skew form \citep{ Griffies_JPO98}.927 \NEMO instead implements eddy induced advection according to the so-called skew form \citep{griffies_JPO98}. 928 928 It is based on a transformation of the advective fluxes using the non-divergent nature of the eddy induced velocity. 929 929 For example in the (\textbf{i},\textbf{k}) plane, … … 1139 1139 it is equivalent to a horizontal eiv (eddy-induced velocity) that is uniform within the mixed layer 1140 1140 \autoref{eq:eiv_v}. 1141 This ensures that the eiv velocities do not restratify the mixed layer \citep{ Treguier1997,Danabasoglu_al_2008}.1141 This ensures that the eiv velocities do not restratify the mixed layer \citep{treguier.held.ea_JPO97,danabasoglu.ferrari.ea_JC08}. 1142 1142 Equivantly, in terms of the skew-flux formulation we use here, 1143 1143 the linear slope tapering within the mixed-layer gives a linearly varying vertical flux, … … 1153 1153 $uw$ (integer +1/2 $i$, integer $j$, integer +1/2 $k$) and $vw$ (integer $i$, integer +1/2 $j$, integer +1/2 $k$) 1154 1154 points (see Table \autoref{tab:cell}) respectively. 1155 We follow \citep{ Griffies_Bk04} and calculate the streamfunction at a given $uw$-point from1155 We follow \citep{griffies_bk04} and calculate the streamfunction at a given $uw$-point from 1156 1156 the surrounding four triads according to: 1157 1157 \[ -
NEMO/trunk/doc/latex/NEMO/subfiles/chap_ASM.tex
r10442 r11123 37 37 it may be preferable to introduce the increment gradually into the ocean model in order to 38 38 minimize spurious adjustment processes. 39 This technique is referred to as Incremental Analysis Updates (IAU) \citep{ Bloom_al_MWR96}.39 This technique is referred to as Incremental Analysis Updates (IAU) \citep{bloom.takacs.ea_MWR96}. 40 40 IAU is a common technique used with 3D assimilation methods such as 3D-Var or OI. 41 41 IAU is used when \np{ln\_asmiau} is set to true. … … 118 118 This type of the initialisation reduces the vertical velocity magnitude and 119 119 alleviates the problem of the excessive unphysical vertical mixing in the first steps of the model integration 120 \citep{ Talagrand_JAS72, Dobricic_al_OS07}.120 \citep{talagrand_JAS72, dobricic.pinardi.ea_OS07}. 121 121 Diffusion coefficients are defined as $A_D = \alpha e_{1t} e_{2t}$, where $\alpha = 0.2$. 122 122 The divergence damping is activated by assigning to \np{nn\_divdmp} in the \textit{nam\_asminc} namelist -
NEMO/trunk/doc/latex/NEMO/subfiles/chap_CONFIG.tex
r11112 r11123 96 96 The two "north pole" are the foci of a series of embedded ellipses (blue curves) which 97 97 are determined analytically and form the i-lines of the ORCA mesh (pseudo latitudes). 98 Then, following \citet{ Madec_Imbard_CD96}, the normal to the series of ellipses (red curves) is computed which98 Then, following \citet{madec.imbard_CD96}, the normal to the series of ellipses (red curves) is computed which 99 99 provides the j-lines of the mesh (pseudo longitudes). 100 100 } … … 109 109 \label{subsec:CFG_orca_grid} 110 110 111 The ORCA grid is a tripolar grid based on the semi-analytical method of \citet{ Madec_Imbard_CD96}.111 The ORCA grid is a tripolar grid based on the semi-analytical method of \citet{madec.imbard_CD96}. 112 112 It allows to construct a global orthogonal curvilinear ocean mesh which has no singularity point inside 113 113 the computational domain since two north mesh poles are introduced and placed on lands. … … 207 207 %climate change (Marti et al., 2009). 208 208 %It is also the basis for the \NEMO contribution to the Coordinate Ocean-ice Reference Experiments (COREs) 209 %documented in \citet{ Griffies_al_OM09}.209 %documented in \citet{griffies.biastoch.ea_OM09}. 210 210 211 211 This version of ORCA\_R2 has 31 levels in the vertical, with the highest resolution (10m) in the upper 150m 212 212 (see \autoref{tab:orca_zgr} and \autoref{fig:zgr}). 213 213 The bottom topography and the coastlines are derived from the global atlas of Smith and Sandwell (1997). 214 The default forcing uses the boundary forcing from \citet{ Large_Yeager_Rep04} (see \autoref{subsec:SBC_blk_core}),214 The default forcing uses the boundary forcing from \citet{large.yeager_rpt04} (see \autoref{subsec:SBC_blk_core}), 215 215 which was developed for the purpose of running global coupled ocean-ice simulations without 216 216 an interactive atmosphere. 217 This \citet{ Large_Yeager_Rep04} dataset is available through217 This \citet{large.yeager_rpt04} dataset is available through 218 218 the \href{http://nomads.gfdl.noaa.gov/nomads/forms/mom4/CORE.html}{GFDL web site}. 219 219 The "normal year" of \citet{Large_Yeager_Rep04} has been chosen of the NEMO distribution since release v3.3. … … 230 230 \label{sec:CFG_gyre} 231 231 232 The GYRE configuration \citep{ Levy_al_OM10} has been built to232 The GYRE configuration \citep{levy.klein.ea_OM10} has been built to 233 233 simulate the seasonal cycle of a double-gyre box model. 234 It consists in an idealized domain similar to that used in the studies of \citet{ Drijfhout_JPO94} and235 \citet{ Hazeleger_Drijfhout_JPO98, Hazeleger_Drijfhout_JPO99, Hazeleger_Drijfhout_JGR00, Hazeleger_Drijfhout_JPO00},234 It consists in an idealized domain similar to that used in the studies of \citet{drijfhout_JPO94} and 235 \citet{hazeleger.drijfhout_JPO98, hazeleger.drijfhout_JPO99, hazeleger.drijfhout_JGR00, hazeleger.drijfhout_JPO00}, 236 236 over which an analytical seasonal forcing is applied. 237 237 This allows to investigate the spontaneous generation of a large number of interacting, transient mesoscale eddies … … 244 244 The configuration is meant to represent an idealized North Atlantic or North Pacific basin. 245 245 The circulation is forced by analytical profiles of wind and buoyancy fluxes. 246 The applied forcings vary seasonally in a sinusoidal manner between winter and summer extrema \citep{ Levy_al_OM10}.246 The applied forcings vary seasonally in a sinusoidal manner between winter and summer extrema \citep{levy.klein.ea_OM10}. 247 247 The wind stress is zonal and its curl changes sign at 22\deg{N} and 36\deg{N}. 248 248 It forces a subpolar gyre in the north, a subtropical gyre in the wider part of the domain and … … 284 284 \protect\label{fig:GYRE} 285 285 Snapshot of relative vorticity at the surface of the model domain in GYRE R9, R27 and R54. 286 From \citet{ Levy_al_OM10}.286 From \citet{levy.klein.ea_OM10}. 287 287 } 288 288 \end{center} -
NEMO/trunk/doc/latex/NEMO/subfiles/chap_DIA.tex
r10509 r11123 1507 1507 remain at a given depth ($w = 0$ in the computation) have been introduced in the system during the CLIPPER project. 1508 1508 Options are defined by \ngn{namflo} namelis variables. 1509 The algorithm used is based either on the work of \cite{ Blanke_Raynaud_JPO97} (default option),1509 The algorithm used is based either on the work of \cite{blanke.raynaud_JPO97} (default option), 1510 1510 or on a $4^th$ Runge-Hutta algorithm (\np{ln\_flork4}\forcode{ = .true.}). 1511 Note that the \cite{ Blanke_Raynaud_JPO97} algorithm have the advantage of providing trajectories which1511 Note that the \cite{blanke.raynaud_JPO97} algorithm have the advantage of providing trajectories which 1512 1512 are consistent with the numeric of the code, so that the trajectories never intercept the bathymetry. 1513 1513 … … 1809 1809 The steric effect is therefore not explicitely represented. 1810 1810 This approximation does not represent a serious error with respect to the flow field calculated by the model 1811 \citep{ Greatbatch_JGR94}, but extra attention is required when investigating sea level,1811 \citep{greatbatch_JGR94}, but extra attention is required when investigating sea level, 1812 1812 as steric changes are an important contribution to local changes in sea level on seasonal and climatic time scales. 1813 1813 This is especially true for investigation into sea level rise due to global warming. 1814 1814 1815 1815 Fortunately, the steric contribution to the sea level consists of a spatially uniform component that 1816 can be diagnosed by considering the mass budget of the world ocean \citep{ Greatbatch_JGR94}.1816 can be diagnosed by considering the mass budget of the world ocean \citep{greatbatch_JGR94}. 1817 1817 In order to better understand how global mean sea level evolves and thus how the steric sea level can be diagnosed, 1818 1818 we compare, in the following, the non-Boussinesq and Boussinesq cases. … … 1888 1888 the ocean surface, not by changes in mean mass of the ocean: the steric effect is missing in a Boussinesq fluid. 1889 1889 1890 Nevertheless, following \citep{ Greatbatch_JGR94}, the steric effect on the volume can be diagnosed by1890 Nevertheless, following \citep{greatbatch_JGR94}, the steric effect on the volume can be diagnosed by 1891 1891 considering the mass budget of the ocean. 1892 1892 The apparent changes in $\mathcal{M}$, mass of the ocean, which are not induced by surface mass flux 1893 1893 must be compensated by a spatially uniform change in the mean sea level due to expansion/contraction of the ocean 1894 \citep{ Greatbatch_JGR94}.1894 \citep{greatbatch_JGR94}. 1895 1895 In others words, the Boussinesq mass, $\mathcal{M}_o$, can be related to $\mathcal{M}$, 1896 1896 the total mass of the ocean seen by the Boussinesq model, via the steric contribution to the sea level, … … 1924 1924 This value is a sensible choice for the reference density used in a Boussinesq ocean climate model since, 1925 1925 with the exception of only a small percentage of the ocean, density in the World Ocean varies by no more than 1926 2$\%$ from this value (\cite{ Gill1982}, page 47).1926 2$\%$ from this value (\cite{gill_bk82}, page 47). 1927 1927 1928 1928 Second, we have assumed here that the total ocean surface, $\mathcal{A}$, … … 1954 1954 so that there are no associated ocean currents. 1955 1955 Hence, the dynamically relevant sea level is the effective sea level, 1956 \ie the sea level as if sea ice (and snow) were converted to liquid seawater \citep{ Campin_al_OM08}.1956 \ie the sea level as if sea ice (and snow) were converted to liquid seawater \citep{campin.marshall.ea_OM08}. 1957 1957 However, in the current version of \NEMO the sea-ice is levitating above the ocean without mass exchanges between 1958 1958 ice and ocean. … … 1986 1986 Among the available diagnostics the following ones are obtained when defining the \key{diahth} CPP key: 1987 1987 1988 - the mixed layer depth (based on a density criterion \citep{de _Boyer_Montegut_al_JGR04}) (\mdl{diahth})1988 - the mixed layer depth (based on a density criterion \citep{de-boyer-montegut.madec.ea_JGR04}) (\mdl{diahth}) 1989 1989 1990 1990 - the turbocline depth (based on a turbulent mixing coefficient criterion) (\mdl{diahth}) -
NEMO/trunk/doc/latex/NEMO/subfiles/chap_DIU.tex
r10442 r11123 60 60 %=============================================================== 61 61 62 The warm layer is calculated using the model of \citet{ Takaya_al_JGR10} (TAKAYA10 model hereafter).62 The warm layer is calculated using the model of \citet{takaya.bidlot.ea_JGR10} (TAKAYA10 model hereafter). 63 63 This is a simple flux based model that is defined by the equations 64 64 \begin{align} … … 87 87 where $Q_{\rm{h}}$ is the sensible and latent heat flux, $Q_{\rm{lw}}$ is the long wave flux, 88 88 and $Q_{\rm{sol}}$ is the solar flux absorbed within the diurnal warm layer. 89 For $Q_{\rm{sol}}$ the 9 term representation of \citet{ Gentemann_al_JGR09} is used.89 For $Q_{\rm{sol}}$ the 9 term representation of \citet{gentemann.minnett.ea_JGR09} is used. 90 90 In equation \autoref{eq:ecmwf1} the function $f(L_a)=\max(1,L_a^{\frac{2}{3}})$, 91 91 where $L_a=0.3$\footnote{ … … 118 118 %=============================================================== 119 119 120 The cool skin is modelled using the framework of \citet{ Saunders_JAS82} who used a formulation of the near surface temperature difference based upon the heat flux and the friction velocity $u^*_{w}$.120 The cool skin is modelled using the framework of \citet{saunders_JAS67} who used a formulation of the near surface temperature difference based upon the heat flux and the friction velocity $u^*_{w}$. 121 121 As the cool skin is so thin (~1\,mm) we ignore the solar flux component to the heat flux and the Saunders equation for the cool skin temperature difference $\Delta T_{\rm{cs}}$ becomes 122 122 \[ … … 132 132 \end{equation} 133 133 where $\mu$ is the kinematic viscosity of sea water and $\lambda$ is a constant of proportionality which 134 \citet{ Saunders_JAS82} suggested varied between 5 and 10.134 \citet{saunders_JAS67} suggested varied between 5 and 10. 135 135 136 The value of $\lambda$ used in equation (\autoref{eq:sunders_thick_eqn}) is that of \citet{ Artale_al_JGR02},137 which is shown in \citet{ Tu_Tsuang_GRL05} to outperform a number of other parametrisations at136 The value of $\lambda$ used in equation (\autoref{eq:sunders_thick_eqn}) is that of \citet{artale.iudicone.ea_JGR02}, 137 which is shown in \citet{tu.tsuang_GRL05} to outperform a number of other parametrisations at 138 138 both low and high wind speeds. 139 139 Specifically, -
NEMO/trunk/doc/latex/NEMO/subfiles/chap_DOM.tex
r10502 r11123 60 60 the centre of each face of the cells (\autoref{fig:cell}). 61 61 This is the generalisation to three dimensions of the well-known ``C'' grid in Arakawa's classification 62 \citep{ Mesinger_Arakawa_Bk76}.62 \citep{mesinger.arakawa_bk76}. 63 63 The relative and planetary vorticity, $\zeta$ and $f$, are defined in the centre of each vertical edge and 64 64 the barotropic stream function $\psi$ is defined at horizontal points overlying the $\zeta$ and $f$-points. … … 397 397 (\ie as the analytical first derivative of the transformation that 398 398 gives $(\lambda,\varphi,z)$ as a function of $(i,j,k)$) 399 is specific to the \NEMO model \citep{ Marti_al_JGR92}.399 is specific to the \NEMO model \citep{marti.madec.ea_JGR92}. 400 400 As an example, $e_{1t}$ is defined locally at a $t$-point, 401 401 whereas many other models on a C grid choose to define such a scale factor as … … 405 405 since they are first introduced in the continuous equations; 406 406 secondly, analytical transformations encourage good practice by the definition of smoothly varying grids 407 (rather than allowing the user to set arbitrary jumps in thickness between adjacent layers) \citep{ Treguier1996}.407 (rather than allowing the user to set arbitrary jumps in thickness between adjacent layers) \citep{treguier.dukowicz.ea_JGR96}. 408 408 An example of the effect of such a choice is shown in \autoref{fig:zgr_e3}. 409 409 %>>>>>>>>>>>>>>>>>>>>>>>>>>>> … … 827 827 The original default NEMO s-coordinate stretching is available if neither of the other options are specified as true 828 828 (\np{ln\_s\_SH94}~\forcode{= .false.} and \np{ln\_s\_SF12}~\forcode{= .false.}). 829 This uses a depth independent $\tanh$ function for the stretching \citep{ Madec_al_JPO96}:829 This uses a depth independent $\tanh$ function for the stretching \citep{madec.delecluse.ea_JPO96}: 830 830 831 831 \[ … … 846 846 847 847 A stretching function, 848 modified from the commonly used \citet{ Song_Haidvogel_JCP94} stretching (\np{ln\_s\_SH94}~\forcode{= .true.}),848 modified from the commonly used \citet{song.haidvogel_JCP94} stretching (\np{ln\_s\_SH94}~\forcode{= .true.}), 849 849 is also available and is more commonly used for shelf seas modelling: 850 850 … … 876 876 877 877 Another example has been provided at version 3.5 (\np{ln\_s\_SF12}) that allows a fixed surface resolution in 878 an analytical terrain-following stretching \citet{ Siddorn_Furner_OM12}.878 an analytical terrain-following stretching \citet{siddorn.furner_OM13}. 879 879 In this case the a stretching function $\gamma$ is defined such that: 880 880 … … 913 913 \includegraphics[]{Fig_DOM_compare_coordinates_surface} 914 914 \caption{ 915 A comparison of the \citet{ Song_Haidvogel_JCP94} $S$-coordinate (solid lines),915 A comparison of the \citet{song.haidvogel_JCP94} $S$-coordinate (solid lines), 916 916 a 50 level $Z$-coordinate (contoured surfaces) and 917 the \citet{ Siddorn_Furner_OM12} $S$-coordinate (dashed lines) in the surface $100~m$ for917 the \citet{siddorn.furner_OM13} $S$-coordinate (dashed lines) in the surface $100~m$ for 918 918 a idealised bathymetry that goes from $50~m$ to $5500~m$ depth. 919 919 For clarity every third coordinate surface is shown. … … 929 929 creating a non-analytical vertical coordinate that 930 930 therefore may suffer from large gradients in the vertical resolutions. 931 This stretching is less straightforward to implement than the \citet{ Song_Haidvogel_JCP94} stretching,931 This stretching is less straightforward to implement than the \citet{song.haidvogel_JCP94} stretching, 932 932 but has the advantage of resolving diurnal processes in deep water and has generally flatter slopes. 933 933 934 As with the \citet{ Song_Haidvogel_JCP94} stretching the stretch is only applied at depths greater than934 As with the \citet{song.haidvogel_JCP94} stretching the stretch is only applied at depths greater than 935 935 the critical depth $h_c$. 936 936 In this example two options are available in depths shallower than $h_c$, … … 940 940 Minimising the horizontal slope of the vertical coordinate is important in terrain-following systems as 941 941 large slopes lead to hydrostatic consistency. 942 A hydrostatic consistency parameter diagnostic following \citet{ Haney1991} has been implemented,942 A hydrostatic consistency parameter diagnostic following \citet{haney_JPO91} has been implemented, 943 943 and is output as part of the model mesh file at the start of the run. 944 944 … … 960 960 961 961 Whatever the vertical coordinate used, the model offers the possibility of representing the bottom topography with 962 steps that follow the face of the model cells (step like topography) \citep{ Madec_al_JPO96}.962 steps that follow the face of the model cells (step like topography) \citep{madec.delecluse.ea_JPO96}. 963 963 The distribution of the steps in the horizontal is defined in a 2D integer array, mbathy, which 964 964 gives the number of ocean levels (\ie those that are not masked) at each $t$-point. -
NEMO/trunk/doc/latex/NEMO/subfiles/chap_DYN.tex
r10499 r11123 127 127 Replacing $T$ by the number $1$ in the tracer equation and summing over the water column must lead to 128 128 the sea surface height equation otherwise tracer content will not be conserved 129 \citep{ Griffies_al_MWR01, Leclair_Madec_OM09}.129 \citep{griffies.pacanowski.ea_MWR01, leclair.madec_OM09}. 130 130 131 131 The vertical velocity is computed by an upward integration of the horizontal divergence starting at the bottom, … … 287 287 Nevertheless, this technique strongly distort the phase and group velocity of Rossby waves....} 288 288 289 A very nice solution to the problem of double averaging was proposed by \citet{ Arakawa_Hsu_MWR90}.289 A very nice solution to the problem of double averaging was proposed by \citet{arakawa.hsu_MWR90}. 290 290 The idea is to get rid of the double averaging by considering triad combinations of vorticity. 291 291 It is noteworthy that this solution is conceptually quite similar to the one proposed by 292 \citep{ Griffies_al_JPO98} for the discretization of the iso-neutral diffusion operator (see \autoref{apdx:C}).293 294 The \citet{ Arakawa_Hsu_MWR90} vorticity advection scheme for a single layer is modified295 for spherical coordinates as described by \citet{ Arakawa_Lamb_MWR81} to obtain the EEN scheme.292 \citep{griffies.gnanadesikan.ea_JPO98} for the discretization of the iso-neutral diffusion operator (see \autoref{apdx:C}). 293 294 The \citet{arakawa.hsu_MWR90} vorticity advection scheme for a single layer is modified 295 for spherical coordinates as described by \citet{arakawa.lamb_MWR81} to obtain the EEN scheme. 296 296 First consider the discrete expression of the potential vorticity, $q$, defined at an $f$-point: 297 297 \[ … … 327 327 (with a systematic reduction of $e_{3f}$ when a model level intercept the bathymetry) 328 328 that tends to reinforce the topostrophy of the flow 329 (\ie the tendency of the flow to follow the isobaths) \citep{ Penduff_al_OS07}.329 (\ie the tendency of the flow to follow the isobaths) \citep{penduff.le-sommer.ea_OS07}. 330 330 331 331 Next, the vorticity triads, $ {^i_j}\mathbb{Q}^{i_p}_{j_p}$ can be defined at a $T$-point as … … 356 356 (\ie $\chi$=$0$) (see \autoref{subsec:C_vorEEN}). 357 357 Applied to a realistic ocean configuration, it has been shown that it leads to a significant reduction of 358 the noise in the vertical velocity field \citep{ Le_Sommer_al_OM09}.358 the noise in the vertical velocity field \citep{le-sommer.penduff.ea_OM09}. 359 359 Furthermore, used in combination with a partial steps representation of bottom topography, 360 360 it improves the interaction between current and topography, 361 leading to a larger topostrophy of the flow \citep{ Barnier_al_OD06, Penduff_al_OS07}.361 leading to a larger topostrophy of the flow \citep{barnier.madec.ea_OD06, penduff.le-sommer.ea_OS07}. 362 362 363 363 %-------------------------------------------------------------------------------------------------------------- … … 403 403 When \np{ln\_dynzad\_zts}\forcode{ = .true.}, 404 404 a split-explicit time stepping with 5 sub-timesteps is used on the vertical advection term. 405 This option can be useful when the value of the timestep is limited by vertical advection \citep{ Lemarie_OM2015}.405 This option can be useful when the value of the timestep is limited by vertical advection \citep{lemarie.debreu.ea_OM15}. 406 406 Note that in this case, 407 407 a similar split-explicit time stepping should be used on vertical advection of tracer to ensure a better stability, … … 475 475 a $2^{nd}$ order centered finite difference scheme, CEN2, 476 476 or a $3^{rd}$ order upstream biased scheme, UBS. 477 The latter is described in \citet{ Shchepetkin_McWilliams_OM05}.477 The latter is described in \citet{shchepetkin.mcwilliams_OM05}. 478 478 The schemes are selected using the namelist logicals \np{ln\_dynadv\_cen2} and \np{ln\_dynadv\_ubs}. 479 479 In flux form, the schemes differ by the choice of a space and time interpolation to define the value of … … 523 523 where $u"_{i+1/2} =\delta_{i+1/2} \left[ {\delta_i \left[ u \right]} \right]$. 524 524 This results in a dissipatively dominant (\ie hyper-diffusive) truncation error 525 \citep{ Shchepetkin_McWilliams_OM05}.526 The overall performance of the advection scheme is similar to that reported in \citet{ Farrow1995}.525 \citep{shchepetkin.mcwilliams_OM05}. 526 The overall performance of the advection scheme is similar to that reported in \citet{farrow.stevens_JPO95}. 527 527 It is a relatively good compromise between accuracy and smoothness. 528 528 It is not a \emph{positive} scheme, meaning that false extrema are permitted. … … 542 542 while the second term, which is the diffusion part of the scheme, 543 543 is evaluated using the \textit{before} velocity (forward in time). 544 This is discussed by \citet{ Webb_al_JAOT98} in the context of the Quick advection scheme.544 This is discussed by \citet{webb.de-cuevas.ea_JAOT98} in the context of the Quick advection scheme. 545 545 546 546 Note that the UBS and QUICK (Quadratic Upstream Interpolation for Convective Kinematics) schemes only differ by 547 547 one coefficient. 548 Replacing $1/6$ by $1/8$ in (\autoref{eq:dynadv_ubs}) leads to the QUICK advection scheme \citep{ Webb_al_JAOT98}.548 Replacing $1/6$ by $1/8$ in (\autoref{eq:dynadv_ubs}) leads to the QUICK advection scheme \citep{webb.de-cuevas.ea_JAOT98}. 549 549 This option is not available through a namelist parameter, since the $1/6$ coefficient is hard coded. 550 550 Nevertheless it is quite easy to make the substitution in the \mdl{dynadv\_ubs} module and obtain a QUICK scheme. … … 652 652 653 653 Pressure gradient formulations in an $s$-coordinate have been the subject of a vast number of papers 654 (\eg, \citet{ Song1998, Shchepetkin_McWilliams_OM05}).654 (\eg, \citet{song_MWR98, shchepetkin.mcwilliams_OM05}). 655 655 A number of different pressure gradient options are coded but the ROMS-like, 656 656 density Jacobian with cubic polynomial method is currently disabled whilst known bugs are under investigation. 657 657 658 $\bullet$ Traditional coding (see for example \citet{ Madec_al_JPO96}: (\np{ln\_dynhpg\_sco}\forcode{ = .true.})658 $\bullet$ Traditional coding (see for example \citet{madec.delecluse.ea_JPO96}: (\np{ln\_dynhpg\_sco}\forcode{ = .true.}) 659 659 \begin{equation} 660 660 \label{eq:dynhpg_sco} … … 679 679 $\bullet$ Pressure Jacobian scheme (prj) (a research paper in preparation) (\np{ln\_dynhpg\_prj}\forcode{ = .true.}) 680 680 681 $\bullet$ Density Jacobian with cubic polynomial scheme (DJC) \citep{ Shchepetkin_McWilliams_OM05}681 $\bullet$ Density Jacobian with cubic polynomial scheme (DJC) \citep{shchepetkin.mcwilliams_OM05} 682 682 (\np{ln\_dynhpg\_djc}\forcode{ = .true.}) (currently disabled; under development) 683 683 684 684 Note that expression \autoref{eq:dynhpg_sco} is commonly used when the variable volume formulation is activated 685 685 (\key{vvl}) because in that case, even with a flat bottom, 686 the coordinate surfaces are not horizontal but follow the free surface \citep{ Levier2007}.686 the coordinate surfaces are not horizontal but follow the free surface \citep{levier.treguier.ea_rpt07}. 687 687 The pressure jacobian scheme (\np{ln\_dynhpg\_prj}\forcode{ = .true.}) is available as 688 688 an improved option to \np{ln\_dynhpg\_sco}\forcode{ = .true.} when \key{vvl} is active. … … 704 704 corresponds to the water replaced by the ice shelf. 705 705 This top pressure is constant over time. 706 A detailed description of this method is described in \citet{ Losch2008}.\\706 A detailed description of this method is described in \citet{losch_JGR08}.\\ 707 707 708 708 The pressure gradient due to ocean load is computed using the expression \autoref{eq:dynhpg_sco} described in … … 722 722 the physical phenomenon that controls the time-step is internal gravity waves (IGWs). 723 723 A semi-implicit scheme for doubling the stability limit associated with IGWs can be used 724 \citep{ Brown_Campana_MWR78, Maltrud1998}.724 \citep{brown.campana_MWR78, maltrud.smith.ea_JGR98}. 725 725 It involves the evaluation of the hydrostatic pressure gradient as 726 726 an average over the three time levels $t-\rdt$, $t$, and $t+\rdt$ … … 790 790 which imposes a very small time step when an explicit time stepping is used. 791 791 Two methods are proposed to allow a longer time step for the three-dimensional equations: 792 the filtered free surface, which is a modification of the continuous equations (see \autoref{eq:PE_flt }),792 the filtered free surface, which is a modification of the continuous equations (see \autoref{eq:PE_flt?}), 793 793 and the split-explicit free surface described below. 794 794 The extra term introduced in the filtered method is calculated implicitly, … … 845 845 846 846 The split-explicit free surface formulation used in \NEMO (\key{dynspg\_ts} defined), 847 also called the time-splitting formulation, follows the one proposed by \citet{ Shchepetkin_McWilliams_OM05}.847 also called the time-splitting formulation, follows the one proposed by \citet{shchepetkin.mcwilliams_OM05}. 848 848 The general idea is to solve the free surface equation and the associated barotropic velocity equations with 849 849 a smaller time step than $\rdt$, the time step used for the three dimensional prognostic variables … … 876 876 (see section \autoref{sec:ZDF_bfr}), explicitly accounted for at each barotropic iteration. 877 877 Temporal discretization of the system above follows a three-time step Generalized Forward Backward algorithm 878 detailed in \citet{ Shchepetkin_McWilliams_OM05}.878 detailed in \citet{shchepetkin.mcwilliams_OM05}. 879 879 AB3-AM4 coefficients used in \NEMO follow the second-order accurate, 880 "multi-purpose" stability compromise as defined in \citet{ Shchepetkin_McWilliams_Bk08}880 "multi-purpose" stability compromise as defined in \citet{shchepetkin.mcwilliams_ibk09} 881 881 (see their figure 12, lower left). 882 882 … … 936 936 and time splitting not compatible. 937 937 Advective barotropic velocities are obtained by using a secondary set of filtering weights, 938 uniquely defined from the filter coefficients used for the time averaging (\citet{ Shchepetkin_McWilliams_OM05}).938 uniquely defined from the filter coefficients used for the time averaging (\citet{shchepetkin.mcwilliams_OM05}). 939 939 Consistency between the time averaged continuity equation and the time stepping of tracers is here the key to 940 940 obtain exact conservation. … … 953 953 external gravity waves in idealized or weakly non-linear cases. 954 954 Although the damping is lower than for the filtered free surface, 955 it is still significant as shown by \citet{ Levier2007} in the case of an analytical barotropic Kelvin wave.955 it is still significant as shown by \citet{levier.treguier.ea_rpt07} in the case of an analytical barotropic Kelvin wave. 956 956 957 957 %>>>>>=============== … … 1051 1051 the leap-frog splitting mode in equation \autoref{eq:DYN_spg_ts_ssh}. 1052 1052 We have tried various forms of such filtering, 1053 with the following method discussed in \cite{ Griffies_al_MWR01} chosen due to1053 with the following method discussed in \cite{griffies.pacanowski.ea_MWR01} chosen due to 1054 1054 its stability and reasonably good maintenance of tracer conservation properties (see ??). 1055 1055 … … 1084 1084 \label{subsec:DYN_spg_fltp} 1085 1085 1086 The filtered formulation follows the \citet{ Roullet_Madec_JGR00} implementation.1086 The filtered formulation follows the \citet{roullet.madec_JGR00} implementation. 1087 1087 The extra term introduced in the equations (see \autoref{subsec:PE_free_surface}) is solved implicitly. 1088 1088 The elliptic solvers available in the code are documented in \autoref{chap:MISC}. … … 1326 1326 There are two main options for wetting and drying code (wd): 1327 1327 (a) an iterative limiter (il) and (b) a directional limiter (dl). 1328 The directional limiter is based on the scheme developed by \cite{ WarnerEtal13} for RO1328 The directional limiter is based on the scheme developed by \cite{warner.defne.ea_CG13} for RO 1329 1329 MS 1330 which was in turn based on ideas developed for POM by \cite{ Oey06}. The iterative1330 which was in turn based on ideas developed for POM by \cite{oey_OM06}. The iterative 1331 1331 limiter is a new scheme. The iterative limiter is activated by setting $\mathrm{ln\_wd\_il} = \mathrm{.true.}$ 1332 1332 and $\mathrm{ln\_wd\_dl} = \mathrm{.false.}$. The directional limiter is activated … … 1400 1400 1401 1401 1402 \cite{ WarnerEtal13} state that in their scheme the velocity masks at the cell faces for the baroclinic1402 \cite{warner.defne.ea_CG13} state that in their scheme the velocity masks at the cell faces for the baroclinic 1403 1403 timesteps are set to 0 or 1 depending on whether the average of the masks over the barotropic sub-steps is respectively less than 1404 1404 or greater than 0.5. That scheme does not conserve tracers in integrations started from constant tracer -
NEMO/trunk/doc/latex/NEMO/subfiles/chap_LBC.tex
r10614 r11123 395 395 396 396 The BDY module was modelled on the OBC module (see NEMO 3.4) and shares many features and 397 a similar coding structure \citep{ Chanut2005}.397 a similar coding structure \citep{chanut_rpt05}. 398 398 The specification of the location of the open boundary is completely flexible and 399 399 allows for example the open boundary to follow an isobath or other irregular contour. … … 475 475 \label{subsec:BDY_FRS_scheme} 476 476 477 The Flow Relaxation Scheme (FRS) \citep{ Davies_QJRMS76,Engerdahl_Tel95},477 The Flow Relaxation Scheme (FRS) \citep{davies_QJRMS76,engedahl_T95}, 478 478 applies a simple relaxation of the model fields to externally-specified values over 479 479 a zone next to the edge of the model domain. … … 514 514 \label{subsec:BDY_flather_scheme} 515 515 516 The \citet{ Flather_JPO94} scheme is a radiation condition on the normal,516 The \citet{flather_JPO94} scheme is a radiation condition on the normal, 517 517 depth-mean transport across the open boundary. 518 518 It takes the form … … 535 535 \label{subsec:BDY_orlanski_scheme} 536 536 537 The Orlanski scheme is based on the algorithm described by \citep{ Marchesiello2001}, hereafter MMS.537 The Orlanski scheme is based on the algorithm described by \citep{marchesiello.mcwilliams.ea_OM01}, hereafter MMS. 538 538 539 539 The adaptive Orlanski condition solves a wave plus relaxation equation at the boundary: -
NEMO/trunk/doc/latex/NEMO/subfiles/chap_LDF.tex
r10442 r11123 44 44 \gmcomment{ 45 45 we should emphasize here that the implementation is a rather old one. 46 Better work can be achieved by using \citet{ Griffies_al_JPO98, Griffies_Bk04} iso-neutral scheme.46 Better work can be achieved by using \citet{griffies.gnanadesikan.ea_JPO98, griffies_bk04} iso-neutral scheme. 47 47 } 48 48 … … 119 119 %In practice, \autoref{eq:ldfslp_iso} is of little help in evaluating the neutral surface slopes. Indeed, for an unsimplified equation of state, the density has a strong dependancy on pressure (here approximated as the depth), therefore applying \autoref{eq:ldfslp_iso} using the $in situ$ density, $\rho$, computed at T-points leads to a flattening of slopes as the depth increases. This is due to the strong increase of the $in situ$ density with depth. 120 120 121 %By definition, neutral surfaces are tangent to the local $in situ$ density \citep{ McDougall1987}, therefore in \autoref{eq:ldfslp_iso}, all the derivatives have to be evaluated at the same local pressure (which in decibars is approximated by the depth in meters).121 %By definition, neutral surfaces are tangent to the local $in situ$ density \citep{mcdougall_JPO87}, therefore in \autoref{eq:ldfslp_iso}, all the derivatives have to be evaluated at the same local pressure (which in decibars is approximated by the depth in meters). 122 122 123 123 %In the $z$-coordinate, the derivative of the \autoref{eq:ldfslp_iso} numerator is evaluated at the same depth \nocite{as what?} ($T$-level, which is the same as the $u$- and $v$-levels), so the $in situ$ density can be used for its evaluation. … … 135 135 thus the $in situ$ density can be used. 136 136 This is not the case for the vertical derivatives: $\delta_{k+1/2}[\rho]$ is replaced by $-\rho N^2/g$, 137 where $N^2$ is the local Brunt-Vais\"{a}l\"{a} frequency evaluated following \citet{ McDougall1987}137 where $N^2$ is the local Brunt-Vais\"{a}l\"{a} frequency evaluated following \citet{mcdougall_JPO87} 138 138 (see \autoref{subsec:TRA_bn2}). 139 139 … … 154 154 Note: The solution for $s$-coordinate passes trough the use of different (and better) expression for 155 155 the constraint on iso-neutral fluxes. 156 Following \citet{ Griffies_Bk04}, instead of specifying directly that there is a zero neutral diffusive flux of156 Following \citet{griffies_bk04}, instead of specifying directly that there is a zero neutral diffusive flux of 157 157 locally referenced potential density, we stay in the $T$-$S$ plane and consider the balance between 158 158 the neutral direction diffusive fluxes of potential temperature and salinity: … … 201 201 a minimum background horizontal diffusion for numerical stability reasons. 202 202 To overcome this problem, several techniques have been proposed in which the numerical schemes of 203 the ocean model are modified \citep{ Weaver_Eby_JPO97, Griffies_al_JPO98}.203 the ocean model are modified \citep{weaver.eby_JPO97, griffies.gnanadesikan.ea_JPO98}. 204 204 Griffies's scheme is now available in \NEMO if \np{traldf\_grif\_iso} is set true; see Appdx \autoref{apdx:triad}. 205 Here, another strategy is presented \citep{ Lazar_PhD97}:205 Here, another strategy is presented \citep{lazar_phd97}: 206 206 a local filtering of the iso-neutral slopes (made on 9 grid-points) prevents the development of 207 207 grid point noise generated by the iso-neutral diffusion operator (\autoref{fig:LDF_ZDF1}). … … 212 212 213 213 Nevertheless, this iso-neutral operator does not ensure that variance cannot increase, 214 contrary to the \citet{ Griffies_al_JPO98} operator which has that property.214 contrary to the \citet{griffies.gnanadesikan.ea_JPO98} operator which has that property. 215 215 216 216 %>>>>>>>>>>>>>>>>>>>>>>>>>>>> … … 235 235 236 236 237 % In addition and also for numerical stability reasons \citep{ Cox1987, Griffies_Bk04},237 % In addition and also for numerical stability reasons \citep{cox_OM87, griffies_bk04}, 238 238 % the slopes are bounded by $1/100$ everywhere. This limit is decreasing linearly 239 239 % to zero fom $70$ meters depth and the surface (the fact that the eddies "feel" the 240 240 % surface motivates this flattening of isopycnals near the surface). 241 241 242 For numerical stability reasons \citep{ Cox1987, Griffies_Bk04}, the slopes must also be bounded by242 For numerical stability reasons \citep{cox_OM87, griffies_bk04}, the slopes must also be bounded by 243 243 $1/100$ everywhere. 244 244 This constraint is applied in a piecewise linear fashion, increasing from zero at the surface to … … 366 366 This variation is intended to reflect the lesser need for subgrid scale eddy mixing where 367 367 the grid size is smaller in the domain. 368 It was introduced in the context of the DYNAMO modelling project \citep{ Willebrand_al_PO01}.368 It was introduced in the context of the DYNAMO modelling project \citep{willebrand.barnier.ea_PO01}. 369 369 Note that such a grid scale dependance of mixing coefficients significantly increase the range of stability of 370 370 model configurations presenting large changes in grid pacing such as global ocean models. … … 376 376 For example, in the ORCA2 global ocean model (see Configurations), 377 377 the laplacian viscosity operator uses \np{rn\_ahm0}~= 4.10$^4$ m$^2$/s poleward of 20$^{\circ}$ north and south and 378 decreases linearly to \np{rn\_aht0}~= 2.10$^3$ m$^2$/s at the equator \citep{ Madec_al_JPO96, Delecluse_Madec_Bk00}.378 decreases linearly to \np{rn\_aht0}~= 2.10$^3$ m$^2$/s at the equator \citep{madec.delecluse.ea_JPO96, delecluse.madec_icol99}. 379 379 This modification can be found in routine \rou{ldf\_dyn\_c2d\_orca} defined in \mdl{ldfdyn\_c2d}. 380 380 Similar modified horizontal variations can be found with the Antarctic or Arctic sub-domain options of … … 475 475 since it allows us to take advantage of all the advection schemes offered for the tracers 476 476 (see \autoref{sec:TRA_adv}) and not just the $2^{nd}$ order advection scheme as in 477 previous releases of OPA \citep{ Madec1998}.477 previous releases of OPA \citep{madec.delecluse.ea_NPM98}. 478 478 This is particularly useful for passive tracers where \emph{positivity} of the advection scheme is of 479 479 paramount importance. -
NEMO/trunk/doc/latex/NEMO/subfiles/chap_OBS.tex
r10442 r11123 612 612 and $M$ corresponds to $B$, $C$ or $D$. 613 613 A more stable form of the great-circle distance formula for small distances ($x$ near 1) 614 involves the arcsine function (\eg see p.~101 of \citet{ Daley_Barker_Bk01}:614 involves the arcsine function (\eg see p.~101 of \citet{daley.barker_bk01}: 615 615 \begin{align*} 616 616 s\left( {\rm P}, {\rm M} \right) & \hspace{-2mm} = \hspace{-2mm} & \sin^{-1} \! \left\{ \sqrt{ 1 - x^2 } \right\} … … 648 648 An iterative scheme that involves first mapping a quadrilateral cell into 649 649 a cell with coordinates (0,0), (1,0), (0,1) and (1,1). 650 This method is based on the SCRIP interpolation package \citep{Jones_1998}.650 This method is based on the \href{https://github.com/SCRIP-Project/SCRIP}{SCRIP interpolation package}. 651 651 652 652 \end{enumerate} … … 744 744 where ${{\bf r}_{}}_{\rm PA}$, ${{\bf r}_{}}_{\rm PB}$, etc. correspond to 745 745 the vectors between points P and A, P and B, etc.. 746 The method used is similar to the method used in the SCRIP interpolation package \citep{Jones_1998}.746 The method used is similar to the method used in the \href{https://github.com/SCRIP-Project/SCRIP}{SCRIP interpolation package}. 747 747 748 748 In order to speed up the grid search, there is the possibility to construct a lookup table for a user specified resolution. -
NEMO/trunk/doc/latex/NEMO/subfiles/chap_SBC.tex
r10614 r11123 313 313 The only tricky point is therefore to specify the date at which we need to do the interpolation and 314 314 the date of the records read in the input files. 315 Following \citet{ Leclair_Madec_OM09}, the date of a time step is set at the middle of the time step.315 Following \citet{leclair.madec_OM09}, the date of a time step is set at the middle of the time step. 316 316 For example, for an experiment starting at 0h00'00" with a one hour time-step, 317 317 a time interpolation will be performed at the following time: 0h30'00", 1h30'00", 2h30'00", etc. … … 632 632 %------------------------------------------------------------------------------------------------------------- 633 633 634 The CORE bulk formulae have been developed by \citet{ Large_Yeager_Rep04}.634 The CORE bulk formulae have been developed by \citet{large.yeager_rpt04}. 635 635 They have been designed to handle the CORE forcing, a mixture of NCEP reanalysis and satellite data. 636 636 They use an inertial dissipative method to compute the turbulent transfer coefficients 637 637 (momentum, sensible heat and evaporation) from the 10 metre wind speed, air temperature and specific humidity. 638 This \citet{ Large_Yeager_Rep04} dataset is available through638 This \citet{large.yeager_rpt04} dataset is available through 639 639 the \href{http://nomads.gfdl.noaa.gov/nomads/forms/mom4/CORE.html}{GFDL web site}. 640 640 641 641 Note that substituting ERA40 to NCEP reanalysis fields does not require changes in the bulk formulea themself. 642 This is the so-called DRAKKAR Forcing Set (DFS) \citep{ Brodeau_al_OM09}.642 This is the so-called DRAKKAR Forcing Set (DFS) \citep{brodeau.barnier.ea_OM10}. 643 643 644 644 Options are defined through the \ngn{namsbc\_core} namelist variables. … … 696 696 697 697 The CLIO bulk formulae were developed several years ago for the Louvain-la-neuve coupled ice-ocean model 698 (CLIO, \cite{ Goosse_al_JGR99}).698 (CLIO, \cite{goosse.deleersnijder.ea_JGR99}). 699 699 They are simpler bulk formulae. 700 700 They assume the stress to be known and compute the radiative fluxes from a climatological cloud cover. … … 839 839 840 840 The SAL term should in principle be computed online as it depends on 841 the model tidal prediction itself (see \citet{ Arbic2004} for a841 the model tidal prediction itself (see \citet{arbic.garner.ea_DSR04} for a 842 842 discussion about the practical implementation of this term). 843 843 Nevertheless, the complex calculations involved would make this … … 871 871 %coastal modelling and becomes more and more often open ocean and climate modelling 872 872 %\footnote{At least a top cells thickness of 1~meter and a 3 hours forcing frequency are 873 %required to properly represent the diurnal cycle \citep{ Bernie_al_JC05}. see also \autoref{fig:SBC_dcy}.}.873 %required to properly represent the diurnal cycle \citep{bernie.woolnough.ea_JC05}. see also \autoref{fig:SBC_dcy}.}. 874 874 875 875 … … 892 892 \footnote{ 893 893 At least a top cells thickness of 1~meter and a 3 hours forcing frequency are required to 894 properly represent the diurnal cycle \citep{ Bernie_al_JC05}.894 properly represent the diurnal cycle \citep{bernie.woolnough.ea_JC05}. 895 895 see also \autoref{fig:SBC_dcy}.}. 896 896 … … 989 989 %-------------------------------------------------------------------------------------------------------- 990 990 The namelist variable in \ngn{namsbc}, \np{nn\_isf}, controls the ice shelf representation. 991 Description and result of sensitivity test to \np{nn\_isf} are presented in \citet{ Mathiot2017}.991 Description and result of sensitivity test to \np{nn\_isf} are presented in \citet{mathiot.jenkins.ea_GMD17}. 992 992 The different options are illustrated in \autoref{fig:SBC_isf}. 993 993 … … 1001 1001 \item[\np{nn\_isfblk}\forcode{ = 1}]: 1002 1002 The melt rate is based on a balance between the upward ocean heat flux and 1003 the latent heat flux at the ice shelf base. A complete description is available in \citet{ Hunter2006}.1003 the latent heat flux at the ice shelf base. A complete description is available in \citet{hunter_rpt06}. 1004 1004 \item[\np{nn\_isfblk}\forcode{ = 2}]: 1005 1005 The melt rate and the heat flux are based on a 3 equations formulation 1006 1006 (a heat flux budget at the ice base, a salt flux budget at the ice base and a linearised freezing point temperature equation). 1007 A complete description is available in \citet{ Jenkins1991}.1007 A complete description is available in \citet{jenkins_JGR91}. 1008 1008 \end{description} 1009 1009 1010 Temperature and salinity used to compute the melt are the average temperature in the top boundary layer \citet{ Losch2008}.1010 Temperature and salinity used to compute the melt are the average temperature in the top boundary layer \citet{losch_JGR08}. 1011 1011 Its thickness is defined by \np{rn\_hisf\_tbl}. 1012 1012 The fluxes and friction velocity are computed using the mean temperature, salinity and velocity in the the first \np{rn\_hisf\_tbl} m. … … 1038 1038 \] 1039 1039 where $u_{*}$ is the friction velocity in the top boundary layer (ie first \np{rn\_hisf\_tbl} meters). 1040 See \citet{ Jenkins2010} for all the details on this formulation. It is the recommended formulation for realistic application.1040 See \citet{jenkins.nicholls.ea_JPO10} for all the details on this formulation. It is the recommended formulation for realistic application. 1041 1041 \item[\np{nn\_gammablk}\forcode{ = 2}]: 1042 1042 The salt and heat exchange coefficients are velocity and stability dependent and defined as: … … 1047 1047 $\Gamma_{Turb}$ the contribution of the ocean stability and 1048 1048 $\Gamma^{T,S}_{Mole}$ the contribution of the molecular diffusion. 1049 See \citet{ Holland1999} for all the details on this formulation.1049 See \citet{holland.jenkins_JPO99} for all the details on this formulation. 1050 1050 This formulation has not been extensively tested in NEMO (not recommended). 1051 1051 \end{description} 1052 1052 \item[\np{nn\_isf}\forcode{ = 2}]: 1053 1053 The ice shelf cavity is not represented. 1054 The fwf and heat flux are computed using the \citet{ Beckmann2003} parameterisation of isf melting.1054 The fwf and heat flux are computed using the \citet{beckmann.goosse_OM03} parameterisation of isf melting. 1055 1055 The fluxes are distributed along the ice shelf edge between the depth of the average grounding line (GL) 1056 1056 (\np{sn\_depmax\_isf}) and the base of the ice shelf along the calving front … … 1166 1166 %------------------------------------------------------------------------------------------------------------- 1167 1167 1168 Icebergs are modelled as lagrangian particles in NEMO \citep{ Marsh_GMD2015}.1169 Their physical behaviour is controlled by equations as described in \citet{ Martin_Adcroft_OM10} ).1168 Icebergs are modelled as lagrangian particles in NEMO \citep{marsh.ivchenko.ea_GMD15}. 1169 Their physical behaviour is controlled by equations as described in \citet{martin.adcroft_OM10} ). 1170 1170 (Note that the authors kindly provided a copy of their code to act as a basis for implementation in NEMO). 1171 1171 Icebergs are initially spawned into one of ten classes which have specific mass and thickness as … … 1265 1265 Then using the routine \rou{turb\_ncar} and starting from the neutral drag coefficent provided, 1266 1266 the drag coefficient is computed according to the stable/unstable conditions of the 1267 air-sea interface following \citet{ Large_Yeager_Rep04}.1267 air-sea interface following \citet{large.yeager_rpt04}. 1268 1268 1269 1269 … … 1274 1274 \label{subsec:SBC_wave_sdw} 1275 1275 1276 The Stokes drift is a wave driven mechanism of mass and momentum transport \citep{ Stokes_1847}.1276 The Stokes drift is a wave driven mechanism of mass and momentum transport \citep{stokes_ibk09}. 1277 1277 It is defined as the difference between the average velocity of a fluid parcel (Lagrangian velocity) 1278 1278 and the current measured at a fixed point (Eulerian velocity). … … 1307 1307 \begin{description} 1308 1308 \item[\np{nn\_sdrift} = 0]: exponential integral profile parameterization proposed by 1309 \citet{ Breivik_al_JPO2014}:1309 \citet{breivik.janssen.ea_JPO14}: 1310 1310 1311 1311 \[ … … 1327 1327 \item[\np{nn\_sdrift} = 1]: velocity profile based on the Phillips spectrum which is considered to be a 1328 1328 reasonable estimate of the part of the spectrum most contributing to the Stokes drift velocity near the surface 1329 \citep{ Breivik_al_OM2016}:1329 \citep{breivik.bidlot.ea_OM16}: 1330 1330 1331 1331 \[ … … 1385 1385 1386 1386 The surface stress felt by the ocean is the atmospheric stress minus the net stress going 1387 into the waves \citep{ Janssen_al_TM13}. Therefore, when waves are growing, momentum and energy is spent and is not1387 into the waves \citep{janssen.breivik.ea_rpt13}. Therefore, when waves are growing, momentum and energy is spent and is not 1388 1388 available for forcing the mean circulation, while in the opposite case of a decaying sea 1389 1389 state more momentum is available for forcing the ocean. … … 1445 1445 the mean value of the analytical cycle (blue line) over a time step, 1446 1446 not as the mid time step value of the analytically cycle (red square). 1447 From \citet{ Bernie_al_CD07}.1447 From \citet{bernie.guilyardi.ea_CD07}. 1448 1448 } 1449 1449 \end{center} … … 1451 1451 %>>>>>>>>>>>>>>>>>>>>>>>>>>>> 1452 1452 1453 \cite{ Bernie_al_JC05} have shown that to capture 90$\%$ of the diurnal variability of SST requires a vertical resolution in upper ocean of 1~m or better and a temporal resolution of the surface fluxes of 3~h or less.1453 \cite{bernie.woolnough.ea_JC05} have shown that to capture 90$\%$ of the diurnal variability of SST requires a vertical resolution in upper ocean of 1~m or better and a temporal resolution of the surface fluxes of 3~h or less. 1454 1454 Unfortunately high frequency forcing fields are rare, not to say inexistent. 1455 1455 Nevertheless, it is possible to obtain a reasonable diurnal cycle of the SST knowning only short wave flux (SWF) at 1456 high frequency \citep{ Bernie_al_CD07}.1456 high frequency \citep{bernie.guilyardi.ea_CD07}. 1457 1457 Furthermore, only the knowledge of daily mean value of SWF is needed, 1458 1458 as higher frequency variations can be reconstructed from them, 1459 1459 assuming that the diurnal cycle of SWF is a scaling of the top of the atmosphere diurnal cycle of incident SWF. 1460 The \cite{ Bernie_al_CD07} reconstruction algorithm is available in \NEMO by1460 The \cite{bernie.guilyardi.ea_CD07} reconstruction algorithm is available in \NEMO by 1461 1461 setting \np{ln\_dm2dc}\forcode{ = .true.} (a \textit{\ngn{namsbc}} namelist variable) when 1462 1462 using CORE bulk formulea (\np{ln\_blk\_core}\forcode{ = .true.}) or 1463 1463 the flux formulation (\np{ln\_flx}\forcode{ = .true.}). 1464 1464 The reconstruction is performed in the \mdl{sbcdcy} module. 1465 The detail of the algoritm used can be found in the appendix~A of \cite{ Bernie_al_CD07}.1465 The detail of the algoritm used can be found in the appendix~A of \cite{bernie.guilyardi.ea_CD07}. 1466 1466 The algorithm preserve the daily mean incoming SWF as the reconstructed SWF at 1467 1467 a given time step is the mean value of the analytical cycle over this time step (\autoref{fig:SBC_diurnal}). … … 1546 1546 (observed, climatological or an atmospheric model product), 1547 1547 \textit{SSS}$_{Obs}$ is a sea surface salinity 1548 (usually a time interpolation of the monthly mean Polar Hydrographic Climatology \citep{ Steele2001}),1548 (usually a time interpolation of the monthly mean Polar Hydrographic Climatology \citep{steele.morley.ea_JC01}), 1549 1549 $\left.S\right|_{k=1}$ is the model surface layer salinity and 1550 1550 $\gamma_s$ is a negative feedback coefficient which is provided as a namelist parameter. 1551 1551 Unlike heat flux, there is no physical justification for the feedback term in \autoref{eq:sbc_dmp_emp} as 1552 the atmosphere does not care about ocean surface salinity \citep{ Madec1997}.1552 the atmosphere does not care about ocean surface salinity \citep{madec.delecluse_IWN97}. 1553 1553 The SSS restoring term should be viewed as a flux correction on freshwater fluxes to 1554 1554 reduce the uncertainties we have on the observed freshwater budget. -
NEMO/trunk/doc/latex/NEMO/subfiles/chap_STO.tex
r10442 r11123 15 15 16 16 The stochastic parametrization module aims to explicitly simulate uncertainties in the model. 17 More particularly, \cite{ Brankart_OM2013} has shown that,17 More particularly, \cite{brankart_OM13} has shown that, 18 18 because of the nonlinearity of the seawater equation of state, unresolved scales represent a major source of 19 19 uncertainties in the computation of the large scale horizontal density gradient (from T/S large scale fields), … … 46 46 A generic approach is thus to add one single new module in NEMO, 47 47 generating processes with appropriate statistics to simulate each kind of uncertainty in the model 48 (see \cite{ Brankart_al_GMD2015} for more details).48 (see \cite{brankart.candille.ea_GMD15} for more details). 49 49 50 50 In practice, at every model grid point, -
NEMO/trunk/doc/latex/NEMO/subfiles/chap_TRA.tex
r10544 r11123 136 136 Nevertheless, in the latter case, it is achieved to a good approximation since 137 137 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 }) is138 two quantities that are not correlated \citep{roullet.madec_JGR00, griffies.pacanowski.ea_MWR01, campin.adcroft.ea_OM04}. 139 140 The velocity field that appears in (\autoref{eq:tra_adv} and \autoref{eq:tra_adv_zco?}) is 141 141 the centred (\textit{now}) \textit{effective} ocean velocity, \ie the \textit{eulerian} velocity 142 142 (see \autoref{chap:DYN}) plus the eddy induced velocity (\textit{eiv}) and/or … … 221 221 \end{equation} 222 222 In the vertical direction (\np{nn\_cen\_v}~\forcode{= 4}), 223 a $4^{th}$ COMPACT interpolation has been prefered \citep{ Demange_PhD2014}.223 a $4^{th}$ COMPACT interpolation has been prefered \citep{demange_phd14}. 224 224 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}.225 spectral characteristics similar to schemes of higher order \citep{lele_JCP92}. 226 226 227 227 Strictly speaking, the CEN4 scheme is not a $4^{th}$ order advection scheme but … … 277 277 (\ie it depends on the setting of \np{nn\_fct\_h} and \np{nn\_fct\_v}). 278 278 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}.279 The one chosen in \NEMO is described in \citet{zalesak_JCP79}. 280 280 $c_u$ only departs from $1$ when the advective term produces a local extremum in the tracer field. 281 281 The resulting scheme is quite expensive but \textit{positive}. 282 282 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}.283 A comparison of FCT-2 with MUSCL and a MPDATA scheme can be found in \citet{levy.estublier.ea_GRL01}. 284 284 285 285 An additional option has been added controlled by \np{nn\_fct\_zts}. … … 287 287 a $2^{nd}$ order FCT scheme is used on both horizontal and vertical direction, but on the latter, 288 288 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}.289 This option can be useful when the size of the timestep is limited by vertical advection \citep{lemarie.debreu.ea_OM15}. 290 290 Note that in this case, a similar split-explicit time stepping should be used on vertical advection of momentum to 291 291 insure a better stability (see \autoref{subsec:DYN_zad}). … … 306 306 MUSCL implementation can be found in the \mdl{traadv\_mus} module. 307 307 308 MUSCL has been first implemented in \NEMO by \citet{ Levy_al_GRL01}.308 MUSCL has been first implemented in \NEMO by \citet{levy.estublier.ea_GRL01}. 309 309 In its formulation, the tracer at velocity points is evaluated assuming a linear tracer variation between 310 310 two $T$-points (\autoref{fig:adv_scheme}). … … 358 358 359 359 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}.360 \citep{shchepetkin.mcwilliams_OM05}. 361 The overall performance of the advection scheme is similar to that reported in \cite{farrow.stevens_JPO95}. 362 362 It is a relatively good compromise between accuracy and smoothness. 363 363 Nevertheless the scheme is not \textit{positive}, meaning that false extrema are permitted, … … 367 367 The intrinsic diffusion of UBS makes its use risky in the vertical direction where 368 368 the control of artificial diapycnal fluxes is of paramount importance 369 \citep{ Shchepetkin_McWilliams_OM05, Demange_PhD2014}.369 \citep{shchepetkin.mcwilliams_OM05, demange_phd14}. 370 370 Therefore the vertical flux is evaluated using either a $2^nd$ order FCT scheme or a $4^th$ order COMPACT scheme 371 371 (\np{nn\_cen\_v}~\forcode{= 2 or 4}). … … 376 376 (which is the diffusive part of the scheme), 377 377 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.378 This choice is discussed by \citet{webb.de-cuevas.ea_JAOT98} in the context of the QUICK advection scheme. 379 379 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}.380 Replacing 1/6 with 1/8 in \autoref{eq:tra_adv_ubs} leads to the QUICK advection scheme \citep{webb.de-cuevas.ea_JAOT98}. 381 381 This option is not available through a namelist parameter, since the 1/6 coefficient is hard coded. 382 382 Nevertheless it is quite easy to make the substitution in the \mdl{traadv\_ubs} module and obtain a QUICK scheme. … … 412 412 413 413 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.}.414 proposed by \citet{leonard_CMAME79} is used when \np{ln\_traadv\_qck}~\forcode{= .true.}. 415 415 QUICKEST implementation can be found in the \mdl{traadv\_qck} module. 416 416 417 417 QUICKEST is the third order Godunov scheme which is associated with the ULTIMATE QUICKEST limiter 418 \citep{ Leonard1991}.418 \citep{leonard_CMAME91}. 419 419 It has been implemented in NEMO by G. Reffray (MERCATOR-ocean) and can be found in the \mdl{traadv\_qck} module. 420 420 The resulting scheme is quite expensive but \textit{positive}. … … 454 454 This latter component is solved implicitly together with the vertical diffusion term (see \autoref{chap:STP}). 455 455 When \np{ln\_traldf\_msc}~\forcode{= .true.}, a Method of Stabilizing Correction is used in which 456 the pure vertical component is split into an explicit and an implicit part \citep{ Lemarie_OM2012}.456 the pure vertical component is split into an explicit and an implicit part \citep{lemarie.debreu.ea_OM12}. 457 457 458 458 % ------------------------------------------------------------------------------------------------------------- … … 590 590 This formulation conserves the tracer but does not ensure the decrease of the tracer variance. 591 591 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}.592 any additional background horizontal diffusion \citep{guilyardi.madec.ea_CD01}. 593 593 594 594 Note that in the partial step $z$-coordinate (\np{ln\_zps}~\forcode{= .true.}), … … 603 603 If the Griffies triad scheme is employed (\np{ln\_traldf\_triad}~\forcode{= .true.}; see \autoref{apdx:triad}) 604 604 605 An alternative scheme developed by \cite{ Griffies_al_JPO98} which ensures tracer variance decreases605 An alternative scheme developed by \cite{griffies.gnanadesikan.ea_JPO98} which ensures tracer variance decreases 606 606 is also available in \NEMO (\np{ln\_traldf\_grif}~\forcode{= .true.}). 607 607 A complete description of the algorithm is given in \autoref{apdx:triad}. … … 747 747 Note that an exact conservation of heat and salt content is only achieved with non-linear free surface. 748 748 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}.749 The imbalance is larger than the imbalance associated with the Asselin time filter \citep{leclair.madec_OM09}. 750 750 This is the reason why the modified filter is not applied in the linear free surface case (see \autoref{chap:STP}). 751 751 … … 794 794 In the simple 2-waveband light penetration scheme (\np{ln\_qsr\_2bd}~\forcode{= .true.}) 795 795 a chlorophyll-independent monochromatic formulation is chosen for the shorter wavelengths, 796 leading to the following expression \citep{ Paulson1977}:796 leading to the following expression \citep{paulson.simpson_JPO77}: 797 797 \[ 798 798 % \label{eq:traqsr_iradiance} … … 805 805 806 806 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}).807 observed light penetration profiles (\cite{morel_JGR88}, see also \autoref{fig:traqsr_irradiance}). 808 808 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 by809 \cite{morel_JGR88} has shown that an accurate representation of light penetration can be provided by 810 810 a 61 waveband formulation. 811 811 Unfortunately, such a model is very computationally expensive. 812 Thus, \cite{ Lengaigne_al_CD07} have constructed a simplified version of this formulation in which812 Thus, \cite{lengaigne.menkes.ea_CD07} have constructed a simplified version of this formulation in which 813 813 visible light is split into three wavebands: blue (400-500 nm), green (500-600 nm) and red (600-700nm). 814 814 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}),815 the full spectral model of \cite{morel_JGR88} (as modified by \cite{morel.maritorena_JGR01}), 816 816 assuming the same power-law relationship. 817 817 As shown in \autoref{fig:traqsr_irradiance}, this formulation, called RGB (Red-Green-Blue), … … 834 834 \item[\np{nn\_chdta}~\forcode{= 2}] 835 835 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;836 Following \cite{morel.berthon_LO89}, the profile is computed from the local surface chlorophyll value; 837 837 \item[\np{ln\_qsr\_bio}~\forcode{= .true.}] 838 838 simulated time varying chlorophyll by TOP biogeochemical model. … … 865 865 61 waveband Morel (1988) formulation (black) for a chlorophyll concentration of 866 866 (a) Chl=0.05 mg/m$^3$ and (b) Chl=0.5 mg/m$^3$. 867 From \citet{ Lengaigne_al_CD07}.867 From \citet{lengaigne.menkes.ea_CD07}. 868 868 } 869 869 \end{center} … … 886 886 \caption{ 887 887 \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}.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_N92}. 890 890 } 891 891 \end{center} … … 897 897 This is the default option in \NEMO, and it is implemented using the masking technique. 898 898 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}),899 This flux is weak compared to surface fluxes (a mean global value of $\sim 0.1 \, W/m^2$ \citep{stein.stein_N92}), 900 900 but it warms systematically the ocean and acts on the densest water masses. 901 901 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}.902 (\ie the one associated with the Antarctic Bottom Water) by a few Sverdrups \citep{emile-geay.madec_OS09}. 903 903 904 904 Options are defined through the \ngn{namtra\_bbc} namelist variables. … … 907 907 the \np{nn\_geoflx\_cst}, which is also a namelist parameter. 908 908 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}.909 the \ifile{geothermal\_heating} NetCDF file (\autoref{fig:geothermal}) \citep{emile-geay.madec_OS09}. 910 910 911 911 % ================================================================ … … 931 931 sometimes over a thickness much larger than the thickness of the observed gravity plume. 932 932 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},933 a sill \citep{willebrand.barnier.ea_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.doscher_JPO97}, 936 936 is to allow a direct communication between two adjacent bottom cells at different levels, 937 937 whenever the densest water is located above the less dense water. … … 939 939 In the current implementation of the BBL, only the tracers are modified, not the velocities. 940 940 Furthermore, it only connects ocean bottom cells, and therefore does not include all the improvements introduced by 941 \citet{ Campin_Goosse_Tel99}.941 \citet{campin.goosse_T99}. 942 942 943 943 % ------------------------------------------------------------------------------------------------------------- … … 955 955 with $\nabla_\sigma$ the lateral gradient operator taken between bottom cells, and 956 956 $A_l^\sigma$ the lateral diffusivity in the BBL. 957 Following \citet{ Beckmann_Doscher1997}, the latter is prescribed with a spatial dependence,957 Following \citet{beckmann.doscher_JPO97}, the latter is prescribed with a spatial dependence, 958 958 \ie in the conditional form 959 959 \begin{equation} … … 1020 1020 \np{nn\_bbl\_adv}~\forcode{= 1}: 1021 1021 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}.1022 (see black arrow in \autoref{fig:bbl}) \citep{beckmann.doscher_JPO97}. 1023 1023 It is a \textit{conditional advection}, that is, advection is allowed only 1024 1024 if dense water overlies less dense water on the slope (\ie $\nabla_\sigma \rho \cdot \nabla H < 0$) and … … 1027 1027 \np{nn\_bbl\_adv}~\forcode{= 2}: 1028 1028 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}.1029 the density difference between the higher cell and lower cell densities \citep{campin.goosse_T99}. 1030 1030 The advection is allowed only if dense water overlies less dense water on the slope 1031 1031 (\ie $\nabla_\sigma \rho \cdot \nabla H < 0$). … … 1041 1041 The parameter $\gamma$ should take a different value for each bathymetric step, but for simplicity, 1042 1042 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}.1043 The possible values for $\gamma$ range between 1 and $10~s$ \citep{campin.goosse_T99}. 1044 1044 1045 1045 Scalar properties are advected by this additional transport $(u^{tr}_{bbl},v^{tr}_{bbl})$ using the upwind scheme. … … 1109 1109 In the vicinity of these walls, $\gamma$ takes large values (equivalent to a time scale of a few days) whereas 1110 1110 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}.1111 The second case corresponds to the use of the robust diagnostic method \citep{sarmiento.bryan_JGR82}. 1112 1112 It allows us to find the velocity field consistent with the model dynamics whilst 1113 1113 having a $T$, $S$ field close to a given climatological field ($T_o$, $S_o$). … … 1121 1121 only below the mixed layer (defined either on a density or $S_o$ criterion). 1122 1122 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}.1123 \citep{madec.delecluse.ea_JPO96}. 1124 1124 1125 1125 For generating \ifile{resto}, see the documentation for the DMP tool provided with the source code under … … 1137 1137 1138 1138 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},1139 The general framework for tracer time stepping is a modified leap-frog scheme \citep{leclair.madec_OM09}, 1140 1140 \ie a three level centred time scheme associated with a Asselin time filter (cf. \autoref{sec:STP_mLF}): 1141 1141 \begin{equation} … … 1186 1186 Nonlinearities of the EOS are of major importance, in particular influencing the circulation through 1187 1187 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}.1188 thus controlling rates of exchange between the atmosphere and the ocean interior \citep{roquet.madec.ea_JPO15}. 1189 Therefore an accurate EOS based on either the 1980 equation of state (EOS-80, \cite{fofonoff.millard_bk83}) or 1190 TEOS-10 \citep{ioc.iapso_bk10} standards should be used anytime a simulation of the real ocean circulation is attempted 1191 \citep{roquet.madec.ea_JPO15}. 1192 1192 The use of TEOS-10 is highly recommended because 1193 1193 \textit{(i)} it is the new official EOS, … … 1195 1195 \textit{(iii)} it uses Conservative Temperature and Absolute Salinity (instead of potential temperature and 1196 1196 practical salinity for EOS-980, both variables being more suitable for use as model variables 1197 \citep{ TEOS10, Graham_McDougall_JPO13}.1197 \citep{ioc.iapso_bk10, graham.mcdougall_JPO13}. 1198 1198 EOS-80 is an obsolescent feature of the NEMO system, kept only for backward compatibility. 1199 1199 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.1200 To that purposed, a simplified EOS (S-EOS) inspired by \citet{vallis_bk06} is also available. 1201 1201 1202 1202 In the computer code, a density anomaly, $d_a = \rho / \rho_o - 1$, is computed, with $\rho_o$ a reference density. … … 1204 1204 This is a sensible choice for the reference density used in a Boussinesq ocean climate model, as, 1205 1205 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}.1206 density in the World Ocean varies by no more than 2$\%$ from that value \citep{gill_bk82}. 1207 1207 1208 1208 Options are defined through the \ngn{nameos} namelist variables, and in particular \np{nn\_eos} which … … 1211 1211 \begin{description} 1212 1212 \item[\np{nn\_eos}~\forcode{= -1}] 1213 the polyTEOS10-bsq equation of seawater \citep{ Roquet_OM2015} is used.1213 the polyTEOS10-bsq equation of seawater \citep{roquet.madec.ea_OM15} is used. 1214 1214 The accuracy of this approximation is comparable to the TEOS-10 rational function approximation, 1215 1215 but it is optimized for a boussinesq fluid and the polynomial expressions have simpler and … … 1217 1217 use in ocean models. 1218 1218 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}.1219 the TEOS-10 rational function approximation for hydrographic data analysis \citep{ioc.iapso_bk10}. 1220 1220 A key point is that conservative state variables are used: 1221 1221 Absolute Salinity (unit: g/kg, notation: $S_A$) and Conservative Temperature (unit: \deg{C}, notation: $\Theta$). 1222 1222 The pressure in decibars is approximated by the depth in meters. 1223 1223 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}.1224 It is set to $C_p = 3991.86795711963~J\,Kg^{-1}\,^{\circ}K^{-1}$, according to \citet{ioc.iapso_bk10}. 1225 1225 Choosing polyTEOS10-bsq implies that the state variables used by the model are $\Theta$ and $S_A$. 1226 1226 In particular, the initial state deined by the user have to be given as \textit{Conservative} Temperature and … … 1238 1238 The pressure in decibars is approximated by the depth in meters. 1239 1239 With thsi EOS, the specific heat capacity of sea water, $C_p$, is a function of temperature, salinity and 1240 pressure \citep{ UNESCO1983}.1240 pressure \citep{fofonoff.millard_bk83}. 1241 1241 Nevertheless, a severe assumption is made in order to have a heat content ($C_p T_p$) which 1242 1242 is conserved by the model: $C_p$ is set to a constant value, the TEOS10 value. 1243 1243 \item[\np{nn\_eos}~\forcode{= 1}] 1244 a simplified EOS (S-EOS) inspired by \citet{ Vallis06} is chosen,1244 a simplified EOS (S-EOS) inspired by \citet{vallis_bk06} is chosen, 1245 1245 the coefficients of which has been optimized to fit the behavior of TEOS10 1246 (Roquet, personal comm.) (see also \citet{ Roquet_JPO2015}).1246 (Roquet, personal comm.) (see also \citet{roquet.madec.ea_JPO15}). 1247 1247 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}.1248 is enough for a proper treatment of the EOS in theoretical studies \citep{roquet.madec.ea_JPO15}. 1249 1249 With such an equation of state there is no longer a distinction between 1250 1250 \textit{conservative} and \textit{potential} temperature, … … 1329 1329 \label{subsec:TRA_fzp} 1330 1330 1331 The freezing point of seawater is a function of salinity and pressure \citep{ UNESCO1983}:1331 The freezing point of seawater is a function of salinity and pressure \citep{fofonoff.millard_bk83}: 1332 1332 \begin{equation} 1333 1333 \label{eq:tra_eos_fzp} -
NEMO/trunk/doc/latex/NEMO/subfiles/chap_ZDF.tex
r10442 r11123 87 87 a dependency between the vertical eddy coefficients and the local Richardson number 88 88 (\ie the ratio of stratification to vertical shear). 89 Following \citet{ Pacanowski_Philander_JPO81}, the following formulation has been implemented:89 Following \citet{pacanowski.philander_JPO81}, the following formulation has been implemented: 90 90 \[ 91 91 % \label{eq:zdfric} … … 124 124 The final $h_{e}$ is further constrained by the adjustable bounds \np{rn\_mldmin} and \np{rn\_mldmax}. 125 125 Once $h_{e}$ is computed, the vertical eddy coefficients within $h_{e}$ are set to 126 the empirical values \np{rn\_wtmix} and \np{rn\_wvmix} \citep{ Lermusiaux2001}.126 the empirical values \np{rn\_wtmix} and \np{rn\_wvmix} \citep{lermusiaux_JMS01}. 127 127 128 128 % ------------------------------------------------------------------------------------------------------------- … … 140 140 a prognostic equation for $\bar{e}$, the turbulent kinetic energy, 141 141 and a closure assumption for the turbulent length scales. 142 This turbulent closure model has been developed by \citet{ Bougeault1989} in the atmospheric case,143 adapted by \citet{ Gaspar1990} for the oceanic case, and embedded in OPA, the ancestor of NEMO,144 by \citet{ Blanke1993} for equatorial Atlantic simulations.145 Since then, significant modifications have been introduced by \citet{ Madec1998} in both the implementation and142 This turbulent closure model has been developed by \citet{bougeault.lacarrere_MWR89} in the atmospheric case, 143 adapted by \citet{gaspar.gregoris.ea_JGR90} for the oceanic case, and embedded in OPA, the ancestor of NEMO, 144 by \citet{blanke.delecluse_JPO93} for equatorial Atlantic simulations. 145 Since then, significant modifications have been introduced by \citet{madec.delecluse.ea_NPM98} in both the implementation and 146 146 the formulation of the mixing length scale. 147 147 The time evolution of $\bar{e}$ is the result of the production of $\bar{e}$ through vertical shear, 148 its destruction through stratification, its vertical diffusion, and its dissipation of \citet{ Kolmogorov1942} type:148 its destruction through stratification, its vertical diffusion, and its dissipation of \citet{kolmogorov_IANS42} type: 149 149 \begin{equation} 150 150 \label{eq:zdftke_e} … … 168 168 $P_{rt}$ is the Prandtl number, $K_m$ and $K_\rho$ are the vertical eddy viscosity and diffusivity coefficients. 169 169 The constants $C_k = 0.1$ and $C_\epsilon = \sqrt {2} /2$ $\approx 0.7$ are designed to deal with 170 vertical mixing at any depth \citep{ Gaspar1990}.170 vertical mixing at any depth \citep{gaspar.gregoris.ea_JGR90}. 171 171 They are set through namelist parameters \np{nn\_ediff} and \np{nn\_ediss}. 172 $P_{rt}$ can be set to unity or, following \citet{ Blanke1993}, be a function of the local Richardson number, $R_i$:172 $P_{rt}$ can be set to unity or, following \citet{blanke.delecluse_JPO93}, be a function of the local Richardson number, $R_i$: 173 173 \begin{align*} 174 174 % \label{eq:prt} … … 185 185 At the sea surface, the value of $\bar{e}$ is prescribed from the wind stress field as 186 186 $\bar{e}_o = e_{bb} |\tau| / \rho_o$, with $e_{bb}$ the \np{rn\_ebb} namelist parameter. 187 The default value of $e_{bb}$ is 3.75. \citep{ Gaspar1990}), however a much larger value can be used when187 The default value of $e_{bb}$ is 3.75. \citep{gaspar.gregoris.ea_JGR90}), however a much larger value can be used when 188 188 taking into account the surface wave breaking (see below Eq. \autoref{eq:ZDF_Esbc}). 189 189 The bottom value of TKE is assumed to be equal to the value of the level just above. … … 191 191 the numerical scheme does not ensure its positivity. 192 192 To overcome this problem, a cut-off in the minimum value of $\bar{e}$ is used (\np{rn\_emin} namelist parameter). 193 Following \citet{ Gaspar1990}, the cut-off value is set to $\sqrt{2}/2~10^{-6}~m^2.s^{-2}$.194 This allows the subsequent formulations to match that of \citet{ Gargett1984} for the diffusion in193 Following \citet{gaspar.gregoris.ea_JGR90}, the cut-off value is set to $\sqrt{2}/2~10^{-6}~m^2.s^{-2}$. 194 This allows the subsequent formulations to match that of \citet{gargett_JMR84} for the diffusion in 195 195 the thermocline and deep ocean : $K_\rho = 10^{-3} / N$. 196 196 In addition, a cut-off is applied on $K_m$ and $K_\rho$ to avoid numerical instabilities associated with … … 202 202 203 203 For computational efficiency, the original formulation of the turbulent length scales proposed by 204 \citet{ Gaspar1990} has been simplified.204 \citet{gaspar.gregoris.ea_JGR90} has been simplified. 205 205 Four formulations are proposed, the choice of which is controlled by the \np{nn\_mxl} namelist parameter. 206 The first two are based on the following first order approximation \citep{ Blanke1993}:206 The first two are based on the following first order approximation \citep{blanke.delecluse_JPO93}: 207 207 \begin{equation} 208 208 \label{eq:tke_mxl0_1} … … 212 212 The resulting length scale is bounded by the distance to the surface or to the bottom 213 213 (\np{nn\_mxl}\forcode{ = 0}) or by the local vertical scale factor (\np{nn\_mxl}\forcode{ = 1}). 214 \citet{ Blanke1993} notice that this simplification has two major drawbacks:214 \citet{blanke.delecluse_JPO93} notice that this simplification has two major drawbacks: 215 215 it makes no sense for locally unstable stratification and the computation no longer uses all 216 216 the information contained in the vertical density profile. 217 To overcome these drawbacks, \citet{ Madec1998} introduces the \np{nn\_mxl}\forcode{ = 2..3} cases,217 To overcome these drawbacks, \citet{madec.delecluse.ea_NPM98} introduces the \np{nn\_mxl}\forcode{ = 2..3} cases, 218 218 which add an extra assumption concerning the vertical gradient of the computed length scale. 219 219 So, the length scales are first evaluated as in \autoref{eq:tke_mxl0_1} and then bounded such that: … … 225 225 \autoref{eq:tke_mxl_constraint} means that the vertical variations of the length scale cannot be larger than 226 226 the variations of depth. 227 It provides a better approximation of the \citet{ Gaspar1990} formulation while being much less227 It provides a better approximation of the \citet{gaspar.gregoris.ea_JGR90} formulation while being much less 228 228 time consuming. 229 229 In particular, it allows the length scale to be limited not only by the distance to the surface or … … 258 258 In the \np{nn\_mxl}\forcode{ = 2} case, the dissipation and mixing length scales take the same value: 259 259 $ l_k= l_\epsilon = \min \left(\ l_{up} \;,\; l_{dwn}\ \right)$, while in the \np{nn\_mxl}\forcode{ = 3} case, 260 the dissipation and mixing turbulent length scales are give as in \citet{ Gaspar1990}:260 the dissipation and mixing turbulent length scales are give as in \citet{gaspar.gregoris.ea_JGR90}: 261 261 \[ 262 262 % \label{eq:tke_mxl_gaspar} … … 270 270 Usually the surface scale is given by $l_o = \kappa \,z_o$ where $\kappa = 0.4$ is von Karman's constant and 271 271 $z_o$ the roughness parameter of the surface. 272 Assuming $z_o=0.1$~m \citep{ Craig_Banner_JPO94} leads to a 0.04~m, the default value of \np{rn\_mxl0}.272 Assuming $z_o=0.1$~m \citep{craig.banner_JPO94} leads to a 0.04~m, the default value of \np{rn\_mxl0}. 273 273 In the ocean interior a minimum length scale is set to recover the molecular viscosity when 274 274 $\bar{e}$ reach its minimum value ($1.10^{-6}= C_k\, l_{min} \,\sqrt{\bar{e}_{min}}$ ). … … 277 277 %-----------------------------------------------------------------------% 278 278 279 Following \citet{ Mellor_Blumberg_JPO04}, the TKE turbulence closure model has been modified to279 Following \citet{mellor.blumberg_JPO04}, the TKE turbulence closure model has been modified to 280 280 include the effect of surface wave breaking energetics. 281 281 This results in a reduction of summertime surface temperature when the mixed layer is relatively shallow. 282 The \citet{ Mellor_Blumberg_JPO04} modifications acts on surface length scale and TKE values and282 The \citet{mellor.blumberg_JPO04} modifications acts on surface length scale and TKE values and 283 283 air-sea drag coefficient. 284 284 The latter concerns the bulk formulea and is not discussed here. 285 285 286 Following \citet{ Craig_Banner_JPO94}, the boundary condition on surface TKE value is :286 Following \citet{craig.banner_JPO94}, the boundary condition on surface TKE value is : 287 287 \begin{equation} 288 288 \label{eq:ZDF_Esbc} 289 289 \bar{e}_o = \frac{1}{2}\,\left( 15.8\,\alpha_{CB} \right)^{2/3} \,\frac{|\tau|}{\rho_o} 290 290 \end{equation} 291 where $\alpha_{CB}$ is the \citet{ Craig_Banner_JPO94} constant of proportionality which depends on the ''wave age'',292 ranging from 57 for mature waves to 146 for younger waves \citep{ Mellor_Blumberg_JPO04}.291 where $\alpha_{CB}$ is the \citet{craig.banner_JPO94} constant of proportionality which depends on the ''wave age'', 292 ranging from 57 for mature waves to 146 for younger waves \citep{mellor.blumberg_JPO04}. 293 293 The boundary condition on the turbulent length scale follows the Charnock's relation: 294 294 \begin{equation} … … 297 297 \end{equation} 298 298 where $\kappa=0.40$ is the von Karman constant, and $\beta$ is the Charnock's constant. 299 \citet{ Mellor_Blumberg_JPO04} suggest $\beta = 2.10^{5}$ the value chosen by300 \citet{ Stacey_JPO99} citing observation evidence, and299 \citet{mellor.blumberg_JPO04} suggest $\beta = 2.10^{5}$ the value chosen by 300 \citet{stacey_JPO99} citing observation evidence, and 301 301 $\alpha_{CB} = 100$ the Craig and Banner's value. 302 302 As the surface boundary condition on TKE is prescribed through $\bar{e}_o = e_{bb} |\tau| / \rho_o$, … … 315 315 Although LC have nothing to do with convection, the circulation pattern is rather similar to 316 316 so-called convective rolls in the atmospheric boundary layer. 317 The detailed physics behind LC is described in, for example, \citet{ Craik_Leibovich_JFM76}.317 The detailed physics behind LC is described in, for example, \citet{craik.leibovich_JFM76}. 318 318 The prevailing explanation is that LC arise from a nonlinear interaction between the Stokes drift and 319 319 wind drift currents. 320 320 321 321 Here we introduced in the TKE turbulent closure the simple parameterization of Langmuir circulations proposed by 322 \citep{ Axell_JGR02} for a $k-\epsilon$ turbulent closure.322 \citep{axell_JGR02} for a $k-\epsilon$ turbulent closure. 323 323 The parameterization, tuned against large-eddy simulation, includes the whole effect of LC in 324 324 an extra source terms of TKE, $P_{LC}$. … … 326 326 \forcode{.true.} in the namtke namelist. 327 327 328 By making an analogy with the characteristic convective velocity scale (\eg, \citet{ D'Alessio_al_JPO98}),328 By making an analogy with the characteristic convective velocity scale (\eg, \citet{dalessio.abdella.ea_JPO98}), 329 329 $P_{LC}$ is assumed to be : 330 330 \[ … … 334 334 With no information about the wave field, $w_{LC}$ is assumed to be proportional to 335 335 the Stokes drift $u_s = 0.377\,\,|\tau|^{1/2}$, where $|\tau|$ is the surface wind stress module 336 \footnote{Following \citet{ Li_Garrett_JMR93}, the surface Stoke drift velocity may be expressed as336 \footnote{Following \citet{li.garrett_JMR93}, the surface Stoke drift velocity may be expressed as 337 337 $u_s = 0.016 \,|U_{10m}|$. 338 338 Assuming an air density of $\rho_a=1.22 \,Kg/m^3$ and a drag coefficient of … … 350 350 \end{cases} 351 351 \] 352 where $c_{LC} = 0.15$ has been chosen by \citep{ Axell_JGR02} as a good compromise to fit LES data.352 where $c_{LC} = 0.15$ has been chosen by \citep{axell_JGR02} as a good compromise to fit LES data. 353 353 The chosen value yields maximum vertical velocities $w_{LC}$ of the order of a few centimeters per second. 354 354 The value of $c_{LC}$ is set through the \np{rn\_lc} namelist parameter, 355 having in mind that it should stay between 0.15 and 0.54 \citep{ Axell_JGR02}.355 having in mind that it should stay between 0.15 and 0.54 \citep{axell_JGR02}. 356 356 357 357 The $H_{LC}$ is estimated in a similar way as the turbulent length scale of TKE equations: … … 368 368 produce mixed-layer depths that are too shallow during summer months and windy conditions. 369 369 This bias is particularly acute over the Southern Ocean. 370 To overcome this systematic bias, an ad hoc parameterization is introduced into the TKE scheme \cite{ Rodgers_2014}.370 To overcome this systematic bias, an ad hoc parameterization is introduced into the TKE scheme \cite{rodgers.aumont.ea_B14}. 371 371 The parameterization is an empirical one, \ie not derived from theoretical considerations, 372 372 but rather is meant to account for observed processes that affect the density structure of … … 427 427 (first line in \autoref{eq:PE_zdf}). 428 428 To do so a special care have to be taken for both the time and space discretization of 429 the TKE equation \citep{ Burchard_OM02,Marsaleix_al_OM08}.429 the TKE equation \citep{burchard_OM02,marsaleix.auclair.ea_OM08}. 430 430 431 431 Let us first address the time stepping issue. \autoref{fig:TKE_time_scheme} shows how … … 524 524 The Generic Length Scale (GLS) scheme is a turbulent closure scheme based on two prognostic equations: 525 525 one for the turbulent kinetic energy $\bar {e}$, and another for the generic length scale, 526 $\psi$ \citep{ Umlauf_Burchard_JMS03, Umlauf_Burchard_CSR05}.526 $\psi$ \citep{umlauf.burchard_JMR03, umlauf.burchard_CSR05}. 527 527 This later variable is defined as: $\psi = {C_{0\mu}}^{p} \ {\bar{e}}^{m} \ l^{n}$, 528 528 where the triplet $(p, m, n)$ value given in Tab.\autoref{tab:GLS} allows to recover a number of 529 well-known turbulent closures ($k$-$kl$ \citep{ Mellor_Yamada_1982}, $k$-$\epsilon$ \citep{Rodi_1987},530 $k$-$\omega$ \citep{ Wilcox_1988} among others \citep{Umlauf_Burchard_JMS03,Kantha_Carniel_CSR05}).529 well-known turbulent closures ($k$-$kl$ \citep{mellor.yamada_RG82}, $k$-$\epsilon$ \citep{rodi_JGR87}, 530 $k$-$\omega$ \citep{wilcox_AJ88} among others \citep{umlauf.burchard_JMR03,kantha.carniel_JMR03}). 531 531 The GLS scheme is given by the following set of equations: 532 532 \begin{equation} … … 577 577 \begin{tabular}{ccccc} 578 578 & $k-kl$ & $k-\epsilon$ & $k-\omega$ & generic \\ 579 % & \citep{ Mellor_Yamada_1982} & \citep{Rodi_1987} & \citep{Wilcox_1988} & \\579 % & \citep{mellor.yamada_RG82} & \citep{rodi_JGR87} & \citep{wilcox_AJ88} & \\ 580 580 \hline 581 581 \hline … … 604 604 the mixing length towards $K z_b$ ($K$: Kappa and $z_b$: rugosity length) value near physical boundaries 605 605 (logarithmic boundary layer law). 606 $C_{\mu}$ and $C_{\mu'}$ are calculated from stability function proposed by \citet{ Galperin_al_JAS88},607 or by \citet{ Kantha_Clayson_1994} or one of the two functions suggested by \citet{Canuto_2001}606 $C_{\mu}$ and $C_{\mu'}$ are calculated from stability function proposed by \citet{galperin.kantha.ea_JAS88}, 607 or by \citet{kantha.clayson_JGR94} or one of the two functions suggested by \citet{canuto.howard.ea_JPO01} 608 608 (\np{nn\_stab\_func}\forcode{ = 0..3}, resp.). 609 609 The value of $C_{0\mu}$ depends of the choice of the stability function. … … 612 612 Neumann condition through \np{nn\_tkebc\_surf} and \np{nn\_tkebc\_bot}, resp. 613 613 As for TKE closure, the wave effect on the mixing is considered when 614 \np{ln\_crban}\forcode{ = .true.} \citep{ Craig_Banner_JPO94, Mellor_Blumberg_JPO04}.614 \np{ln\_crban}\forcode{ = .true.} \citep{craig.banner_JPO94, mellor.blumberg_JPO04}. 615 615 The \np{rn\_crban} namelist parameter is $\alpha_{CB}$ in \autoref{eq:ZDF_Esbc} and 616 616 \np{rn\_charn} provides the value of $\beta$ in \autoref{eq:ZDF_Lsbc}. … … 619 619 almost all authors apply a clipping of the length scale as an \textit{ad hoc} remedy. 620 620 With this clipping, the maximum permissible length scale is determined by $l_{max} = c_{lim} \sqrt{2\bar{e}}/ N$. 621 A value of $c_{lim} = 0.53$ is often used \citep{ Galperin_al_JAS88}.622 \cite{ Umlauf_Burchard_CSR05} show that the value of the clipping factor is of crucial importance for621 A value of $c_{lim} = 0.53$ is often used \citep{galperin.kantha.ea_JAS88}. 622 \cite{umlauf.burchard_CSR05} show that the value of the clipping factor is of crucial importance for 623 623 the entrainment depth predicted in stably stratified situations, 624 624 and that its value has to be chosen in accordance with the algebraic model for the turbulent fluxes. … … 627 627 628 628 The time and space discretization of the GLS equations follows the same energetic consideration as for 629 the TKE case described in \autoref{subsec:ZDF_tke_ene} \citep{ Burchard_OM02}.630 Examples of performance of the 4 turbulent closure scheme can be found in \citet{ Warner_al_OM05}.629 the TKE case described in \autoref{subsec:ZDF_tke_ene} \citep{burchard_OM02}. 630 Examples of performance of the 4 turbulent closure scheme can be found in \citet{warner.sherwood.ea_OM05}. 631 631 632 632 % ------------------------------------------------------------------------------------------------------------- … … 700 700 the water column, but only until the density structure becomes neutrally stable 701 701 (\ie until the mixed portion of the water column has \textit{exactly} the density of the water just below) 702 \citep{ Madec_al_JPO91}.702 \citep{madec.delecluse.ea_JPO91}. 703 703 The associated algorithm is an iterative process used in the following way (\autoref{fig:npc}): 704 704 starting from the top of the ocean, the first instability is found. … … 718 718 the algorithm used in \NEMO converges for any profile in a number of iterations which is less than 719 719 the number of vertical levels. 720 This property is of paramount importance as pointed out by \citet{ Killworth1989}:720 This property is of paramount importance as pointed out by \citet{killworth_iprc89}: 721 721 it avoids the existence of permanent and unrealistic static instabilities at the sea surface. 722 722 This non-penetrative convective algorithm has been proved successful in studies of the deep water formation in 723 the north-western Mediterranean Sea \citep{ Madec_al_JPO91, Madec_al_DAO91, Madec_Crepon_Bk91}.723 the north-western Mediterranean Sea \citep{madec.delecluse.ea_JPO91, madec.chartier.ea_DAO91, madec.crepon_iprc91}. 724 724 725 725 The current implementation has been modified in order to deal with any non linear equation of seawater … … 748 748 In this case, the vertical eddy mixing coefficients are assigned very large values 749 749 (a typical value is $10\;m^2s^{-1})$ in regions where the stratification is unstable 750 (\ie when $N^2$ the Brunt-Vais\"{a}l\"{a} frequency is negative) \citep{ Lazar_PhD97, Lazar_al_JPO99}.750 (\ie when $N^2$ the Brunt-Vais\"{a}l\"{a} frequency is negative) \citep{lazar_phd97, lazar.madec.ea_JPO99}. 751 751 This is done either on tracers only (\np{nn\_evdm}\forcode{ = 0}) or 752 752 on both momentum and tracers (\np{nn\_evdm}\forcode{ = 1}). … … 764 764 Note that the stability test is performed on both \textit{before} and \textit{now} values of $N^2$. 765 765 This removes a potential source of divergence of odd and even time step in 766 a leapfrog environment \citep{ Leclair_PhD2010} (see \autoref{sec:STP_mLF}).766 a leapfrog environment \citep{leclair_phd10} (see \autoref{sec:STP_mLF}). 767 767 768 768 % ------------------------------------------------------------------------------------------------------------- … … 807 807 The former condition leads to salt fingering and the latter to diffusive convection. 808 808 Double-diffusive phenomena contribute to diapycnal mixing in extensive regions of the ocean. 809 \citet{ Merryfield1999} include a parameterisation of such phenomena in a global ocean model and show that809 \citet{merryfield.holloway.ea_JPO99} include a parameterisation of such phenomena in a global ocean model and show that 810 810 it leads to relatively minor changes in circulation but exerts significant regional influences on 811 811 temperature and salinity. … … 842 842 \caption{ 843 843 \protect\label{fig:zdfddm} 844 From \citet{ Merryfield1999} :844 From \citet{merryfield.holloway.ea_JPO99} : 845 845 (a) Diapycnal diffusivities $A_f^{vT}$ and $A_f^{vS}$ for temperature and salt in regions of salt fingering. 846 846 Heavy curves denote $A^{\ast v} = 10^{-3}~m^2.s^{-1}$ and thin curves $A^{\ast v} = 10^{-4}~m^2.s^{-1}$; … … 855 855 856 856 The factor 0.7 in \autoref{eq:zdfddm_f_T} reflects the measured ratio $\alpha F_T /\beta F_S \approx 0.7$ of 857 buoyancy flux of heat to buoyancy flux of salt (\eg, \citet{ McDougall_Taylor_JMR84}).858 Following \citet{ Merryfield1999}, we adopt $R_c = 1.6$, $n = 6$, and $A^{\ast v} = 10^{-4}~m^2.s^{-1}$.857 buoyancy flux of heat to buoyancy flux of salt (\eg, \citet{mcdougall.taylor_JMR84}). 858 Following \citet{merryfield.holloway.ea_JPO99}, we adopt $R_c = 1.6$, $n = 6$, and $A^{\ast v} = 10^{-4}~m^2.s^{-1}$. 859 859 860 860 To represent mixing of S and T by diffusive layering, the diapycnal diffusivities suggested by … … 963 963 This coefficient is generally estimated by setting a typical decay time $\tau$ in the deep ocean, 964 964 and setting $r = H / \tau$, where $H$ is the ocean depth. 965 Commonly accepted values of $\tau$ are of the order of 100 to 200 days \citep{ Weatherly_JMR84}.965 Commonly accepted values of $\tau$ are of the order of 100 to 200 days \citep{weatherly_JMR84}. 966 966 A value $\tau^{-1} = 10^{-7}$~s$^{-1}$ equivalent to 115 days, is usually used in quasi-geostrophic models. 967 967 One may consider the linear friction as an approximation of quadratic friction, $r \approx 2\;C_D\;U_{av}$ 968 (\citet{ Gill1982}, Eq. 9.6.6).968 (\citet{gill_bk82}, Eq. 9.6.6). 969 969 For example, with a drag coefficient $C_D = 0.002$, a typical speed of tidal currents of $U_{av} =0.1$~m\;s$^{-1}$, 970 970 and assuming an ocean depth $H = 4000$~m, the resulting friction coefficient is $r = 4\;10^{-4}$~m\;s$^{-1}$. … … 1005 1005 internal waves breaking and other short time scale currents. 1006 1006 A typical value of the drag coefficient is $C_D = 10^{-3} $. 1007 As an example, the CME experiment \citep{ Treguier_JGR92} uses $C_D = 10^{-3}$ and1008 $e_b = 2.5\;10^{-3}$m$^2$\;s$^{-2}$, while the FRAM experiment \citep{ Killworth1992} uses $C_D = 1.4\;10^{-3}$ and1007 As an example, the CME experiment \citep{treguier_JGR92} uses $C_D = 10^{-3}$ and 1008 $e_b = 2.5\;10^{-3}$m$^2$\;s$^{-2}$, while the FRAM experiment \citep{killworth_JPO92} uses $C_D = 1.4\;10^{-3}$ and 1009 1009 $e_b =2.5\;\;10^{-3}$m$^2$\;s$^{-2}$. 1010 1010 The CME choices have been set as default values (\np{rn\_bfri2} and \np{rn\_bfeb2} namelist parameters). … … 1235 1235 Options are defined through the \ngn{namzdf\_tmx} namelist variables. 1236 1236 The parameterization of tidal mixing follows the general formulation for the vertical eddy diffusivity proposed by 1237 \citet{ St_Laurent_al_GRL02} and first introduced in an OGCM by \citep{Simmons_al_OM04}.1237 \citet{st-laurent.simmons.ea_GRL02} and first introduced in an OGCM by \citep{simmons.jayne.ea_OM04}. 1238 1238 In this formulation an additional vertical diffusivity resulting from internal tide breaking, 1239 1239 $A^{vT}_{tides}$ is expressed as a function of $E(x,y)$, … … 1252 1252 with the remaining $1-q$ radiating away as low mode internal waves and 1253 1253 contributing to the background internal wave field. 1254 A value of $q=1/3$ is typically used \citet{ St_Laurent_al_GRL02}.1254 A value of $q=1/3$ is typically used \citet{st-laurent.simmons.ea_GRL02}. 1255 1255 The vertical structure function $F(z)$ models the distribution of the turbulent mixing in the vertical. 1256 1256 It is implemented as a simple exponential decaying upward away from the bottom, 1257 1257 with a vertical scale of $h_o$ (\np{rn\_htmx} namelist parameter, 1258 with a typical value of $500\,m$) \citep{ St_Laurent_Nash_DSR04},1258 with a typical value of $500\,m$) \citep{st-laurent.nash_DSR04}, 1259 1259 \[ 1260 1260 % \label{eq:Fz} … … 1274 1274 the unrepresented internal waves induced by the tidal flow over rough topography in a stratified ocean. 1275 1275 In the current version of \NEMO, the map is built from the output of 1276 the barotropic global ocean tide model MOG2D-G \citep{ Carrere_Lyard_GRL03}.1276 the barotropic global ocean tide model MOG2D-G \citep{carrere.lyard_GRL03}. 1277 1277 This model provides the dissipation associated with internal wave energy for the M2 and K1 tides component 1278 1278 (\autoref{fig:ZDF_M2_K1_tmx}). … … 1280 1280 The internal wave energy is thus : $E(x, y) = 1.25 E_{M2} + E_{K1}$. 1281 1281 Its global mean value is $1.1$ TW, 1282 in agreement with independent estimates \citep{ Egbert_Ray_Nat00, Egbert_Ray_JGR01}.1282 in agreement with independent estimates \citep{egbert.ray_N00, egbert.ray_JGR01}. 1283 1283 1284 1284 %>>>>>>>>>>>>>>>>>>>>>>>>>>>> … … 1288 1288 \caption{ 1289 1289 \protect\label{fig:ZDF_M2_K1_tmx} 1290 (a) M2 and (b) K1 internal wave drag energy from \citet{ Carrere_Lyard_GRL03} ($W/m^2$).1290 (a) M2 and (b) K1 internal wave drag energy from \citet{carrere.lyard_GRL03} ($W/m^2$). 1291 1291 } 1292 1292 \end{center} … … 1306 1306 1307 1307 When \np{ln\_tmx\_itf}\forcode{ = .true.}, the two key parameters $q$ and $F(z)$ are adjusted following 1308 the parameterisation developed by \citet{ Koch-Larrouy_al_GRL07}:1308 the parameterisation developed by \citet{koch-larrouy.madec.ea_GRL07}: 1309 1309 1310 1310 First, the Indonesian archipelago is a complex geographic region with a series of … … 1318 1318 Second, the vertical structure function, $F(z)$, is no more associated with a bottom intensification of the mixing, 1319 1319 but with a maximum of energy available within the thermocline. 1320 \citet{ Koch-Larrouy_al_GRL07} have suggested that the vertical distribution of1320 \citet{koch-larrouy.madec.ea_GRL07} have suggested that the vertical distribution of 1321 1321 the energy dissipation proportional to $N^2$ below the core of the thermocline and to $N$ above. 1322 1322 The resulting $F(z)$ is: … … 1335 1335 Introduced in a regional OGCM, the parameterization improves the water mass characteristics in 1336 1336 the different Indonesian seas, suggesting that the horizontal and vertical distributions of 1337 the mixing are adequately prescribed \citep{ Koch-Larrouy_al_GRL07, Koch-Larrouy_al_OD08a, Koch-Larrouy_al_OD08b}.1337 the mixing are adequately prescribed \citep{koch-larrouy.madec.ea_GRL07, koch-larrouy.madec.ea_OD08*a, koch-larrouy.madec.ea_OD08*b}. 1338 1338 Note also that such a parameterisation has a significant impact on the behaviour of 1339 global coupled GCMs \citep{ Koch-Larrouy_al_CD10}.1339 global coupled GCMs \citep{koch-larrouy.lengaigne.ea_CD10}. 1340 1340 1341 1341 % ================================================================ … … 1351 1351 1352 1352 The parameterization of mixing induced by breaking internal waves is a generalization of 1353 the approach originally proposed by \citet{ St_Laurent_al_GRL02}.1353 the approach originally proposed by \citet{st-laurent.simmons.ea_GRL02}. 1354 1354 A three-dimensional field of internal wave energy dissipation $\epsilon(x,y,z)$ is first constructed, 1355 1355 and the resulting diffusivity is obtained as … … 1361 1361 the energy available for mixing. 1362 1362 If the \np{ln\_mevar} namelist parameter is set to false, the mixing efficiency is taken as constant and 1363 equal to 1/6 \citep{ Osborn_JPO80}.1363 equal to 1/6 \citep{osborn_JPO80}. 1364 1364 In the opposite (recommended) case, $R_f$ is instead a function of 1365 1365 the turbulence intensity parameter $Re_b = \frac{ \epsilon}{\nu \, N^2}$, 1366 with $\nu$ the molecular viscosity of seawater, following the model of \cite{ Bouffard_Boegman_DAO2013} and1367 the implementation of \cite{de _lavergne_JPO2016_efficiency}.1366 with $\nu$ the molecular viscosity of seawater, following the model of \cite{bouffard.boegman_DAO13} and 1367 the implementation of \cite{de-lavergne.madec.ea_JPO16}. 1368 1368 Note that $A^{vT}_{wave}$ is bounded by $10^{-2}\,m^2/s$, a limit that is often reached when 1369 1369 the mixing efficiency is constant. … … 1371 1371 In addition to the mixing efficiency, the ratio of salt to heat diffusivities can chosen to vary 1372 1372 as a function of $Re_b$ by setting the \np{ln\_tsdiff} parameter to true, a recommended choice. 1373 This parameterization of differential mixing, due to \cite{ Jackson_Rehmann_JPO2014},1374 is implemented as in \cite{de _lavergne_JPO2016_efficiency}.1373 This parameterization of differential mixing, due to \cite{jackson.rehmann_JPO14}, 1374 is implemented as in \cite{de-lavergne.madec.ea_JPO16}. 1375 1375 1376 1376 The three-dimensional distribution of the energy available for mixing, $\epsilon(i,j,k)$, … … 1395 1395 $h_{cri}$ is related to the large-scale topography of the ocean (etopo2) and 1396 1396 $h_{bot}$ is a function of the energy flux $E_{bot}$, the characteristic horizontal scale of 1397 the abyssal hill topography \citep{ Goff_JGR2010} and the latitude.1397 the abyssal hill topography \citep{goff_JGR10} and the latitude. 1398 1398 1399 1399 % ================================================================ -
NEMO/trunk/doc/latex/NEMO/subfiles/chap_conservation.tex
r10442 r11123 21 21 horizontal kinetic energy and/or potential enstrophy of horizontally non-divergent flow, 22 22 and variance of temperature and salinity will be conserved in the absence of dissipative effects and forcing. 23 \citet{ Arakawa1966} has first pointed out the advantage of this approach.23 \citet{arakawa_JCP66} has first pointed out the advantage of this approach. 24 24 He showed that if integral constraints on energy are maintained, 25 25 the computation will be free of the troublesome "non linear" instability originally pointed out by 26 \citet{ Phillips1959}.26 \citet{phillips_TAMS59}. 27 27 A consistent formulation of the energetic properties is also extremely important in carrying out 28 28 long-term numerical simulations for an oceanographic model. 29 Such a formulation avoids systematic errors that accumulate with time \citep{ Bryan1997}.29 Such a formulation avoids systematic errors that accumulate with time \citep{bryan_JCP97}. 30 30 31 31 The general philosophy of OPA which has led to the discrete formulation presented in {\S}II.2 and II.3 is to … … 39 39 Note that in some very specific cases as passive tracer studies, the positivity of the advective scheme is required. 40 40 In that case, and in that case only, the advective scheme used for passive tracer is a flux correction scheme 41 \citep{Marti1992 , Levy1996, Levy1998}.41 \citep{Marti1992?, Levy1996?, Levy1998?}. 42 42 43 43 % ------------------------------------------------------------------------------------------------------------- -
NEMO/trunk/doc/latex/NEMO/subfiles/chap_misc.tex
r10601 r11123 272 272 and their propagation and accumulation cause uncertainty in final simulation reproducibility on 273 273 different numbers of processors. 274 To avoid so, based on \citet{ He_Ding_JSC01} review of different technics,274 To avoid so, based on \citet{he.ding_JS01} review of different technics, 275 275 we use a so called self-compensated summation method. 276 276 The idea is to estimate the roundoff error, store it in a buffer, and then add it back in the next addition. -
NEMO/trunk/doc/latex/NEMO/subfiles/chap_model_basics.tex
r10544 r11123 258 258 If further, an approximative conservation of heat and salt contents is sufficient for the problem solved, 259 259 then it is sufficient to solve a linearized version of \autoref{eq:PE_ssh}, 260 which still allows to take into account freshwater fluxes applied at the ocean surface \citep{ Roullet_Madec_JGR00}.260 which still allows to take into account freshwater fluxes applied at the ocean surface \citep{roullet.madec_JGR00}. 261 261 Nevertheless, with the linearization, an exact conservation of heat and salt contents is lost. 262 262 263 263 The filtering of EGWs in models with a free surface is usually a matter of discretisation of 264 264 the temporal derivatives, 265 using a split-explicit method \citep{ Killworth_al_JPO91, Zhang_Endoh_JGR92} or266 the implicit scheme \citep{ Dukowicz1994} or267 the addition of a filtering force in the momentum equation \citep{ Roullet_Madec_JGR00}.265 using a split-explicit method \citep{killworth.webb.ea_JPO91, zhang.endoh_JGR92} or 266 the implicit scheme \citep{dukowicz.smith_JGR94} or 267 the addition of a filtering force in the momentum equation \citep{roullet.madec_JGR00}. 268 268 With the present release, \NEMO offers the choice between 269 269 an explicit free surface (see \autoref{subsec:DYN_spg_exp}) or 270 a split-explicit scheme strongly inspired the one proposed by \citet{ Shchepetkin_McWilliams_OM05}270 a split-explicit scheme strongly inspired the one proposed by \citet{shchepetkin.mcwilliams_OM05} 271 271 (see \autoref{subsec:DYN_spg_ts}). 272 272 … … 292 292 cannot be easily treated in a global model without filtering. 293 293 A solution consists of introducing an appropriate coordinate transformation that 294 shifts the singular point onto land \citep{ Madec_Imbard_CD96, Murray_JCP96}.294 shifts the singular point onto land \citep{madec.imbard_CD96, murray_JCP96}. 295 295 As a consequence, it is important to solve the primitive equations in various curvilinear coordinate systems. 296 296 An efficient way of introducing an appropriate coordinate transform can be found when using a tensorial formalism. … … 298 298 Ocean modellers mainly use three-dimensional orthogonal grids on the sphere (spherical earth approximation), 299 299 with preservation of the local vertical. Here we give the simplified equations for this particular case. 300 The general case is detailed by \citet{ Eiseman1980} in their survey of the conservation laws of fluid dynamics.300 The general case is detailed by \citet{eiseman.stone_SR80} in their survey of the conservation laws of fluid dynamics. 301 301 302 302 Let $(i,j,k)$ be a set of orthogonal curvilinear coordinates on … … 577 577 In order to satisfy two or more constrains one can even be tempted to mixed these coordinate systems, as in 578 578 HYCOM (mixture of $z$-coordinate at the surface, isopycnic coordinate in the ocean interior and $\sigma$ at 579 the ocean bottom) \citep{ Chassignet_al_JPO03} or579 the ocean bottom) \citep{chassignet.smith.ea_JPO03} or 580 580 OPA (mixture of $z$-coordinate in vicinity the surface and steep topography areas and $\sigma$-coordinate elsewhere) 581 \citep{ Madec_al_JPO96} among others.581 \citep{madec.delecluse.ea_JPO96} among others. 582 582 583 583 In fact one is totally free to choose any space and time vertical coordinate by … … 592 592 the $(i,j,s,t)$ generalised coordinate system with $s$ depending on the other three variables through 593 593 \autoref{eq:PE_s}. 594 This so-called \textit{generalised vertical coordinate} \citep{ Kasahara_MWR74} is in fact594 This so-called \textit{generalised vertical coordinate} \citep{kasahara_MWR74} is in fact 595 595 an Arbitrary Lagrangian--Eulerian (ALE) coordinate. 596 596 Indeed, choosing an expression for $s$ is an arbitrary choice that determines 597 597 which part of the vertical velocity (defined from a fixed referential) will cross the levels (Eulerian part) and 598 598 which part will be used to move them (Lagrangian part). 599 The coordinate is also sometime referenced as an adaptive coordinate \citep{ Hofmeister_al_OM09},599 The coordinate is also sometime referenced as an adaptive coordinate \citep{hofmeister.burchard.ea_OM10}, 600 600 since the coordinate system is adapted in the course of the simulation. 601 601 Its most often used implementation is via an ALE algorithm, 602 602 in which a pure lagrangian step is followed by regridding and remapping steps, 603 603 the later step implicitly embedding the vertical advection 604 \citep{ Hirt_al_JCP74, Chassignet_al_JPO03, White_al_JCP09}.605 Here we follow the \citep{ Kasahara_MWR74} strategy:604 \citep{hirt.amsden.ea_JCP74, chassignet.smith.ea_JPO03, white.adcroft.ea_JCP09}. 605 Here we follow the \citep{kasahara_MWR74} strategy: 606 606 a regridding step (an update of the vertical coordinate) followed by an eulerian step with 607 607 an explicit computation of vertical advection relative to the moving s-surfaces. … … 744 744 (b) $z$-coordinate in non-linear free surface case ; 745 745 (c) re-scaled height coordinate 746 (become popular as the \zstar-coordinate \citep{ Adcroft_Campin_OM04}).746 (become popular as the \zstar-coordinate \citep{adcroft.campin_OM04}). 747 747 } 748 748 \end{center} … … 751 751 752 752 In that case, the free surface equation is nonlinear, and the variations of volume are fully taken into account. 753 These coordinates systems is presented in a report \citep{ Levier2007} available on the \NEMO web site.753 These coordinates systems is presented in a report \citep{levier.treguier.ea_rpt07} available on the \NEMO web site. 754 754 755 755 The \zstar coordinate approach is an unapproximated, non-linear free surface implementation which allows one to 756 deal with large amplitude free-surface variations relative to the vertical resolution \citep{ Adcroft_Campin_OM04}.756 deal with large amplitude free-surface variations relative to the vertical resolution \citep{adcroft.campin_OM04}. 757 757 In the \zstar formulation, 758 758 the variation of the column thickness due to sea-surface undulations is not concentrated in the surface level, … … 805 805 The quasi -horizontal nature of the coordinate surfaces also facilitates the implementation of 806 806 neutral physics parameterizations in \zstar models using the same techniques as in $z$-models 807 (see Chapters 13-16 of \cite{ Griffies_Bk04}) for a discussion of neutral physics in $z$-models,807 (see Chapters 13-16 of \cite{griffies_bk04}) for a discussion of neutral physics in $z$-models, 808 808 as well as \autoref{sec:LDF_slp} in this document for treatment in \NEMO). 809 809 … … 849 849 The response to such a velocity field often leads to numerical dispersion effects. 850 850 One solution to strongly reduce this error is to use a partial step representation of bottom topography instead of 851 a full step one \cite{ Pacanowski_Gnanadesikan_MWR98}.851 a full step one \cite{pacanowski.gnanadesikan_MWR98}. 852 852 Another solution is to introduce a terrain-following coordinate system (hereafter $s$-coordinate). 853 853 … … 876 876 introduces a truncation error that is not present in a $z$-model. 877 877 In the special case of a $\sigma$-coordinate (i.e. a depth-normalised coordinate system $\sigma = z/H$), 878 \citet{ Haney1991} and \citet{Beckmann1993} have given estimates of the magnitude of this truncation error.878 \citet{haney_JPO91} and \citet{beckmann.haidvogel_JPO93} have given estimates of the magnitude of this truncation error. 879 879 It depends on topographic slope, stratification, horizontal and vertical resolution, the equation of state, 880 880 and the finite difference scheme. … … 884 884 The large-scale slopes require high horizontal resolution, and the computational cost becomes prohibitive. 885 885 This problem can be at least partially overcome by mixing $s$-coordinate and 886 step-like representation of bottom topography \citep{ Gerdes1993a,Gerdes1993b,Madec_al_JPO96}.886 step-like representation of bottom topography \citep{gerdes_JGR93*a,gerdes_JGR93*b,madec.delecluse.ea_JPO96}. 887 887 However, the definition of the model domain vertical coordinate becomes then a non-trivial thing for 888 888 a realistic bottom topography: … … 904 904 In contrast, the ocean will stay at rest in a $z$-model. 905 905 As for the truncation error, the problem can be reduced by introducing the terrain-following coordinate below 906 the strongly stratified portion of the water column (\ie the main thermocline) \citep{ Madec_al_JPO96}.906 the strongly stratified portion of the water column (\ie the main thermocline) \citep{madec.delecluse.ea_JPO96}. 907 907 An alternate solution consists of rotating the lateral diffusive tensor to geopotential or to isoneutral surfaces 908 908 (see \autoref{subsec:PE_ldf}). … … 910 910 strongly exceeding the stability limit of such a operator when it is discretized (see \autoref{chap:LDF}). 911 911 912 The $s$-coordinates introduced here \citep{ Lott_al_OM90,Madec_al_JPO96} differ mainly in two aspects from912 The $s$-coordinates introduced here \citep{lott.madec.ea_OM90,madec.delecluse.ea_JPO96} differ mainly in two aspects from 913 913 similar models: 914 914 it allows a representation of bottom topography with mixed full or partial step-like/terrain following topography; … … 921 921 \label{subsec:PE_zco_tilde} 922 922 923 The \ztilde -coordinate has been developed by \citet{ Leclair_Madec_OM11}.923 The \ztilde -coordinate has been developed by \citet{leclair.madec_OM11}. 924 924 It is available in \NEMO since the version 3.4. 925 925 Nevertheless, it is currently not robust enough to be used in all possible configurations. … … 1005 1005 The resulting lateral diffusive and dissipative operators are of second order. 1006 1006 Observations show that lateral mixing induced by mesoscale turbulence tends to be along isopycnal surfaces 1007 (or more precisely neutral surfaces \cite{ McDougall1987}) rather than across them.1007 (or more precisely neutral surfaces \cite{mcdougall_JPO87}) rather than across them. 1008 1008 As the slope of neutral surfaces is small in the ocean, a common approximation is to assume that 1009 1009 the `lateral' direction is the horizontal, \ie the lateral mixing is performed along geopotential surfaces. … … 1016 1016 both horizontal and isoneutral operators have no effect on mean (\ie large scale) potential energy whereas 1017 1017 potential energy is a main source of turbulence (through baroclinic instabilities). 1018 \citet{ Gent1990} have proposed a parameterisation of mesoscale eddy-induced turbulence which1018 \citet{gent.mcwilliams_JPO90} have proposed a parameterisation of mesoscale eddy-induced turbulence which 1019 1019 associates an eddy-induced velocity to the isoneutral diffusion. 1020 1020 Its mean effect is to reduce the mean potential energy of the ocean. … … 1040 1040 There are not all available in \NEMO. For active tracers (temperature and salinity) the main ones are: 1041 1041 Laplacian and bilaplacian operators acting along geopotential or iso-neutral surfaces, 1042 \citet{ Gent1990} parameterisation, and various slightly diffusive advection schemes.1042 \citet{gent.mcwilliams_JPO90} parameterisation, and various slightly diffusive advection schemes. 1043 1043 For momentum, the main ones are: Laplacian and bilaplacian operators acting along geopotential surfaces, 1044 1044 and UBS advection schemes when flux form is chosen for the momentum advection. … … 1062 1062 the rotation between geopotential and $s$-surfaces, 1063 1063 while it is only an approximation for the rotation between isoneutral and $z$- or $s$-surfaces. 1064 Indeed, in the latter case, two assumptions are made to simplify \autoref{eq:PE_iso_tensor} \citep{ Cox1987}.1064 Indeed, in the latter case, two assumptions are made to simplify \autoref{eq:PE_iso_tensor} \citep{cox_OM87}. 1065 1065 First, the horizontal contribution of the dianeutral mixing is neglected since the ratio between iso and 1066 1066 dia-neutral diffusive coefficients is known to be several orders of magnitude smaller than unity. … … 1087 1087 \subsubsection{Eddy induced velocity} 1088 1088 1089 When the \textit{eddy induced velocity} parametrisation (eiv) \citep{ Gent1990} is used,1089 When the \textit{eddy induced velocity} parametrisation (eiv) \citep{gent.mcwilliams_JPO90} is used, 1090 1090 an additional tracer advection is introduced in combination with the isoneutral diffusion of tracers: 1091 1091 \[ … … 1162 1162 \ie on a $f$- or $\beta$-plane, not on the sphere. 1163 1163 It is also a very good approximation in vicinity of the Equator in 1164 a geographical coordinate system \citep{ Lengaigne_al_JGR03}.1164 a geographical coordinate system \citep{lengaigne.madec.ea_JGR03}. 1165 1165 1166 1166 \subsubsection{lateral bilaplacian momentum diffusive operator} -
NEMO/trunk/doc/latex/NEMO/subfiles/chap_model_basics_zstar.tex
r10544 r11123 18 18 19 19 In that case, the free surface equation is nonlinear, and the variations of volume are fully taken into account. 20 These coordinates systems is presented in a report \citep{ Levier2007} available on the \NEMO web site.20 These coordinates systems is presented in a report \citep{levier.treguier.ea_rpt07} available on the \NEMO web site. 21 21 22 22 \colorbox{yellow}{ end of to be updated} … … 89 89 which imposes a very small time step when an explicit time stepping is used. 90 90 Two methods are proposed to allow a longer time step for the three-dimensional equations: 91 the filtered free surface, which is a modification of the continuous equations %(see \autoref{eq:PE_flt }),91 the filtered free surface, which is a modification of the continuous equations %(see \autoref{eq:PE_flt?}), 92 92 and the split-explicit free surface described below. 93 93 The extra term introduced in the filtered method is calculated implicitly, … … 139 139 \nlst{namdom} 140 140 %-------------------------------------------------------------------------------------------------------------- 141 The split-explicit free surface formulation used in OPA follows the one proposed by \citet{Griffies2004 }.141 The split-explicit free surface formulation used in OPA follows the one proposed by \citet{Griffies2004?}. 142 142 The general idea is to solve the free surface equation with a small time step, 143 143 while the three dimensional prognostic variables are solved with a longer time step that … … 151 151 \protect\label{fig:DYN_dynspg_ts} 152 152 Schematic of the split-explicit time stepping scheme for the barotropic and baroclinic modes, 153 after \citet{Griffies2004 }.153 after \citet{Griffies2004?}. 154 154 Time increases to the right. 155 155 Baroclinic time steps are denoted by $t-\Delta t$, $t, t+\Delta t$, and $t+2\Delta t$. … … 171 171 172 172 The split-explicit formulation has a damping effect on external gravity waves, 173 which is weaker than the filtered free surface but still significant as shown by \citet{ Levier2007} in173 which is weaker than the filtered free surface but still significant as shown by \citet{levier.treguier.ea_rpt07} in 174 174 the case of an analytical barotropic Kelvin wave. 175 175 … … 294 294 \label{subsec:DYN_spg_flt} 295 295 296 The filtered formulation follows the \citet{Roullet2000 } implementation.296 The filtered formulation follows the \citet{Roullet2000?} implementation. 297 297 The extra term introduced in the equations (see {\S}I.2.2) is solved implicitly. 298 298 The elliptic solvers available in the code are documented in \autoref{chap:MISC}. 299 299 The amplitude of the extra term is given by the namelist variable \np{rnu}. 300 The default value is 1, as recommended by \citet{Roullet2000 }300 The default value is 1, as recommended by \citet{Roullet2000?} 301 301 302 302 \colorbox{red}{\np{rnu}\forcode{ = 1} to be suppressed from namelist !} … … 309 309 310 310 In the non-linear free surface formulation, the variations of volume are fully taken into account. 311 This option is presented in a report \citep{ Levier2007} available on the NEMO web site.311 This option is presented in a report \citep{levier.treguier.ea_rpt07} available on the NEMO web site. 312 312 The three time-stepping methods (explicit, split-explicit and filtered) are the same as in 313 313 \autoref{DYN_spg_linear} except that the ocean depth is now time-dependent. -
NEMO/trunk/doc/latex/NEMO/subfiles/chap_time_domain.tex
r10501 r11123 64 64 65 65 The time stepping used for processes other than diffusion is the well-known leapfrog scheme 66 \citep{ Mesinger_Arakawa_Bk76}.66 \citep{mesinger.arakawa_bk76}. 67 67 This scheme is widely used for advection processes in low-viscosity fluids. 68 68 It is a time centred scheme, \ie the RHS in \autoref{eq:STP} is evaluated at time step $t$, the now time step. … … 80 80 To prevent it, the leapfrog scheme is often used in association with a Robert-Asselin time filter 81 81 (hereafter the LF-RA scheme). 82 This filter, first designed by \citet{ Robert_JMSJ66} and more comprehensively studied by \citet{Asselin_MWR72},82 This filter, first designed by \citet{robert_JMSJ66} and more comprehensively studied by \citet{asselin_MWR72}, 83 83 is a kind of laplacian diffusion in time that mixes odd and even time steps: 84 84 \begin{equation} … … 89 89 $\gamma$ is initialized as \np{rn\_atfp} (namelist parameter). 90 90 Its default value is \np{rn\_atfp}~\forcode{= 10.e-3} (see \autoref{sec:STP_mLF}), 91 causing only a weak dissipation of high frequency motions (\citep{ Farge1987}).91 causing only a weak dissipation of high frequency motions (\citep{farge-coulombier_phd87}). 92 92 The addition of a time filter degrades the accuracy of the calculation from second to first order. 93 93 However, the second order truncation error is proportional to $\gamma$, which is small compared to 1. … … 115 115 116 116 This is diffusive in time and conditionally stable. 117 The conditions for stability of second and fourth order horizontal diffusion schemes are \citep{ Griffies_Bk04}:117 The conditions for stability of second and fourth order horizontal diffusion schemes are \citep{griffies_bk04}: 118 118 \begin{equation} 119 119 \label{eq:STP_euler_stability} … … 183 183 $c(k)$ and $d(k)$ are positive and the diagonal term is greater than the sum of the two extra-diagonal terms, 184 184 therefore a special adaptation of the Gauss elimination procedure is used to find the solution 185 (see for example \citet{ Richtmyer1967}).185 (see for example \citet{richtmyer.morton_bk67}). 186 186 187 187 % ------------------------------------------------------------------------------------------------------------- … … 200 200 \caption{ 201 201 \protect\label{fig:TimeStep_flowchart} 202 Sketch of the leapfrog time stepping sequence in \NEMO from \citet{ Leclair_Madec_OM09}.202 Sketch of the leapfrog time stepping sequence in \NEMO from \citet{leclair.madec_OM09}. 203 203 The use of a semi -implicit computation of the hydrostatic pressure gradient requires the tracer equation to 204 204 be stepped forward prior to the momentum equation. … … 219 219 \label{sec:STP_mLF} 220 220 221 Significant changes have been introduced by \cite{ Leclair_Madec_OM09} in the LF-RA scheme in order to221 Significant changes have been introduced by \cite{leclair.madec_OM09} in the LF-RA scheme in order to 222 222 ensure tracer conservation and to allow the use of a much smaller value of the Asselin filter parameter. 223 223 The modifications affect both the forcing and filtering treatments in the LF-RA scheme. … … 237 237 The change in the forcing formulation given by \autoref{eq:STP_forcing} (see \autoref{fig:MLF_forcing}) 238 238 has a significant effect: 239 the forcing term no longer excites the divergence of odd and even time steps \citep{ Leclair_Madec_OM09}.239 the forcing term no longer excites the divergence of odd and even time steps \citep{leclair.madec_OM09}. 240 240 % forcing seen by the model.... 241 241 This property improves the LF-RA scheme in two respects. … … 245 245 (last term in \autoref{eq:STP_RA} compared to \autoref{eq:STP_asselin}). 246 246 Since the filtering of the forcing was the source of non-conservation in the classical LF-RA scheme, 247 the modified formulation becomes conservative \citep{ Leclair_Madec_OM09}.247 the modified formulation becomes conservative \citep{leclair.madec_OM09}. 248 248 Second, the LF-RA becomes a truly quasi -second order scheme. 249 249 Indeed, \autoref{eq:STP_forcing} used in combination with a careful treatment of static instability -
NEMO/trunk/doc/latex/NEMO/subfiles/introduction.tex
r10544 r11123 27 27 28 28 The ocean component of \NEMO has been developed from the legacy of the OPA model, release 8.2, 29 described in \citet{ Madec1998}.29 described in \citet{madec.delecluse.ea_NPM98}. 30 30 This model has been used for a wide range of applications, both regional or global, as a forced ocean model and 31 31 as a model coupled with the sea-ice and/or the atmosphere. … … 67 67 Within the \NEMO system the ocean model is interactively coupled with a sea ice model (SI$^3$) and 68 68 a biogeochemistry model (PISCES). 69 Interactive coupling to Atmospheric models is possible via the OASIS coupler \citep{OASIS2006}.69 Interactive coupling to Atmospheric models is possible via the \href{https://portal.enes.org/oasis}{OASIS coupler}. 70 70 Two-way nesting is also available through an interface to the AGRIF package 71 (Adaptative Grid Refinement in \fortran) \citep{ Debreu_al_CG2008}.71 (Adaptative Grid Refinement in \fortran) \citep{debreu.vouland.ea_CG08}. 72 72 % Needs to be reviewed 73 73 %The interface code for coupling to an alternative sea ice model (CICE, \citet{Hunke2008}) has now been upgraded so … … 83 83 The lateral Laplacian and biharmonic viscosity and diffusion can be rotated following 84 84 a geopotential or neutral direction. 85 There is an optional eddy induced velocity \citep{ Gent1990} with a space and time variable coefficient86 \citet{ Treguier1997}.85 There is an optional eddy induced velocity \citep{gent.mcwilliams_JPO90} with a space and time variable coefficient 86 \citet{treguier.held.ea_JPO97}. 87 87 The model has vertical harmonic viscosity and diffusion with a space and time variable coefficient, 88 with options to compute the coefficients with \citet{ Blanke1993}, \citet{Pacanowski_Philander_JPO81}, or89 \citet{ Umlauf_Burchard_JMS03} mixing schemes.88 with options to compute the coefficients with \citet{blanke.delecluse_JPO93}, \citet{pacanowski.philander_JPO81}, or 89 \citet{umlauf.burchard_JMR03} mixing schemes. 90 90 91 91 %%gm To be put somewhere else .... … … 213 213 NEMO/OPA, like all research tools, is in perpetual evolution. 214 214 The present document describes the OPA version include in the release 3.4 of NEMO. 215 This release differs significantly from version 8, documented in \citet{ Madec1998}. \\215 This release differs significantly from version 8, documented in \citet{madec.delecluse.ea_NPM98}. \\ 216 216 217 217 The main modifications from OPA v8 and NEMO/OPA v3.2 are : … … 222 222 \item 223 223 introduction of partial step representation of bottom topography 224 \citep{ Barnier_al_OD06, Le_Sommer_al_OM09, Penduff_al_OS07};224 \citep{barnier.madec.ea_OD06, le-sommer.penduff.ea_OM09, penduff.le-sommer.ea_OS07}; 225 225 \item 226 226 partial reactivation of a terrain-following vertical coordinate ($s$- and hybrid $s$-$z$) with … … 242 242 additional advection schemes for tracers; 243 243 \item 244 implementation of the AGRIF package (Adaptative Grid Refinement in \fortran) \citep{ Debreu_al_CG2008};244 implementation of the AGRIF package (Adaptative Grid Refinement in \fortran) \citep{debreu.vouland.ea_CG08}; 245 245 \item 246 246 online diagnostics : tracers trend in the mixed layer and vorticity balance; … … 255 255 RGB light penetration and optional use of ocean color 256 256 \item 257 major changes in the TKE schemes: it now includes a Langmuir cell parameterization \citep{ Axell_JGR02},258 the \citet{ Mellor_Blumberg_JPO04} surface wave breaking parameterization, and has a time discretization which259 is energetically consistent with the ocean model equations \citep{ Burchard_OM02, Marsaleix_al_OM08};257 major changes in the TKE schemes: it now includes a Langmuir cell parameterization \citep{axell_JGR02}, 258 the \citet{mellor.blumberg_JPO04} surface wave breaking parameterization, and has a time discretization which 259 is energetically consistent with the ocean model equations \citep{burchard_OM02, marsaleix.auclair.ea_OM08}; 260 260 \item 261 261 tidal mixing parametrisation (bottom intensification) + Indonesian specific tidal mixing 262 \citep{ Koch-Larrouy_al_GRL07};262 \citep{koch-larrouy.madec.ea_GRL07}; 263 263 \item 264 264 introduction of LIM-3, the new Louvain-la-Neuve sea-ice model 265 265 (C-grid rheology and new thermodynamics including bulk ice salinity) 266 \citep{ Vancoppenolle_al_OM09a, Vancoppenolle_al_OM09b}266 \citep{vancoppenolle.fichefet.ea_OM09*a, vancoppenolle.fichefet.ea_OM09*b} 267 267 \end{itemize} 268 268 … … 272 272 \item 273 273 introduction of a modified leapfrog-Asselin filter time stepping scheme 274 \citep{ Leclair_Madec_OM09};275 \item 276 additional scheme for iso-neutral mixing \citep{ Griffies_al_JPO98}, although it is still a "work in progress";277 \item 278 a rewriting of the bottom boundary layer scheme, following \citet{ Campin_Goosse_Tel99};279 \item 280 addition of a Generic Length Scale vertical mixing scheme, following \citet{ Umlauf_Burchard_JMS03};274 \citep{leclair.madec_OM09}; 275 \item 276 additional scheme for iso-neutral mixing \citep{griffies.gnanadesikan.ea_JPO98}, although it is still a "work in progress"; 277 \item 278 a rewriting of the bottom boundary layer scheme, following \citet{campin.goosse_T99}; 279 \item 280 addition of a Generic Length Scale vertical mixing scheme, following \citet{umlauf.burchard_JMR03}; 281 281 \item 282 282 addition of the atmospheric pressure as an external forcing on both ocean and sea-ice dynamics; 283 283 \item 284 addition of a diurnal cycle on solar radiation \citep{ Bernie_al_CD07};284 addition of a diurnal cycle on solar radiation \citep{bernie.guilyardi.ea_CD07}; 285 285 \item 286 286 river runoffs added through a non-zero depth, and having its own temperature and salinity; … … 296 296 coupling interface adjusted for WRF atmospheric model; 297 297 \item 298 C-grid ice rheology now available fro both LIM-2 and LIM-3 \citep{ Bouillon_al_OM09};298 C-grid ice rheology now available fro both LIM-2 and LIM-3 \citep{bouillon.maqueda.ea_OM09}; 299 299 \item 300 300 LIM-3 ice-ocean momentum coupling applied to LIM-2; … … 318 318 319 319 \begin{itemize} 320 \item finalisation of above iso-neutral mixing \citep{ Griffies_al_JPO98}";320 \item finalisation of above iso-neutral mixing \citep{griffies.gnanadesikan.ea_JPO98}"; 321 321 \item "Neptune effect" parametrisation; 322 322 \item horizontal pressure gradient suitable for s-coordinate;
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