East Asia and Western Pacific METEOROLOGY AND CLIMATE

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505 In this study, the following parameter values are chosen to represent typical atmospheric conditions: f Q = 10~ 4 sec" 1 , 3 = I.G^IO" 11 m"" 1 sec" 1 , R 287 m 3 sec" 3 sec 2 °K I r S « 0.33 m 3 sec" 2 rob" 2 K s = 4 K.J. = {6.5 day)""" , p = (20 day)" T^ = 280°K, which gives £ = 1.22018*10~ 8 m" 1 sec" 1 Following Lorenz (1963) and Yao (1977), we further simplify our model by using a truncated spectral representation for each variable. In a rectangular domain, trigonometric functions are the most convenient expansion functions. The truncated Fourier expansions for all variables are chosen as follows: (KM ~
506 The coefficients Z, T, H, and T are spectral coefficients of the vertically averaged and vertically differenced geopotential, the topography and the radiative equilibrium^temperature, respectively. In the above spectral representations, T is represented by mode Al only. Only one zonal wave number, n=3, is retained in the model and two kinds of meridional truncation m=l and m=l,2,3 are used in this study. In the case m=l, the topography is represented by mode LI with H LI = 250 m. In the case m=l,2,3, the topography is represented by a superposition of LI and L3 modes, with H LI = -3 H L3 = 250 m. 3. MULTIPLE EQUILIBRIA (STEADY SOLUTIONS) With only one meridional mode (m=l), this is the simplest case that includes nonlinear interaction between the mean zonal flow, waves, and topography. With this truncation, the governing equations are reduced to six ordinary differential equations with six dependent variables. By requiring all tendency of the six equations to be zero, we can solve the six nonlinear algebra equations with six unknowns. As we searched for a forcing range of AT = 20°C to 80°C, we found more than one (three) stationary solutions (equilibria) whe AT* is greater than 76°C. Fig. 2 shows the AT vs AT plot for the equilibria states. There are three branches in the region 20°K < AT < 80°K, Branches 1, 2, and 3, which correspond to the high-index equilibrium, intermediate equilibrium and low-index equilibrium, respectively. A linear stability analysis has been performed by perturbing the spectral coefficients of the equilibria in the form of cj>' = cj) e . For Branch 3 all equilibrium states are stable, for Branch 2 all equilibrium states are monotonically unstable (real 0) t and for Branch 1 all equilibrium states are oscillatorily unstable (complex O ). We identify the monotonic instability as the baroclinic version of orographic instability. It can be inferred qualitatively in the AT vs. AT diagram (Fig. 2) . The orographic instability is due to the existence of the resonance that makes a perturbation in AT deviate from its equilibrium state through a change of the eddy heat flux divergence larger than the change of Newtonian heating. Again, unlike the barotropic case, a change in eddy heat flux rather than mountain torque is responsible for this instability. We find that all equilibria are unstable with respect to m=2 perturbations,except for the low-index equilibrium at very low AT , AT < 29°K. To allow eddy momentum flux and possible double jets pattern zonal flows in the model, we have relaxed the spectral truncation to additionally include second and their meridional modes (m—1,2,3) in the model. The thermal forcing is kept the same with only mode Al, while a third mode component is added in the topography spectrum. By choosing H^ = -1/3 H LI , the topography is flattened near the lateral boundaries. There are 18 variables in the system, 6 for mean zonal components and 12 for wave components, with 18 ordinary differential
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UNIVERSITY OF HONG KOHG LlBEAEY
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International Conference on East As
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FOREWORD The International Conferen
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VHI LIST OF PARTICIPANTS IN THE PHO
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45 LIM, Hock National University of
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XIII INTERNATIONAL ORGANIZING COMMI
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XV! The mean heat sources over Asia
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XVIII , Jhe impact of urbanization
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XX The East Asia heavy rainfall num
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THE THERMAL STRUCTURE AND CONVECTIV
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THE COUPLING OF UPPER-LEVEL AND LOW
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Q \ ed atmospheric processes * 2. M
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2) DH Experiment The horizontal flo
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of the orography, establishing a na
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11 a o 12 21 36 4$ 60 fZ Pig.3. Nea
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14 OVERVIB/V CF MEI-YU RESEARCH IN
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16 Fig.l Climatological daily rainf
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18 showed a marked contrast between
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20 3. SWDPTiC ^mLYSIS WD DIA^DSTIC
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22 and Chang (27). It was also foun
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24 triggering mechanisms. In additi
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26 important mechanism for creating
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28 mature convections. Satellite pi
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30 States included 70 scientists an
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1-4 M-H C CO *+-« C CD 4-9 C o •
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34 19.Chen, G.T. J., "A study on sy
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36 complexes: 27-28 May 1981 case",
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38 On Temporal Variations of Low Le
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40 low-level flows of the Asian sum
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42 the northern part of the Pacific
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44 cycle is observed for the amplit
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46 SUMMER (6-85 : 12 2 M979 P:850 M
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Observed Structure and Propagation
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50 southeasterly current in the wes
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40°N 30°N 15°N Equator 90°E 105
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54 The pattern of arrows in Fig. 3
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56 Figure 5. Vertical cross-section
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58 TOE MEAN HEAT SOURCES OVER ASIAN
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60 over tost parts of India, Southe
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62 inctly different types. One is t
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64 60 70 too no 120 00
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Fig.2.The 7-month mean values of (a
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68 A NUMERICAL SIMULATION OF THE ME
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70 Synoptic circulation patterns fo
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72 (iii) The mid-latitude westerlie
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74 and the temperate latitude weste
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76 O 1 - (b) Total I Rainf a" 4 0
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78 LONGITUDE TIME WINOCROS5 SECTION
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A simulation of Lee-Cyclogenesis ov
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82 implemented to the global model
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84 In all three experiments, a deep
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86 References: Ballish, A.B., 1980:
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93 1.2-a I2.S 120. 127,5 US. 11.5 7
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95 2. Climatology of East Asian mon
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97 850 MB WIND (U*. V) S. 0 30N i~^
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99 120 ISO ISO 210 2VJ 770 ISO 180
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Figure 6 (a) Time-longitude section
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103 Monsoon cyclones /-~N I Subtrop
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105 INFLUENCE OF VARIATIONS OF THE
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surface during the rainy period of
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located at the position of the firs
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egion of western Australia. These t
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115 Fig.^57 Characteristics of vari
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119 Some Dynamic Aspects of the Equ
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121 equatorial zonal plane. In this
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123 where N is nondimensional Newto
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125 moisture concentration graduall
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127 boundary layer frictional conve
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129 000 - 20 30 WAVELENGTH (10 3 KM
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131 CHINESE POLAR ORBITING METEOROL
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some middle and small receiving sta
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135 local meteorology units through
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140 The Mesoscale Monitoring System
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142 The weather radar network is co
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144 where V and L are in centimeter
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146 PRF: 80-2000 Hz Minimum detecta
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148 [UHF Doppler RadaT] ^Pibalk ' Z
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150 STRUCTURAL FEATURES OF A SQUALL
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152 25 2200L 16 MAY 0000 L 17 MAY X
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154 0*73 KN 0,73 KM TAMEX IOF2 00*1
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156 4.2 East-west Cross Section The
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158 KM -20 EAST OF TOGA -10 0043 28
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160 Radar Observation of Precipitat
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162 Fig. 2. A triple doppler networ
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164 for this presentation Fig. 5a(0
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166 near the northern tip of Taiwan
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168 In order to understand the inte
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170 REMOTE SENSING OF ATMOSPHERIC C
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172 In the meantime, with the incre
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174 method (scanning frequency) and
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176 For sharp absorption lines, the
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178 [10]* Sun Jinhui, Qiu Jinhuan e
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180 COMPARISION OF RADAR ESTIMATES
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182 of 29 %). The Ra/Rg and the rel
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184 under 1) errors in estimating r
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186 Table 1. Summary of Ra/Rg for t
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188 FIGURE 3. CORRELATION COEFFICIE
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190 DOPPLER WEATHER RADAR OBSERVATI
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192 which are concerned about by th
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194 fly on schedule, take off and l
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196 and minus value. Fig. 4 is the
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198 REFERENCES 1. Donald Turnbull e
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200 evaporation, condensation, wind
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202 control valve which permits amp
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204 Table 1 Rainfall Records of a T
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206 various rainfall intensity shou
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208 c 400-- £ o "5 350 H — A —
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210 IMPACT OF HOURLY S-VISSR SATELL
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212 Fig. 1. Daily 1.200 UTC • 500
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I Fig. 2. GMS-3 IR picture taken at
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216 110E 20 115E 30. 20" X J 4o*N'\
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218 Fig. 7. Provisional best track
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220 PREDICTABILITY OF LOW FREQUENCY
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222 expressions that invoke the Mon
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224 b) A low frequency mode experim
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226 A CLOUD WAVE THEORY AND ITS APP
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228 heating indicating a substantia
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230 If N Fig. I, A schematic diagra
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232 2. A Quasi-Diabatic Geostrophic
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234 X can be q, £ c, v, or T. The
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236 On the basis of the preceding d
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238 west of the maximum cloud cover
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240 NORMAL MODES OF CLIMATOLOGICAL
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242 (1983) pointed out that simulat
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244 reach the top of model atmosphe
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246 is not clear in the tropics. Th
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248 Wang, J.-T., J.-W. Kim and W.L.
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250 (a) 30°N-30°S (January) (b) 3
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252 An Important element of the ear
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254 IOCS I02S 3SN Fig. 1 A general
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256 staion of LID (farmland in the
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258 start from October 1990 and end
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260 The measurements of surface rad
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262 Secular trends in urban tempera
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264 LONGTERM TEMPERATURE TRENDS AT
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266 Using these data sources It has
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268 (3) a nearly static phase where
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270 greater rate of increasing mini
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272 consistent with accepted theory
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274 RECENT APPLICATIONS OF THE PENN
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276 upward motion (Fig. Ib) of air
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278 Stauffer and Warner (1987) used
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280 observed precipitation rates fo
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282 coupled model system show that
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284 Baroclinic Instability of Modif
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286 Eq (2.4) corresponds to the con
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288 conventional Eady waves, except
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290 perturbations in Mode I remains
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292 5: Summary And Remarks Two diff
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294 INFLUENCES OF OROGRAPHY ON FLOW
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296 (13) The next step is to determ
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298 where „ = 1 - R a = - R 2>x c
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300 — -~ 1, thus the above relati
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302 The vertical velocity at the to
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304 THE MIGEOPHYSICS OF A MEI-YU CA
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306 O.Qg-m" 3 , which is probably d
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308 snowflakes aggregation generate
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310 (a) TRP.CK - 2 (1652 0 - 1711 0
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312 1987 6/16 17QSSO U 0.9 C 2 = 1.
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314 2. Heavy Rainfall Upstream of a
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316 accumulated rainfall amount on
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318 Figures 11 and 12 demonstrate t
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320 DEGREE K IT ( M/S ) QC (G/KG) -
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322 270 290 310 330 350 370 POTJEMP
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324 A primitive equation model was
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326 had already been affected by so
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328 I .011 I 1...J/1 l\l l-L-l L I
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330 «'.. Fig. 11 Same as Fig. 9 ex
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332 Mathiar, M. B., 1983: A quasi-L
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334 Long (1985), the maximum occure
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336 February 1979. It clearly indic
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338 Jiang H. M. and Jeng H. N., "Nu
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TEMP.GRAD.(C/100KM3 1979/2/04/OOZ 1
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TKANS.C1R. 9 1979/2/04/OE2 •; J97
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344 however, the sharp decrease in
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346 00 " XD 3 b D 3 aD b dD = [ N.
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348 heights. The median diameter an
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350 going on within the melting lay
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352 TRFICK - I (HIS 0 - H31 0J PR0B
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354 MONTHLY AND SEASONAL FORECASTS
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356 In another experiment, the heat
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358 4. CONCLUSION The forecasting e
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360 TABLE 1. COMPARISONS OF THE COR
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362 Fig. 3. Map of the correlation
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364 THE TELECONNECTION OF EQUATORIA
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366 3-*-j-] dag grid % ^Showing eve
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368 oBE (6) fl(uP) , fl(vP) ... 0(w
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370 the major tidal components over
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372 one meter. Most of the water le
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374 and Technology Advisory Group,
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376 INTRODUCTION In 1%6, Bjerknes,
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378 THE INTERANNUAL VARIABILITIES O
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380 current between 127° E—128°
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382 El Nino and Southern Oscillatio
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384 Fig.5. The ADCP measurements (s
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386 I. Introduction Climate is one
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388 specifically at the modeling an
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390 Even during the warm phase of t
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392 (iv) To investigate the morphol
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394 Change program under IGBP is a
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396 TABLE 1: PROCESSES TO BE STUDIE
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398 w / / / / / / / / /-"V / / Z Fi
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400 CHINA-JAPAN JOINT RESEARCH PROG
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402 eastward. In addition to mainta
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404 Processes of Hicroscale Air-Sea
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406 phase velocity; both ratios, th
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T i l l ! o I • GO 00 J Wind Velo
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410 Concluding Remarks In order to
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412 THE VARIATIONS OF THE SST IN TH
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414 maps, there is an extensive are
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416 Flg.1. Time series of the annua
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418 90 N 90 S|. . . 20E 20E Fig.3c.
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420 ON LABORATORY SIMULATION OF SEA
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422 EXPERIMENT: Only simple and eas
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424 With the ability to simulate co
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426 (5) Meroney, R.N., Cermak, J.E.
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428 Fig. 3 Composite Photograph of
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430 A detailed description of the m
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432 However, the schemes failed to
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434 REFERENCES Anderson, E. and A.
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436 Figure 2 Vertical structure of
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438 36 HOUR FORECAST MEAN SEA LEVEL
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440 al.,1984). In this paper, a gen
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442 where subscript x denotes u, v,
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444 AM AM PO- N3 A/i + N3' and NH--
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446 there is only a minor differenc
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448 Guo X.R.,Yan Z.H.,Zhang Y.L. an
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450 THE EAST ASIA HEAVY RAINFALL NU
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452 (described in section 2) carrie
Page 477 and 478: 454 Fig. . 2. Validation of Tempera
Page 479 and 480: 456 simulate the partly cloudy cond
Page 481 and 482: 458 3.3 Nesting Run with 2 km Grids
Page 483 and 484: 460 REFERENCES Bhumralker, C. M., 1
Page 485 and 486: 462 The Impact of the Termination o
Page 487 and 488: 464 and 45.8 km respectively, which
Page 489 and 490: 466 relative to (P+O/2, they actual
Page 491 and 492: 468 Chang, S. W., 1982: The ore-gra
Page 493 and 494: 470 Table 3. 24-hour forecast error
Page 495 and 496: 472 Initial Position Errors 1983-19
Page 497 and 498: 474 A SPECTRAL MODEL FOR MEDIUM RAN
Page 499 and 500: 476 where I p u = FC-
Page 501 and 502: 478 given. This is treated separate
Page 503 and 504: 480 predicted location is too far t
Page 505 and 506: 482 Fig.2 Distribution of 24h preci
Page 507 and 508: 484 LONG-RANGE FORECASTING OF TAIWA
Page 509 and 510: 486 monsoon in east Asia and for co
Page 511 and 512: 488 unfortunately are not integral
Page 513 and 514: Figure 1. SPECTRAL ANALYSIS FOR MAY
Page 515 and 516: 492 TaUj.g_ji Multiple rnfjross i o
Page 517 and 518: 494 THE NONLINEAR INTERACTION OF IN
Page 519 and 520: 496 Burgers(l948) had put forward a
Page 521 and 522: 498 From Eqs,(8), the necessary con
Page 523 and 524: 500 In order to show quantitatively
Page 525 and 526: 502 Multiple Equilibria Of a Therma
Page 527: 504 For the two-level quasi-geostro
Page 531 and 532: 508 just the stable Branch 7 for st
Page 533 and 534: 510 REFERENCES Bolin, B., 1950: On
Page 535 and 536: 512 STATIONARY SOLUTIONS WITH TOPOG
Page 537 and 538: 514 ANNTTAL CYCLE OF 2TTT Fig. 7 An
Page 539 and 540: 516 CISK modes have narrow axes of
Page 541 and 542: 518 about one to three weeks. Predi
Page 543 and 544: 520 first one. In his work, the lon
Page 545 and 546: 522 The works mentioned are qualita
Page 547 and 548: 524 [12] Wang, S.-W., Adv. in Atmos
Page 549 and 550: 526 processes that give rise to a d
Page 551 and 552: 528 3 Local energetics analysis The
Page 553 and 554: 530 dominant waves of a local mode
Page 555 and 556: 532 slightly longer than the length
Page 557 and 558: 534 tends to induce a westerly jet
Page 559 and 560: 536 TYPHOON FORMATION AND DEVELOPME
Page 561 and 562: 538 influence of the mean wind prof
Page 563 and 564: 540 3. Steady-State Solutions The p
Page 565 and 566: 542 of maximum wind (Fig 7 c). This
Page 567 and 568: 544 (A) b- l.O.(B) b- 0.8.(C) b- 0.
Page 569 and 570: 546 b= 1.0,C= 0.03,0 = 120., T = 50
Page 571 and 572: 548 tropical cyclones. Then, Shapir
Page 573 and 574: 550 fine equation (2) will be used
Page 575 and 576: 552 4) Cumulus vertical flux of hea
Page 577 and 578: 554 Fig. 4 Same as Fig, 1, but for
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556 n=800 bPa and r **1. Now it is
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558 RRFKRRNCF Challa, M., and R. T,
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560 The limited-area forecast syste
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562 Our study is to obtain and anal
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564 coarse grid (Fig. 5). The struc
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566 ACCUMULATED PRECIPITATION Fig.
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569 AUTHOR INDEX ANTHES, Richard A.
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571 LIOU, Chi-Sann LIU, Cho-Teng LI
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