East Asia and Western Pacific METEOROLOGY AND CLIMATE

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The digital radar at RO has been very useful for indicating the occurrence of intense rain and is indispensible for the issuance of landslip and flooding warnings during inclement weather. However, for estimating quantitative rainfall and for producing objective rainfall forecast2] r means of calibrating the radar with raingauges should be used. 185 ACKNOWLEDGEMENT The authors wish to thank Mr. F.C. Lam for supplying programs to extract CAPPI data, Mr. Y.C. Yeung for his help in data processing and Mr. L.K. Yau for supplying software to plot radar/gauge time traces. REFERENCES 1. Austin, P. M. r "Relation between measured radar reflectivity and Surface Rainfall", Mon. Weather Rev., Vol 115, 1053-1071 (1987). 2. Lam, C.Y.,"Digital Radar Data as an Aid in Nowcasting in Hong Kong", Proc. Nowcasting-II Symposium, Norrkoping, Sweden, 3-7 Sept. 1984. 3. Wilson, J, W. and Brandes, E. A., "Radar Measurement of Rainfall - A Summary", Bull. Amer. Meteor. Soc., Vol 6iQ, No. 9, 1048-1058 (1979). 4. Zawadzki, I., Desrochers, C., Torlaschi, E. and Bellon, A., "A Radar-Raingauge Comparison", Preprints, 23rd Conf. on Radar Meteorology, Snowmass, Amer. Meteor. Soc., 121-124 (1986). Notes for the Tables: 1) I indicates that gauges with Ra/Rg outside 2 s.d. of the Ra/Rg.for the storm, have been retained. 2) * denotes cases with significant difference between 1 km and 3 km radar estimated rainfall. 3) Weather is the severest weather reported during the rain case. TS denotes thunderstorms. 4) The maximum intensity (MI) is the average of the 10 largest rate of rainfall detected by the radar over the area of Hong Kong during the rain case. 5) The RO gauge total is the sum of the gauge data in the series of available 5-minute radar/gauge pairs for the Royal Observatory (RD1) during the rain case. It is not identical with the rainfall recorded at the Royal Observatory for the same time period because radar data is not always available.
186 Table 1. Summary of Ra/Rg for the 19 cases —Ra/Rg (3 km) — Time Type(weather) mean s.d. gauges 87040515-0518 trough(TS,hail) .97! .98 19 87040518-0521 trough(TS) .35 .15 19 87040600-0703 trough(TS) .79* .12 20 87041206-1212 cold front(isol TS) .37* .12 21 87041212-1400 cold frbnt(isol TS) .59 .18 21 87050308-0312 cold front(TS) .64 .23 12 87051600-1700 trough(water spout) .92 .23 15 87052200-2300 trough(TS) .49 .19 15 87061900-2000 T.S. Ruth(showers) .12* .06 11 87072200-2306 trough(TS) .57 .19 14 87072712-2900 trough(TS) .53 ,15 17 87072900-3003 trough(TS) .30 .06 15 87081500-1600 T. Betty(isol TS) .23* .08 16 87081600-1714 after T. Betty(TS) .44 .11 14 87082000-2100 T. Cary(TS) .33 .13 10 88052606-2621 trough(TS) .62 .18 9 88062300-2500 trough(TS) .46 .13 16 88071900-1906 T. Warren(TS) .36 .16 10 88071916-2008 T. Warren(TS) .52 .28 16 —Ra/Rg (1 mean s.d. .80! .63 .42 .17 .66 .15 .52 .14 .56 .19 .73 .20 .87 .27 .58 .22 .35 .16 .54 .21 .48 .09 .33 .06 .38 .14 .44 .12 .43 .12 .56 .19 .43 .11 .47 .15 .52 .25 km) — gauges 19 21 20 21 21 12 16 15 14 15 14 15 15 15 9 9 16 9 16 Table 2. Mean correlation coefficient for the 19 .cases. Time 87040515-0518 87040518-0521 87040600-0703 87041206-1212 87041212-1400 87050308-0312 87051600-1700 87052200-2300 87061900-2000 87072200-2306 87072712-2900 87072900-3003 87081500-1600 87081600-1714 87082000-2100 88052606-2621 88062300-2500 88071900-1906 88071916-2008 3 km CAPPI-— mean %s.d . gauges ,24 .35 ,49 .32 .19 108 63 31 75 137 17 19 18 19 20 .50 58 10 .51 39 15 ,38 ,48 ,49 .50 .64 .52 .55 .54 .52 .42 71 48 69 54 17 48 40 54 35 50 13 11 13 16 14 15 12 9 8 15 .53 28 9 .66 20 •16 1 km CAPPI — mean %s,d , gauges ,47 .58 .68 .43 .30 .57 .70 .64 .58 .66 .53 .72 .67 .58 .58 .48 .53 ,57 .76 47 34 19 47 60 54 21 33 45 45 42 13 31 41 43 50 42 23 16 12 19 12 14 15 8 11 10 11 11 11 10 12 10 5 7 10 4 13 MI (mm/h) 172 81 97 63 43 66 102 68 26 57 38 56 35 40 35 50 55 74 81 RO gauge total (mm) 4.5 36.0 136.0 43.0 21.0 31.5 61.5 73.0 42.0 66.5 79.5 139.5 21.5 54.5 38.0 28.5 120,5 70.5 86.0 mean ,46 55 .58 37
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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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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 and 174: 150 STRUCTURAL FEATURES OF A SQUALL
Page 175 and 176: 152 25 2200L 16 MAY 0000 L 17 MAY X
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
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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: 184 under 1) errors in estimating r
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
Page 225 and 226: 202 control valve which permits amp
Page 227 and 228: 204 Table 1 Rainfall Records of a T
Page 229 and 230: 206 various rainfall intensity shou
Page 231 and 232: 208 c 400-- £ o "5 350 H — A —
Page 233 and 234: 210 IMPACT OF HOURLY S-VISSR SATELL
Page 235 and 236: 212 Fig. 1. Daily 1.200 UTC • 500
Page 237 and 238: I Fig. 2. GMS-3 IR picture taken at
Page 239 and 240: 216 110E 20 115E 30. 20" X J 4o*N'\
Page 241 and 242: 218 Fig. 7. Provisional best track
Page 243 and 244: 220 PREDICTABILITY OF LOW FREQUENCY
Page 245 and 246: 222 expressions that invoke the Mon
Page 247 and 248: 224 b) A low frequency mode experim
Page 249 and 250: 226 A CLOUD WAVE THEORY AND ITS APP
Page 251 and 252: 228 heating indicating a substantia
Page 253 and 254: 230 If N Fig. I, A schematic diagra
Page 255 and 256: 232 2. A Quasi-Diabatic Geostrophic
Page 257 and 258: 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
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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
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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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