East Asia and Western Pacific METEOROLOGY AND CLIMATE

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151 1. INTRODUCTION In this study, structural features of a squall line, which occurred on 17 May 1987 in IOP-2 over the Taiwan straits, were investigated using the thermodynamic retrieval method of Gal-Chen (1978). Dual-Doppler data collected from the CP-4 and TOGA radars (Fig. 1) at three analysis times were objectively analyzed in the horizontal domain of 45 km by 35 km (see the shaded area in Fig. 1) using a 2.5 km scan radius. There were 10 analysis levels in the vertical ranging from 0.35 to 8.75 km. The grid spacing was 1 km for all three directions. Vertical velocities were calculated from the anelastic continuity equation by integrating downward with variational adjustment. Subsequently, fields of deviation perturbation pressure and temperature were retrieved from the Doppler derived winds using the three momentum equations. These fields were then employed to investigate some kinematic, dynamic and thermodynamic structures of a squall line. The goal is to better understand the structure and internal dynamics of a squall line which produced heavy rain in the Taiwan straits. 2. DATA At 2000 LST 16 May, a small squall line had organized in a north-south direction over the Taiwan straits, and was moving eastward at about 25 to 30 kts. The conventional 10-cm radar located in Kaohsiung (Fig. 1) showed the intensification of a squall line after 2000 LST as depicted in Fig. 2. The northern portion of the squall line moved into the SW lobe of a triple Doppler network, Dual-Doppler data were collected from the CP-4 and TOGA radars after the line entered the coverage area near the 0030 LST 17 May 1987. The data considered in this study centered at 0043 LST. Figure 3 shows the 2000 LST 16 May sounding released at Makung over the Taiwan straits (see Fig. 1). Note that moisture was available in the layers from the surface to the upper troposphere. The sounding exhibited conditional instability. A moist adiabat (dotted line) denotes the ascent of an undiluted parcel from the cloud base. In the absence of mixing with the environment, this air parcel would ascend freely above 200 mb with the maximum temperature excess (* 4 C) near 600 mb. Winds were from the southwest throughout the whole tropor sphere. A low-level jet (LLJ) with a maximum speed near 20 m s occurred in the layer between 3 and 4 km. Chen and Yu (1988) found that extremely heavy rainfall in Japan and China is associated with a LLJ. A composite, vertically smoothed hodograph, based on the Makung soundings released at 14, 17 and 20 LST, is presented in Fig z .4. Storm motion during the analysis times was from 250° at 16.5 m s (see the dashed line in Fig. 4 ). Note that veering occurred in the lower and upper layers, while backing occurred in the middle layer. The strong winds observed in the lower levels near 4 km were associated with a LLJ mentioned previously. Using the environmental soundings of tropical mesoscale cloud lines in GATE, Barnes and Sieckman (1984) found that the environment of the fast-moving line was characterized by strong low-level shear, and the principal component of the shear is perpendicular to the line.
152 25 2200L 16 MAY 0000 L 17 MAY X- , 23 I 19" , 12!' Fig. 1. A TAMEX tripple Doppler Fig. 2. PPI displays revealed by network showing the locations the conventional 10-cm radar of CE-4, TOGA and CAA radars. in Kaohsiung. A black area The shaded box signifies the signifies the radar reflecdomain of interest. tivity > 30 dBZ. / \ x Y / XV/A \V\ \/// /^/ / -. \ / ,«ky \ , \' f 600 X\/ ^ 800 1000 Fig. 4. A wind hodograph showing Fig. 3. The Markung sounding at winds at various heights (km) 2000 LST 16 May. in the prestorm environment.
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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
Page 124 and 125: Figure 6 (a) Time-longitude section
Page 126 and 127: 103 Monsoon cyclones /-~N I Subtrop
Page 128 and 129: 105 INFLUENCE OF VARIATIONS OF THE
Page 130 and 131: surface during the rainy period of
Page 132 and 133: located at the position of the firs
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Page 138: 115 Fig.^57 Characteristics of vari
Page 142 and 143: 119 Some Dynamic Aspects of the Equ
Page 144 and 145: 121 equatorial zonal plane. In this
Page 146 and 147: 123 where N is nondimensional Newto
Page 148 and 149: 125 moisture concentration graduall
Page 150 and 151: 127 boundary layer frictional conve
Page 152 and 153: 129 000 - 20 30 WAVELENGTH (10 3 KM
Page 154 and 155: 131 CHINESE POLAR ORBITING METEOROL
Page 156 and 157: some middle and small receiving sta
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Page 163 and 164: 140 The Mesoscale Monitoring System
Page 165 and 166: 142 The weather radar network is co
Page 167 and 168: 144 where V and L are in centimeter
Page 169 and 170: 146 PRF: 80-2000 Hz Minimum detecta
Page 171 and 172: 148 [UHF Doppler RadaT] ^Pibalk ' Z
Page 173: 150 STRUCTURAL FEATURES OF A SQUALL
Page 177 and 178: 154 0*73 KN 0,73 KM TAMEX IOF2 00*1
Page 179 and 180: 156 4.2 East-west Cross Section The
Page 181 and 182: 158 KM -20 EAST OF TOGA -10 0043 28
Page 183 and 184: 160 Radar Observation of Precipitat
Page 185 and 186: 162 Fig. 2. A triple doppler networ
Page 187 and 188: 164 for this presentation Fig. 5a(0
Page 189 and 190: 166 near the northern tip of Taiwan
Page 191 and 192: 168 In order to understand the inte
Page 193 and 194: 170 REMOTE SENSING OF ATMOSPHERIC C
Page 195 and 196: 172 In the meantime, with the incre
Page 197 and 198: 174 method (scanning frequency) and
Page 199 and 200: 176 For sharp absorption lines, the
Page 201 and 202: 178 [10]* Sun Jinhui, Qiu Jinhuan e
Page 203 and 204: 180 COMPARISION OF RADAR ESTIMATES
Page 205 and 206: 182 of 29 %). The Ra/Rg and the rel
Page 207 and 208: 184 under 1) errors in estimating r
Page 209 and 210: 186 Table 1. Summary of Ra/Rg for t
Page 211 and 212: 188 FIGURE 3. CORRELATION COEFFICIE
Page 213 and 214: 190 DOPPLER WEATHER RADAR OBSERVATI
Page 215 and 216: 192 which are concerned about by th
Page 217 and 218: 194 fly on schedule, take off and l
Page 219 and 220: 196 and minus value. Fig. 4 is the
Page 221 and 222: 198 REFERENCES 1. Donald Turnbull e
Page 223 and 224: 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
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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
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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
Page 519 and 520:
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
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
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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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