Extrait du deliverable EMBRACE (http://www.embrace-project.eu/)
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VOIR LE SETUP DU CAS DANS 1D_setupII_final.pdf
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Les profils initiaux sont dans ~script_rio/initial_profil_zPthrv_uv_Tq_ref.txt
Les forcages sont dans ~script_rio/tendency_profil_zPthrv_uv_Tq_ref.txt
Ces deux fichiers sont ensuite transformes en un fichier unique: amma.nc  (par create_netcdf.F90 dans ~script_rio)
Les differents fichiers de forcage sont dans ~script_rio et portent un nom qui les rattache a tel ou tel
test de sensibilite.
Il faut ensuite le recopier dans ../script_rio/amma.nc car l executable ne connait que ce fichier.
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Des tests de sensibilite et d'ensemble ont ete faits ensuite.
Leur description est disponible dans: ~amma/tab_sensitivity_tests.pdf
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Pour compiler: compile.x
Pour executer, utiliser le fichier mr (modele run)
en precisant:
	+ le nombre de niveaux dans NLEV=
	+ le pas de temps dans TSTEP=, qui sera ecrit dans gcm.def
	+ la physique a utiliser dans une ligne de la forme:
	7)  PHYSIQ=toto           ;EXPER="$PHYSIQ"_L"$NLEV"_"$TSTEP"s;;
	Vous devez avoir sous ~1dcases/amma, un directory deftoto contenant les fichers *.def
	Si vous lancez mr 7, le modele produira un directory "$toto"_L"$NLEV"_"$TSTEP"s
	contenant les fichiers resultat et les fichiers *def
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Pour faire tourner le cas avec une discretisation verticale imposee de 70 niveaux,
mettre vert_sampling=read dans gcm.def
Sinon, verifier que vert_sampling=tropo !!!
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The case study investigated here is the AMMA case of 10 July 2006 where a relatively small and short-lived convective system  developed over Niamey (Lothon et al., 2011). Note nevertheless, than even if small, the system involved the development of a few cells during its whole life cycle which ended 300 km to the west of the location of initiation. The whole transition has been caught by several ground-based instruments (radar, wind profiler and atmospheric soundings) and completed by satellite data. This case study concerns a typical case of transition from shallow to deep convection over semi-arid lands, as frequently observed in the Sahel in late Spring, before the onset of the monsoon. It is characterized by a high Bowen Ratio (Bo~10), and associated with an elevated cloud base (about 2.5 km). In the following, the set-up, the different Earth System Models (ESM), and the different runs are described.
The set-up is the same one for the ESM 1D column simulations and  for the high-resolution simulation. It is  summarized here but more extensively described in Couvreux et al. (2012). Surface sensible and latent heat fluxes inferred from observations (Figure 1) are prescribed. The initial profiles are  derived from an early morning sounding and are shown in Figure 1. Compared to other cases of inter-comparison (over the Southern Great Plains: Guichard et al., 2004 or the Amazons : Kharoutdinov and Randall, 2006), the vertical profile  is warmer and characterized by a smaller lapse rate between 1000 and 5000 m. Finally, a specificity of West Africa is the existence of the African easterly jet, located at about 4000 m. The early-morning low-level jet is also a typical feature. However, this jet is quickly eroded and wind speed decreases substantially within a few hours on this day (at 0900 UTC it is already less than 5 m s−1 in the boundary layer).
	The large-scale advection are based on the ECMWF reanalysis (Agusti-Panareda et al., 2010) together with inferences from observations. Namely, they consist in a cooling (0.3 K h−1 maximum) and a moistening (0.3 g kg−1 h−1 maximum) of the low levels (below 3000m) in the morning. This is a simple but physically based approach accounting for the thermodynamic impact of the monsoon flow. In fact, the vertical structure, magnitude and diurnal phasing of these advective processes are fairly consistent with the horizontal advection simulated by the ECMWF analysis over the Sahel prior to the monsoon onset (not shown) and with the results of Peyrille and Lafore (2007). The radiative tendency is also prescribed as the models are  run without activating the radiation scheme; this implies cutting off any feedbacks between clouds and radiation. Eventually, a large-scale vertical velocity of 1.5 cm s−1 from 1200 to 1800 UTC is prescribed below 5000m to represent the mesoscale circulations induced by surface heterogeneities. The influence of surface heterogeneities will be addressed in a future deliverable. 
The Coriolis effect is ignored. The simulations starts at 0600 UTC and runs up to 1800 or 2400 UTC depending on the cases and models. 
