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25 ème Colloque de l’Association Internationale de Climatologie, Grenoble 2012Gallée H. et G. Schayes, 1994 : Development of a Three-Dimensional Meso-gamma Primitive Equations Model,Katabatic Winds Simulation in the area of Terra Nova Bay, Antarctica. Mon. Wea. Rev., 122, 671-685.Gallée H., 1995 : Simulation of the mesocyclonic activity in the Ross Sea, Antarctica. Mon. Wea. Rev., 123,2051-2069.Gallée H. et Duynkerke P. G., 1996 : Air-Snow Interactions and the Surface Energy and Mass Balance over theMelting Zone of West Greenland during GIMEX. Journal of Geophysical Research, 102, 13813-13824.Gallée H., P. Pettré et G. Schayes, 1996 : Sudden cessation of katabatic winds in Adélie Land. Antarctica. J.Appl. Meteorol., 35, 1142-1152.Gallée H. et P. Pettré, 1998 : Dynamical constraints on katabatic wind cessation in Adélie Land. Antarctica. J.Atmos. Sci., 55, 1755-1770.Gallée H., 1998 : A simulation of blowing Snow over the Antarctic Ice Sheet. Ann. Glaciol., 26, 203-205.Gallée H., Guyomarc'h G. et E. Brun, 2001 : Impact of Snow Drift on the Antarctic Ice Sheet Surface MassBalance. Possible Sensitivity to Snow Surface Properties. Boundary-Layer Meterorol., 99, 1-19.Gallée H., Peyaud V. et I. Goodwin, 2005 : Simulation of the net snow accumulation along the Wilkes Landtransect, Antarctica, with a regional climate model. Ann. Glaciol., 41, 17-22.Gallée H., A. Trouvilliez, C. Agosta, C. Genthon, V. Favier et F. Naaim-Bouvet, 2012 : Transport of snow by thewind: a comparison between observations made in Adélie Land, Antarctica, and simulations made with theRegional Climate Model MAR. Accepted for publication in Boundary Layer Meteorology.Parish T. R., 1988 : Surface winds over the Antarctic continent: A review. Rev. Geophys., 26(1), 169-180,doi:10.1029/RG026i001p00169Solomon S., D. Qin, M. Manning, Z. Chen, M. Marquis, K. B. Averyt, M. Tignor et H. L. Miller (eds.), 2007 :Contribution of Working Group I to the Fourth Assessment Report of the Intergovernmental Panel on ClimateChange. Cambridge University Press, Cambridge, United Kingdom and New York, NY, USA, 996 pp.320
25 ème Colloque de l’Association Internationale de Climatologie, Grenoble 2012UTILISATION DES INDICATEURS DU DÉFICIT HYDRIQUE DANSLES SYNTHÈSES BIOCLIMATIQUES MÉDITERRANÉENNESAmor Mokhtar GAMMAR 1 et Zouheir HLAOUI 21UR BiCADE, Université de la Manouba – Tunisie. amorgammar@yahoo.fr2UR GRECACHOT, Université de Tunis – Tunisie. Zouhaierhlaoui@yahoo.frRésumé : L’établissement du bilan hydrique de 18 stations tunisiennes permet le calcul du déficit hydriquerelatif et son utilisation pour exprimer l’intensité de la sécheresse. Les valeurs de cet indicateur donnent unclassement des stations qui paraît en concordance avec l’interprétation de la végétation et de l’occupation dessols et qui permet de délimiter et redéfinir les étages bioclimatiques méditerranéens à déterminisme xérique.Mots-clés : Bioclimatologie, bilan hydrique, Tunisie, phyto-écologie.Abstract: Use of water deficit indicators in the Mediterranean bioclimatic synthesis.The water balance of 18 Tunisian stations allows the calculation of the relative water deficit and its use toexpress the intensity of drought. The values of this indicator show the stations classifying which seems inaccordance with the interpretation of vegetation and land use and it enable a new delimitation and redefine thebioclimatic Mediterranean Thresholds with xeric determinism.Keywords: Bioclimatology, water balance, Tunisia, phyto-écology.IntroductionDeux systèmes majeurs qui proposent des synthèses bioclimatiques adaptées au domaineméditerranéen sont couramment utilisés par les chercheurs. Le système de Gaussen etBagnouls exploite les diagrammes ombrothermiques qui permettent une estimation de ladurée de la période sèche (Bagnouls et Gaussen 1957).Le système d’Emberger repose sur leclimagramme d’Emberger, que des auteurs phytoécologuesont repris et retouché pour le rendre plussimple et plus conforme à la répartition desformations végétales, objet de leurs observations(Gounot, 1958 ; Bortoli, 1967 ; Le Houérou, 1959,1977 ; Lecompte, 1986). Dans ce document (figure1), la rigueur du froid hivernal est représentée parla valeur de la moyenne des minima du mois le plusfroid (m), alors que l’intensité de la sécheresse estdéterminée par un système complexe qui se réfère àun indice empirique d’aridité (le quotientpluviothermique d’Emberger : Q 2 ) et surtout quis’appuie sur l’interprétation de la végétation auxalentours des stations climatiques, pour les classerdans des étages bioclimatiques. Par rapport à l’axede l’indice pluviothermique, ces limites inspiréespar la végétation et les performances agricoles, sontcourbes, ce qui prouve la difficulté d’exprimerdirectement et synthétiquement la sécheresse pardes paramètres climatiques.Figure 1 : Stations tunisiennes dans leclimagramme d’Emberger.Le développement de la notion de l’évapotranspiration potentielle (ETP) à partir du milieudu XX ème siècle a permis d’envisager de construire des bilans hydriques bioclimatiques à la321
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