East Asia and Western Pacific METEOROLOGY AND CLIMATE

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289 Figs. 7-8 (for case 2e) show that a stronger stratification aloft reduces the amplitude of 0* in the upper layer considerably. This also reduces the height of the steering level so that c r of 2e is smaller than that of 2a, as discussed in Fig. 3. Overall, the fundamental 7'i'"r r in i 111 i IITTI r-f i i ri/ ri'i i;i i n rrrn TrrvT'i 9. * for 2a with X=1600 km, the height 10. 0* for 2a with X=1600 km. of the domain is 8500 m. 11. d>* for 2e with X=1600 km. 12. 8* for 2e with X=1600 km.
290 perturbations in Mode I remains similar to the original Eady waves. 4> * and 0* for a 2 =1.25*rc (i.e., X, =1600 km) of Mode n are presented in Figs. 9-10 for 2a, and in Fig. 11-12 for 2e. The perturbations are more confined in the lower atmosphere, especially for case 2e. The temperature slightly tilts eastward in the lower layer, atop a transition layer, where it tilts westward drastically. The tilt of 9* is very small in the middle and upper atmosphere. The structures of * and 0* for 2e are similar to the short waves discussed by Nakainura ^1 Bretherton 15,16] argues that the presence of the new unstable modes can be caused by the existence of a gradient of the basic state potential vorticity (i.e, 3Q/3y ^ 0) in the interior of the flow, according to Eq. (2.6). The height of the disturbance may be measured by the Rossby depth of penetration, h « c r /(V/H). h2a ~3 km for 2a, and h2e«2.5 km for 2e. Those heights are comparable to the height of the transition level of 0 * in Figs. 10 and 12. The average a0/3z=2.15 K km' 1 at z « 3 km for 2a; and 90/3z=2.63 K km" 1 at z « 2.5 km for 2e. The effective stratification of 2a is smaller than that of case 2e, but the growth rate of 2e is larger, as shown in Fig. 4. Therefore, the short waves are sensitive to the stratification not only just in the lower atmosphere but also in the upper layer. Comparing perturbations fields of 2a (Figs. 9-10) and 2e (Figs. 11-12), we can see that decrease of I h. The change of w'0' across h is much smaller in 2a than 2e, because motion in 2e is more confined in the lower layer and is able to
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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
Page 261 and 262: 238 west of the maximum cloud cover
Page 263 and 264: 240 NORMAL MODES OF CLIMATOLOGICAL
Page 265 and 266: 242 (1983) pointed out that simulat
Page 267 and 268: 244 reach the top of model atmosphe
Page 269 and 270: 246 is not clear in the tropics. Th
Page 271 and 272: 248 Wang, J.-T., J.-W. Kim and W.L.
Page 273 and 274: 250 (a) 30°N-30°S (January) (b) 3
Page 275 and 276: 252 An Important element of the ear
Page 277 and 278: 254 IOCS I02S 3SN Fig. 1 A general
Page 279 and 280: 256 staion of LID (farmland in the
Page 281 and 282: 258 start from October 1990 and end
Page 283 and 284: 260 The measurements of surface rad
Page 285 and 286: 262 Secular trends in urban tempera
Page 287 and 288: 264 LONGTERM TEMPERATURE TRENDS AT
Page 289 and 290: 266 Using these data sources It has
Page 291 and 292: 268 (3) a nearly static phase where
Page 293 and 294: 270 greater rate of increasing mini
Page 295 and 296: 272 consistent with accepted theory
Page 297 and 298: 274 RECENT APPLICATIONS OF THE PENN
Page 299 and 300: 276 upward motion (Fig. Ib) of air
Page 301 and 302: 278 Stauffer and Warner (1987) used
Page 303 and 304: 280 observed precipitation rates fo
Page 305 and 306: 282 coupled model system show that
Page 307 and 308: 284 Baroclinic Instability of Modif
Page 309 and 310: 286 Eq (2.4) corresponds to the con
Page 311: 288 conventional Eady waves, except
Page 315 and 316: 292 5: Summary And Remarks Two diff
Page 317 and 318: 294 INFLUENCES OF OROGRAPHY ON FLOW
Page 319 and 320: 296 (13) The next step is to determ
Page 321 and 322: 298 where „ = 1 - R a = - R 2>x c
Page 323 and 324: 300 — -~ 1, thus the above relati
Page 325 and 326: 302 The vertical velocity at the to
Page 327 and 328: 304 THE MIGEOPHYSICS OF A MEI-YU CA
Page 329 and 330: 306 O.Qg-m" 3 , which is probably d
Page 331 and 332: 308 snowflakes aggregation generate
Page 333 and 334: 310 (a) TRP.CK - 2 (1652 0 - 1711 0
Page 335 and 336: 312 1987 6/16 17QSSO U 0.9 C 2 = 1.
Page 337 and 338: 314 2. Heavy Rainfall Upstream of a
Page 339 and 340: 316 accumulated rainfall amount on
Page 341 and 342: 318 Figures 11 and 12 demonstrate t
Page 343 and 344: 320 DEGREE K IT ( M/S ) QC (G/KG) -
Page 345 and 346: 322 270 290 310 330 350 370 POTJEMP
Page 347 and 348: 324 A primitive equation model was
Page 349 and 350: 326 had already been affected by so
Page 351 and 352: 328 I .011 I 1...J/1 l\l l-L-l L I
Page 353 and 354: 330 «'.. Fig. 11 Same as Fig. 9 ex
Page 355 and 356: 332 Mathiar, M. B., 1983: A quasi-L
Page 357 and 358: 334 Long (1985), the maximum occure
Page 359 and 360: 336 February 1979. It clearly indic
Page 361 and 362: 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
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454 Fig. . 2. Validation of Tempera
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456 simulate the partly cloudy cond
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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
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464 and 45.8 km respectively, which
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466 relative to (P+O/2, they actual
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468 Chang, S. W., 1982: The ore-gra
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470 Table 3. 24-hour forecast error
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472 Initial Position Errors 1983-19
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474 A SPECTRAL MODEL FOR MEDIUM RAN
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476 where I p u = FC-
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478 given. This is treated separate
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480 predicted location is too far t
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482 Fig.2 Distribution of 24h preci
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484 LONG-RANGE FORECASTING OF TAIWA
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486 monsoon in east Asia and for co
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488 unfortunately are not integral
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Figure 1. SPECTRAL ANALYSIS FOR MAY
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492 TaUj.g_ji Multiple rnfjross i o
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494 THE NONLINEAR INTERACTION OF IN
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496 Burgers(l948) had put forward a
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498 From Eqs,(8), the necessary con
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500 In order to show quantitatively
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502 Multiple Equilibria Of a Therma
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504 For the two-level quasi-geostro
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506 The coefficients Z, T, H, and T
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508 just the stable Branch 7 for st
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510 REFERENCES Bolin, B., 1950: On
Page 535 and 536:
512 STATIONARY SOLUTIONS WITH TOPOG
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514 ANNTTAL CYCLE OF 2TTT Fig. 7 An
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516 CISK modes have narrow axes of
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518 about one to three weeks. Predi
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520 first one. In his work, the lon
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522 The works mentioned are qualita
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524 [12] Wang, S.-W., Adv. in Atmos
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526 processes that give rise to a d
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528 3 Local energetics analysis The
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530 dominant waves of a local mode
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532 slightly longer than the length
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534 tends to induce a westerly jet
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536 TYPHOON FORMATION AND DEVELOPME
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538 influence of the mean wind prof
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540 3. Steady-State Solutions The p
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542 of maximum wind (Fig 7 c). This
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544 (A) b- l.O.(B) b- 0.8.(C) b- 0.
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546 b= 1.0,C= 0.03,0 = 120., T = 50
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548 tropical cyclones. Then, Shapir
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550 fine equation (2) will be used
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552 4) Cumulus vertical flux of hea
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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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East Asia and Western Pacific METEOROLOGY AND CLIMATE

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