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194 1 0.98 0.96 0.94 0.92 0.9 0.88 0.86 0.84 0.82 0.8 BI IP FR ME SC AL MT EE 1 0.9 0.8 0.7 0.6 0.5 0.4 0.3 0.2 0.1 0 BI IP FR ME SC AL MT EE ALL ALL 1 0.98 0.96 0.94 0.92 0.9 0.88 0.86 0.84 0.82 0.8 BI IP FR ME SC AL MT EE 1 0.9 0.8 0.7 0.6 0.5 0.4 0.3 0.2 0.1 0 BI IP FR ME SC AL MT EE ALL ALL 1 0.98 0.96 0.94 0.92 0.9 0.88 0.86 0.84 0.82 0.8 BI IP FR ME SC AL MT EE 1 0.9 0.8 0.7 0.6 0.5 0.4 0.3 0.2 0.1 0 BI IP FR ME SC AL MT EE ALL ALL Figure 1. Taylor’s scores for the first, second and fourth order, temperature. Figure 2. Taylor’s scores for the first, second and fourth order, precipitation
195 AMMA-Model Intercomparison Project F Hourdin., J Polcher, F Guichard, F Favot, JP Lafore, JL Redelsperger, Ruti PM*., A Dell'Aquila, T Losada., AK Traoer paolo.ruti@enea.it AMMA-MIP is a Model Intercomparison Project developed in the frame of the African Monsoon Multi disciplinary Analysis project (AMMA). It is a light exercise of intercomparison and evaluation of both global and regional atmospheric models, focused on the study of the seasonal and intraseasonal variations of the climate and rainfall over Sahel. Taking advantage of the relative zonal symmetry of the West African climate, one major target of the exercise is the documentation of a meridional cross section made of zonally averaged (10W-10E) outputs. The African Monsoon is characterized by a well defined meridional structure of albedo and vegetation (Fig. 1 A), with weaker longitudinal variations. This structure is tightly connected to that of the mean rainfall (Fig. 1 B), with maximum rainfall occuring in the Sudanian region (8N-12N) during northern summer, and a sharp transition over Sahel (12N-20N), a particularly sensitive region which has undergone a strong drought in the late 70s and 80s. The meridional structure of the mean rainfall is itself related to the mean meridional circulation with a near surface monsoon flow which brings to the African continent water evaporated over the Guinea gulf. This monsoon flow converges with a southward dry air flow coming from Sahara at the ”intertropical discontinuity”, in the region of the Saharian heat low where dry convection occurs. The return branch of this Hadley circulation at around 600 hPa is associated through angular momentum budget and thermal wind balance with the African Easterly Jet which, in turn, carries additional water from the Indian ocean. At around 10N, one finds the Inter Tropical Convergence Zone where most of the convective rainfall occurs, with a mean upward motion which reaches 200 hPa where the Tropopause Easterly Jet takes place. Figure 1:Picture of West Africa albedo (A) (source EUMETSAT/GEM,http://wwwgem.jrc.it/stars/ albedo.htm) and GPCP cumulated rainfall (B) for year 2000 (mm). The red rectangle corresponds to the zone retained for the AMMA-CROSS section and the green rectangles to the meso-scale AMMA sites. We present here the main diagnostics tailored for the West African monsoon dynamics and we discuss first results and further extension.
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2 nd International Lund RCM Worksho
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Associated Organisations ENSEMBLES
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Preface This Second Lund Regional-s
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II High-resolution dynamical downsc
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IV Investigation of added value at
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VI Soil organic layer: Implications
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VIII Session 4: Regional Observatio
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X Predicting water resources in Wes
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XII The impact of atmospheric therm
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XIV Observation and simulation with
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XVI Favot F .......................
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XVIII Ruoho-Airola T...............
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2 5. Influence of SN on the Ensembl
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4 (+/- 5 days) were used to increas
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6 Dynamical downscaling: Assessment
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8 Improvement of long-term integrat
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10 air temperature annual cycle (Fi
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12 Sensitivity study of CRCM-simula
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14 Regional precipitation anomalies
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16 Assessment of precipitation as s
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18 The Asian summer monsoon in ERA4
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20 Added value of limited area mode
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22 Sensitivity of CRCM basin annual
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24 High-resolution dynamical downsc
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26 There is nevertheless a large ag
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28 technique, as it is based on the
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30 4. Heating mechanism In order to
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32 The geographical distribution of
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34 The CCM scheme reveals a distinc
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36 Performance of pattern scaling i
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38 Evaluation of the analyzed large
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40 Sensitivity studies with a stati
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42 5SL, the results suggest that 5S
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44 are however occasional episodes
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46 this season, as well as the high
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48 Figure 1. Precipitation rate (mm
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50 References Biau. G., E. Zorita,
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52 Investigation of regional climat
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54 Selected examples of the added v
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56 The climate change in Europe sim
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58 Simulation of South Asian summer
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7.5 8.5 9.5 10.5 60 For the climato
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62 precipitation field was more clo
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64 3. Results Fig. 2 shows the anal
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66 Is the position of the model dom
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68 question E. Finally a 10-member
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Figure 2. Same as in Fig.1 but for
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72 Will, A., M. Baldauf, B. Rockel,
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74 ( ) with i = 1,K,n; j = 1,K,m;
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76 Investigation of precipitation o
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78 Impacts of the spectral nudging
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80 Extremes and predictability in t
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82 Large-scale skill in regional cl
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84 Figure 3: As Figure 1 but for Wi
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86 The models capture this pattern
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88 of the simulations due to the di
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91 Examining the relative roles con
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93 Dynamical coupling of the HIRHAM
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95 A parameterization of aircraft i
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97 Stratospheric variability and it
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99 Effects of numerical methods on
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101 Development of a climate model
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103 Study of the capability of the
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105 Evaluation of the land surface
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107 Simulation of the precipitation
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109 Climate simulations over North
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111 Soil organic layer: Implication
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113 4. Results The method how to do
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115 Figure 1. Observed (a) and simu
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117 Evaluation of the Rossby Centre
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119 Simulating aerosols in the regi
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121 Moisture availability and the r
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123 Temperature and precipitation s
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125 4. Preliminary results for down
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127 a) Knutson, T.R., J.J. Sirutis,
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129 Effects of variations in climat
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131 3.2. Precipitation The ensemble
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133 knowledge is essential to asses
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135 pronounced biases in the simula
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137 variability was concentrated at
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139 Investigation of ‘Hurricane K
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141 Evaluation of seasonal forecast
Page 169 and 170: 143 NASH J. E., SUTCLIFFE J. V., 19
Page 171 and 172: 145 Climate change assessment over
Page 173 and 174: 147 For relative operating characte
Page 175 and 176: 149 responsible for the excessive s
Page 177 and 178: 151 and 30km). Domains D1 (90 and 6
Page 179 and 180: 153 can be seen in Fig. 2, where th
Page 181 and 182: 155 High-resolution simulation of a
Page 183 and 184: 157 MesoClim - A mesoscale alpine c
Page 185 and 186: 159 Observed and modeled extremes i
Page 187 and 188: 161 analyzed the surface wind behav
Page 189 and 190: 163 summer particularly in the Paci
Page 191 and 192: 165 since 01.01.2004. For the Meteo
Page 193 and 194: 167 Wind, m/s 12 10 8 6 4 2 Vilsand
Page 195 and 196: 169 heterogeneity. For example, lar
Page 197 and 198: 171 Analysis of surface air tempera
Page 199 and 200: 173 Environmental database and the
Page 201 and 202: Climate change and water pollution
Page 203 and 204: 177 During summer, winds over the M
Page 205 and 206: 179 followed nearly the correct pat
Page 207 and 208: 181 Verification of simulated near
Page 209 and 210: 183 The North American Regional Cli
Page 211 and 212: 185 An atmosphere-ocean regional cl
Page 213 and 214: 187 different rainfall characterist
Page 215 and 216: 189 with increasing temperature. Mo
Page 217 and 218: 191 Inter-comparison of Asian monso
Page 219: 193 On the validation of RCMs in te
Page 223 and 224: 197 parameterization are used in th
Page 225 and 226: 199 Evaluation of European snow cov
Page 227 and 228: 201 Projections of eastern Mediterr
Page 229 and 230: 203 Atmospheric river induced heavy
Page 231 and 232: 205 CLARIS project: Towards climate
Page 233 and 234: 207 Influence of soil moisture init
Page 235 and 236: 209 Projection of the Changes in th
Page 237 and 238: 211 Regional climate model studies
Page 239 and 240: 213 ENSEMBLES regional climate mode
Page 241 and 242: 215 Assessing the performance of se
Page 243 and 244: 217 Applying the Rossby Centre Regi
Page 245 and 246: 219 Interactions between European s
Page 247 and 248: 221 ALADIN-Climate/CZ simulation of
Page 249 and 250: 223 experiment of recreating the pr
Page 251 and 252: 225 Figure 2. the 10-year averaged
Page 253 and 254: 227 Use of regional climate models
Page 255 and 256: 229 Wave estimations using winds fr
Page 257 and 258: 231 Figure 1. Model domain for the
Page 259 and 260: 233 A coupled regional climate mode
Page 261 and 262: 235 Arctic regional coupled downsca
Page 263 and 264: 237 Convection-resolving regional c
Page 265 and 266: 239 4. Outlook Currently a coupled
Page 267 and 268: 241 distribution within the Netherl
Page 269 and 270: 243 Very high-resolution regional c
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245 Impact of convective parameteri
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247 Development of a regional ocean
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249 Regional climate change impact
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251 River runoff projection of futu
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253 Application of regional-scale c
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255 Local air mass dependence of ex
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257 Impact of vegetation on the sim
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259 Climate change impacts on the w
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261 Influence of soil moisture-near
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263 Forest damage in a changing cli
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265 Future challenges for regional
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267 Linking climate factors and ada
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269 GCMs. In the end of the 21 st c
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271 Climate change impacts on extre
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273 Winter storms with high loss po
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275 The impact of land use change a
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277 6. Analysis of Results (Rain) T
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279 (a) (b) Figure 3. Impact of veg
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281 that cold (Fig. 5). Winter temp
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283 Streamflow in the upper Mississ
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285 Dynamical downscaling of urban
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287 Souma, K., K. Tanaka, E. Nakaki
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289 In April 2000, the fire emissio
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291 Impacts of vegetation on global
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International BALTEX Secretariat Pu
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No. 34: BALTEX Phase II 2003 - 2012
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