Changeset 11123 for NEMO/trunk/doc/latex/NEMO/subfiles/chap_SBC.tex
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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.
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