Changeset 11263 for NEMO/branches/2019/dev_r10984_HPC-13_IRRMANN_BDY_optimization/doc/latex/NEMO/subfiles/chap_SBC.tex
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NEMO/branches/2019/dev_r10984_HPC-13_IRRMANN_BDY_optimization/doc/latex/NEMO/subfiles/chap_SBC.tex
r10614 r11263 5 5 % Chapter —— Surface Boundary Condition (SBC, ISF, ICB) 6 6 % ================================================================ 7 \chapter{Surface Boundary Condition (SBC, ISF, ICB) 7 \chapter{Surface Boundary Condition (SBC, ISF, ICB)} 8 8 \label{chap:SBC} 9 9 \minitoc … … 226 226 % Input Data specification (\mdl{fldread}) 227 227 % ------------------------------------------------------------------------------------------------------------- 228 \subsection{Input data specification (\protect\mdl{fldread})} 228 \subsection[Input data specification (\textit{fldread.F90})] 229 {Input data specification (\protect\mdl{fldread})} 229 230 \label{subsec:SBC_fldread} 230 231 … … 313 314 The only tricky point is therefore to specify the date at which we need to do the interpolation and 314 315 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.316 Following \citet{leclair.madec_OM09}, the date of a time step is set at the middle of the time step. 316 317 For example, for an experiment starting at 0h00'00" with a one hour time-step, 317 318 a time interpolation will be performed at the following time: 0h30'00", 1h30'00", 2h30'00", etc. … … 559 560 % Analytical formulation (sbcana module) 560 561 % ================================================================ 561 \section{Analytical formulation (\protect\mdl{sbcana})} 562 \section[Analytical formulation (\textit{sbcana.F90})] 563 {Analytical formulation (\protect\mdl{sbcana})} 562 564 \label{sec:SBC_ana} 563 565 … … 584 586 % Flux formulation 585 587 % ================================================================ 586 \section{Flux formulation (\protect\mdl{sbcflx})} 588 \section[Flux formulation (\textit{sbcflx.F90})] 589 {Flux formulation (\protect\mdl{sbcflx})} 587 590 \label{sec:SBC_flx} 588 591 %------------------------------------------namsbc_flx---------------------------------------------------- … … 606 609 % ================================================================ 607 610 \section[Bulk formulation {(\textit{sbcblk\{\_core,\_clio\}.F90})}] 608 611 {Bulk formulation {(\protect\mdl{sbcblk\_core}, \protect\mdl{sbcblk\_clio})}} 609 612 \label{sec:SBC_blk} 610 613 … … 625 628 % CORE Bulk formulea 626 629 % ------------------------------------------------------------------------------------------------------------- 627 \subsection{CORE formulea (\protect\mdl{sbcblk\_core}, \protect\np{ln\_core}\forcode{ = .true.})} 630 \subsection[CORE formulea (\textit{sbcblk\_core.F90}, \forcode{ln_core = .true.})] 631 {CORE formulea (\protect\mdl{sbcblk\_core}, \protect\np{ln\_core}\forcode{ = .true.})} 628 632 \label{subsec:SBC_blk_core} 629 633 %------------------------------------------namsbc_core---------------------------------------------------- … … 632 636 %------------------------------------------------------------------------------------------------------------- 633 637 634 The CORE bulk formulae have been developed by \citet{ Large_Yeager_Rep04}.638 The CORE bulk formulae have been developed by \citet{large.yeager_rpt04}. 635 639 They have been designed to handle the CORE forcing, a mixture of NCEP reanalysis and satellite data. 636 640 They use an inertial dissipative method to compute the turbulent transfer coefficients 637 641 (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 through642 This \citet{large.yeager_rpt04} dataset is available through 639 643 the \href{http://nomads.gfdl.noaa.gov/nomads/forms/mom4/CORE.html}{GFDL web site}. 640 644 641 645 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}.646 This is the so-called DRAKKAR Forcing Set (DFS) \citep{brodeau.barnier.ea_OM10}. 643 647 644 648 Options are defined through the \ngn{namsbc\_core} namelist variables. … … 688 692 % CLIO Bulk formulea 689 693 % ------------------------------------------------------------------------------------------------------------- 690 \subsection{CLIO formulea (\protect\mdl{sbcblk\_clio}, \protect\np{ln\_clio}\forcode{ = .true.})} 694 \subsection[CLIO formulea (\textit{sbcblk\_clio.F90}, \forcode{ln_clio = .true.})] 695 {CLIO formulea (\protect\mdl{sbcblk\_clio}, \protect\np{ln\_clio}\forcode{ = .true.})} 691 696 \label{subsec:SBC_blk_clio} 692 697 %------------------------------------------namsbc_clio---------------------------------------------------- … … 696 701 697 702 The CLIO bulk formulae were developed several years ago for the Louvain-la-neuve coupled ice-ocean model 698 (CLIO, \cite{ Goosse_al_JGR99}).703 (CLIO, \cite{goosse.deleersnijder.ea_JGR99}). 699 704 They are simpler bulk formulae. 700 705 They assume the stress to be known and compute the radiative fluxes from a climatological cloud cover. … … 729 734 % Coupled formulation 730 735 % ================================================================ 731 \section{Coupled formulation (\protect\mdl{sbccpl})} 736 \section[Coupled formulation (\textit{sbccpl.F90})] 737 {Coupled formulation (\protect\mdl{sbccpl})} 732 738 \label{sec:SBC_cpl} 733 739 %------------------------------------------namsbc_cpl---------------------------------------------------- … … 770 776 % Atmospheric pressure 771 777 % ================================================================ 772 \section{Atmospheric pressure (\protect\mdl{sbcapr})} 778 \section[Atmospheric pressure (\textit{sbcapr.F90})] 779 {Atmospheric pressure (\protect\mdl{sbcapr})} 773 780 \label{sec:SBC_apr} 774 781 %------------------------------------------namsbc_apr---------------------------------------------------- … … 806 813 % Surface Tides Forcing 807 814 % ================================================================ 808 \section{Surface tides (\protect\mdl{sbctide})} 815 \section[Surface tides (\textit{sbctide.F90})] 816 {Surface tides (\protect\mdl{sbctide})} 809 817 \label{sec:SBC_tide} 810 818 … … 819 827 \[ 820 828 % \label{eq:PE_dyn_tides} 821 \frac{\partial {\ rm {\bf U}}_h }{\partial t}= ...829 \frac{\partial {\mathrm {\mathbf U}}_h }{\partial t}= ... 822 830 +g\nabla (\Pi_{eq} + \Pi_{sal}) 823 831 \] … … 839 847 840 848 The SAL term should in principle be computed online as it depends on 841 the model tidal prediction itself (see \citet{ Arbic2004} for a849 the model tidal prediction itself (see \citet{arbic.garner.ea_DSR04} for a 842 850 discussion about the practical implementation of this term). 843 851 Nevertheless, the complex calculations involved would make this … … 857 865 % River runoffs 858 866 % ================================================================ 859 \section{River runoffs (\protect\mdl{sbcrnf})} 867 \section[River runoffs (\textit{sbcrnf.F90})] 868 {River runoffs (\protect\mdl{sbcrnf})} 860 869 \label{sec:SBC_rnf} 861 870 %------------------------------------------namsbc_rnf---------------------------------------------------- … … 871 880 %coastal modelling and becomes more and more often open ocean and climate modelling 872 881 %\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}.}.882 %required to properly represent the diurnal cycle \citep{bernie.woolnough.ea_JC05}. see also \autoref{fig:SBC_dcy}.}. 874 883 875 884 … … 892 901 \footnote{ 893 902 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}.903 properly represent the diurnal cycle \citep{bernie.woolnough.ea_JC05}. 895 904 see also \autoref{fig:SBC_dcy}.}. 896 905 … … 982 991 % Ice shelf melting 983 992 % ================================================================ 984 \section{Ice shelf melting (\protect\mdl{sbcisf})} 993 \section[Ice shelf melting (\textit{sbcisf.F90})] 994 {Ice shelf melting (\protect\mdl{sbcisf})} 985 995 \label{sec:SBC_isf} 986 996 %------------------------------------------namsbc_isf---------------------------------------------------- … … 989 999 %-------------------------------------------------------------------------------------------------------- 990 1000 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}.1001 Description and result of sensitivity test to \np{nn\_isf} are presented in \citet{mathiot.jenkins.ea_GMD17}. 992 1002 The different options are illustrated in \autoref{fig:SBC_isf}. 993 1003 … … 1001 1011 \item[\np{nn\_isfblk}\forcode{ = 1}]: 1002 1012 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}.1013 the latent heat flux at the ice shelf base. A complete description is available in \citet{hunter_rpt06}. 1004 1014 \item[\np{nn\_isfblk}\forcode{ = 2}]: 1005 1015 The melt rate and the heat flux are based on a 3 equations formulation 1006 1016 (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}.1017 A complete description is available in \citet{jenkins_JGR91}. 1008 1018 \end{description} 1009 1019 1010 Temperature and salinity used to compute the melt are the average temperature in the top boundary layer \citet{ Losch2008}.1020 Temperature and salinity used to compute the melt are the average temperature in the top boundary layer \citet{losch_JGR08}. 1011 1021 Its thickness is defined by \np{rn\_hisf\_tbl}. 1012 1022 The fluxes and friction velocity are computed using the mean temperature, salinity and velocity in the the first \np{rn\_hisf\_tbl} m. … … 1038 1048 \] 1039 1049 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.1050 See \citet{jenkins.nicholls.ea_JPO10} for all the details on this formulation. It is the recommended formulation for realistic application. 1041 1051 \item[\np{nn\_gammablk}\forcode{ = 2}]: 1042 1052 The salt and heat exchange coefficients are velocity and stability dependent and defined as: … … 1047 1057 $\Gamma_{Turb}$ the contribution of the ocean stability and 1048 1058 $\Gamma^{T,S}_{Mole}$ the contribution of the molecular diffusion. 1049 See \citet{ Holland1999} for all the details on this formulation.1059 See \citet{holland.jenkins_JPO99} for all the details on this formulation. 1050 1060 This formulation has not been extensively tested in NEMO (not recommended). 1051 1061 \end{description} 1052 1062 \item[\np{nn\_isf}\forcode{ = 2}]: 1053 1063 The ice shelf cavity is not represented. 1054 The fwf and heat flux are computed using the \citet{ Beckmann2003} parameterisation of isf melting.1064 The fwf and heat flux are computed using the \citet{beckmann.goosse_OM03} parameterisation of isf melting. 1055 1065 The fluxes are distributed along the ice shelf edge between the depth of the average grounding line (GL) 1056 1066 (\np{sn\_depmax\_isf}) and the base of the ice shelf along the calving front … … 1089 1099 \begin{figure}[!t] 1090 1100 \begin{center} 1091 \includegraphics[width= 0.8\textwidth]{Fig_SBC_isf}1101 \includegraphics[width=\textwidth]{Fig_SBC_isf} 1092 1102 \caption{ 1093 1103 \protect\label{fig:SBC_isf} … … 1166 1176 %------------------------------------------------------------------------------------------------------------- 1167 1177 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} ).1178 Icebergs are modelled as lagrangian particles in NEMO \citep{marsh.ivchenko.ea_GMD15}. 1179 Their physical behaviour is controlled by equations as described in \citet{martin.adcroft_OM10} ). 1170 1180 (Note that the authors kindly provided a copy of their code to act as a basis for implementation in NEMO). 1171 1181 Icebergs are initially spawned into one of ten classes which have specific mass and thickness as … … 1227 1237 % Interactions with waves (sbcwave.F90, ln_wave) 1228 1238 % ------------------------------------------------------------------------------------------------------------- 1229 \section{Interactions with waves (\protect\mdl{sbcwave}, \protect\np{ln\_wave})} 1239 \section[Interactions with waves (\textit{sbcwave.F90}, \texttt{ln\_wave})] 1240 {Interactions with waves (\protect\mdl{sbcwave}, \protect\np{ln\_wave})} 1230 1241 \label{sec:SBC_wave} 1231 1242 %------------------------------------------namsbc_wave-------------------------------------------------------- … … 1258 1269 1259 1270 % ================================================================ 1260 \subsection{Neutral drag coefficient from wave model (\protect\np{ln\_cdgw})} 1271 \subsection[Neutral drag coefficient from wave model (\texttt{ln\_cdgw})] 1272 {Neutral drag coefficient from wave model (\protect\np{ln\_cdgw})} 1261 1273 \label{subsec:SBC_wave_cdgw} 1262 1274 … … 1265 1277 Then using the routine \rou{turb\_ncar} and starting from the neutral drag coefficent provided, 1266 1278 the drag coefficient is computed according to the stable/unstable conditions of the 1267 air-sea interface following \citet{ Large_Yeager_Rep04}.1279 air-sea interface following \citet{large.yeager_rpt04}. 1268 1280 1269 1281 … … 1271 1283 % 3D Stokes Drift (ln_sdw, nn_sdrift) 1272 1284 % ================================================================ 1273 \subsection{3D Stokes Drift (\protect\np{ln\_sdw, nn\_sdrift})} 1285 \subsection[3D Stokes Drift (\texttt{ln\_sdw}, \texttt{nn\_sdrift})] 1286 {3D Stokes Drift (\protect\np{ln\_sdw, nn\_sdrift})} 1274 1287 \label{subsec:SBC_wave_sdw} 1275 1288 1276 The Stokes drift is a wave driven mechanism of mass and momentum transport \citep{ Stokes_1847}.1289 The Stokes drift is a wave driven mechanism of mass and momentum transport \citep{stokes_ibk09}. 1277 1290 It is defined as the difference between the average velocity of a fluid parcel (Lagrangian velocity) 1278 1291 and the current measured at a fixed point (Eulerian velocity). … … 1307 1320 \begin{description} 1308 1321 \item[\np{nn\_sdrift} = 0]: exponential integral profile parameterization proposed by 1309 \citet{ Breivik_al_JPO2014}:1322 \citet{breivik.janssen.ea_JPO14}: 1310 1323 1311 1324 \[ … … 1327 1340 \item[\np{nn\_sdrift} = 1]: velocity profile based on the Phillips spectrum which is considered to be a 1328 1341 reasonable estimate of the part of the spectrum most contributing to the Stokes drift velocity near the surface 1329 \citep{ Breivik_al_OM2016}:1342 \citep{breivik.bidlot.ea_OM16}: 1330 1343 1331 1344 \[ … … 1367 1380 % Stokes-Coriolis term (ln_stcor) 1368 1381 % ================================================================ 1369 \subsection{Stokes-Coriolis term (\protect\np{ln\_stcor})} 1382 \subsection[Stokes-Coriolis term (\texttt{ln\_stcor})] 1383 {Stokes-Coriolis term (\protect\np{ln\_stcor})} 1370 1384 \label{subsec:SBC_wave_stcor} 1371 1385 … … 1381 1395 % Waves modified stress (ln_tauwoc, ln_tauw) 1382 1396 % ================================================================ 1383 \subsection{Wave modified sress (\protect\np{ln\_tauwoc, ln\_tauw})} 1397 \subsection[Wave modified sress (\texttt{ln\_tauwoc}, \texttt{ln\_tauw})] 1398 {Wave modified sress (\protect\np{ln\_tauwoc, ln\_tauw})} 1384 1399 \label{subsec:SBC_wave_tauw} 1385 1400 1386 1401 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 not1402 into the waves \citep{janssen.breivik.ea_rpt13}. Therefore, when waves are growing, momentum and energy is spent and is not 1388 1403 available for forcing the mean circulation, while in the opposite case of a decaying sea 1389 1404 state more momentum is available for forcing the ocean. … … 1428 1443 % Diurnal cycle 1429 1444 % ------------------------------------------------------------------------------------------------------------- 1430 \subsection{Diurnal cycle (\protect\mdl{sbcdcy})} 1445 \subsection[Diurnal cycle (\textit{sbcdcy.F90})] 1446 {Diurnal cycle (\protect\mdl{sbcdcy})} 1431 1447 \label{subsec:SBC_dcy} 1432 1448 %------------------------------------------namsbc_rnf---------------------------------------------------- … … 1438 1454 \begin{figure}[!t] 1439 1455 \begin{center} 1440 \includegraphics[width= 0.8\textwidth]{Fig_SBC_diurnal}1456 \includegraphics[width=\textwidth]{Fig_SBC_diurnal} 1441 1457 \caption{ 1442 1458 \protect\label{fig:SBC_diurnal} … … 1445 1461 the mean value of the analytical cycle (blue line) over a time step, 1446 1462 not as the mid time step value of the analytically cycle (red square). 1447 From \citet{ Bernie_al_CD07}.1463 From \citet{bernie.guilyardi.ea_CD07}. 1448 1464 } 1449 1465 \end{center} … … 1451 1467 %>>>>>>>>>>>>>>>>>>>>>>>>>>>> 1452 1468 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.1469 \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 1470 Unfortunately high frequency forcing fields are rare, not to say inexistent. 1455 1471 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}.1472 high frequency \citep{bernie.guilyardi.ea_CD07}. 1457 1473 Furthermore, only the knowledge of daily mean value of SWF is needed, 1458 1474 as higher frequency variations can be reconstructed from them, 1459 1475 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 by1476 The \cite{bernie.guilyardi.ea_CD07} reconstruction algorithm is available in \NEMO by 1461 1477 setting \np{ln\_dm2dc}\forcode{ = .true.} (a \textit{\ngn{namsbc}} namelist variable) when 1462 1478 using CORE bulk formulea (\np{ln\_blk\_core}\forcode{ = .true.}) or 1463 1479 the flux formulation (\np{ln\_flx}\forcode{ = .true.}). 1464 1480 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}.1481 The detail of the algoritm used can be found in the appendix~A of \cite{bernie.guilyardi.ea_CD07}. 1466 1482 The algorithm preserve the daily mean incoming SWF as the reconstructed SWF at 1467 1483 a given time step is the mean value of the analytical cycle over this time step (\autoref{fig:SBC_diurnal}). … … 1476 1492 \begin{figure}[!t] 1477 1493 \begin{center} 1478 \includegraphics[width= 0.7\textwidth]{Fig_SBC_dcy}1494 \includegraphics[width=\textwidth]{Fig_SBC_dcy} 1479 1495 \caption{ 1480 1496 \protect\label{fig:SBC_dcy} … … 1514 1530 % Surface restoring to observed SST and/or SSS 1515 1531 % ------------------------------------------------------------------------------------------------------------- 1516 \subsection{Surface restoring to observed SST and/or SSS (\protect\mdl{sbcssr})} 1532 \subsection[Surface restoring to observed SST and/or SSS (\textit{sbcssr.F90})] 1533 {Surface restoring to observed SST and/or SSS (\protect\mdl{sbcssr})} 1517 1534 \label{subsec:SBC_ssr} 1518 1535 %------------------------------------------namsbc_ssr---------------------------------------------------- … … 1546 1563 (observed, climatological or an atmospheric model product), 1547 1564 \textit{SSS}$_{Obs}$ is a sea surface salinity 1548 (usually a time interpolation of the monthly mean Polar Hydrographic Climatology \citep{ Steele2001}),1565 (usually a time interpolation of the monthly mean Polar Hydrographic Climatology \citep{steele.morley.ea_JC01}), 1549 1566 $\left.S\right|_{k=1}$ is the model surface layer salinity and 1550 1567 $\gamma_s$ is a negative feedback coefficient which is provided as a namelist parameter. 1551 1568 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}.1569 the atmosphere does not care about ocean surface salinity \citep{madec.delecluse_IWN97}. 1553 1570 The SSS restoring term should be viewed as a flux correction on freshwater fluxes to 1554 1571 reduce the uncertainties we have on the observed freshwater budget. … … 1593 1610 % {Description of Ice-ocean interface to be added here or in LIM 2 and 3 doc ?} 1594 1611 1595 \subsection{Interface to CICE (\protect\mdl{sbcice\_cice})} 1612 \subsection[Interface to CICE (\textit{sbcice\_cice.F90})] 1613 {Interface to CICE (\protect\mdl{sbcice\_cice})} 1596 1614 \label{subsec:SBC_cice} 1597 1615 … … 1626 1644 % Freshwater budget control 1627 1645 % ------------------------------------------------------------------------------------------------------------- 1628 \subsection{Freshwater budget control (\protect\mdl{sbcfwb})} 1646 \subsection[Freshwater budget control (\textit{sbcfwb.F90})] 1647 {Freshwater budget control (\protect\mdl{sbcfwb})} 1629 1648 \label{subsec:SBC_fwb} 1630 1649
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