East Asia and Western Pacific METEOROLOGY AND CLIMATE

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11 a o 12 21 36 4$ 60 fZ Pig.3. Near-surface mean V component in m/s (a) <strong>and</strong> temperature in °C (b) between 110-120°B during the integration. 20 V Pig.-4. The 120°B meridional circulation at the 24 hr (a) <strong>and</strong> 48 hr integration (b')j (c) is the difference in vertical speed W,g - W^.* Speed is magnified by a factor of 1,000*
Page 2 and 3: UNIVERSITY OF HONG KOHG LlBEAEY
Page 5 and 6: International Conference on East As
Page 7 and 8: FOREWORD The International Conferen
Page 10 and 11: VHI LIST OF PARTICIPANTS IN THE PHO
Page 12 and 13: 45 LIM, Hock National University of
Page 15: XIII INTERNATIONAL ORGANIZING COMMI
Page 18 and 19: XV! The mean heat sources over Asia
Page 20 and 21: XVIII , Jhe impact of urbanization
Page 22 and 23: XX The East Asia heavy rainfall num
Page 24 and 25: THE THERMAL STRUCTURE AND CONVECTIV
Page 26 and 27: THE COUPLING OF UPPER-LEVEL AND LOW
Page 28 and 29: Q \ ed atmospheric processes * 2. M
Page 30 and 31: 2) DH Experiment The horizontal flo
Page 32 and 33: of the orography, establishing a na
Page 36 and 37: 13 Pig.7* Difference in mean vertic
Page 38 and 39: l.INIRCDUCTICN Climatological data
Page 40 and 41: the forecast capability of the Cent
Page 42 and 43: A marked interannual variation exis
Page 44 and 45: Diagnosis using the balanced o> equ
Page 46 and 47: 23 Fig.4 Distribution of the 326 ca
Page 48 and 49: Wu et al.(82) analyzed 43 cases of
Page 50 and 51: (2,75,79). Over southern China, geo
Page 52 and 53: 29 Fig.5 Distribution of the mesolo
Page 54 and 55: 31 9. CCNCLIDIN3 REMARKS The Mei-Yu
Page 56 and 57: for the growth of nocturnal inversi
Page 58 and 59: 34.Qien, G.T. J., and C.P. Pu, "A c
Page 60 and 61: 68.Liu, K.Y. , "On the heavy rainfa
Page 62 and 63: 39 .0 heating which follows the mov
Page 64 and 65: 41 to the pre-onset level by the en
Page 66 and 67: 43 5.625 N and 15 N (region Bl) and
Page 68 and 69: 45 REFERENCES ^Krishnamurti, T. N.,
Page 70 and 71: 47 s s : SUBTROP. H. CIR. C850M81
Page 72 and 73: 49 taken during the Global Atmosphe
Page 74 and 75: 51 105°£ ISO'E 165°E 30°N 15 8
Page 76 and 77: Scale: 8 °ld 40°N 30°N 15°N Equ
Page 78 and 79: 40°N 30°N 15°N Equator 90°E 105
Page 80 and 81: 57 gence. This interpretation is su
Page 82 and 83: 59 exists discrepancy among differe
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61 The heating over the South China
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63 the deep tropospheric heating ov
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65 . 3 Fig.l. The monthly mean valu
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Fig.6. Time sections of the areal m
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69 WIND AND MOISTURE FIELDS DURING
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71 recorded on the 27th. The period
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73 cross-sections for specific humi
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75 (vi) It will be very useful and
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77 Figure 2 Streamline Analyses (a)
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79 N uo 35 - 30 - 25 - 20 - IS - 10
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81 appreciable intensity throughout
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83 center over the Yun Gui area. Th
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85 (C) With the reduction of the te
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92 10-.. 10-c S1.S S. B2.S M. IBS.
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94 SEASONAL AND INTRASEASONAL VARIA
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96 However, not all subseasonal sca
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98 waves. Fig. 3 adopted from Murak
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100 Indian Ocean and the western Pa
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102 the development of an equatoria
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104 of these clusters may develop i
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106 I . INTRODUCTION The structure
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108 But, as discussed in the next s
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110 cell extended northward to 30 N
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112 References Bourke, W., McAvaney
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^ - ^^KiKS^;--^Sxy^^ . ^ &^>sx^>^.-
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120 The model results also demonstr
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122 The diabatic heating rate Q inc
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124 MODE SELECTION (WL=200QQ KM) MO
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126 (a) OEOPOTEHTIflL FRED (A] VEKT
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128 CQMPRRISON OF GROWTH RflTE KELV
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130 from the dynamic effect of the
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132 Altitude: Inclination: Period:
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134 Local enhanced cloud image Clou
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139 APPLYING TROPOPAUSE DATA OBSERV
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The main objectives of the Program
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143 system, method of assimilation
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145 Some radiosonde data were used
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147 [13 [2] [3] [43 [5] [6] [73 [8]
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149 0 1 2 3 4 o T(°K) FLq. 7 The R
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151 1. INTRODUCTION In this study,
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153 3. METHODOLOGY The data analysi
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155 0*73 KM TAMEX IOP2 00*31 a P »
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157 • cooling to a minimum from t
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159 6. ACKNOWLEDGMENTS The authors
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161 seasons sometimes brought great
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163 carefully analyzed. In Fig.3 th
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165 Fig. 6. (a) The 850 mb map of 0
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167 i: Fig.10. The CAA radar reflec
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169 convergence. Consequently a str
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171 Atmospheric optical remote sens
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Lambert reflector, there is no need
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175 occurs and the average is 0.^1.
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In order to futher broaden applicat
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[21]* Lu Daren, "Lidar Equation Tak
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time to derive the radar estimated
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time interval of 60 minutes, the av
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The digital radar at RO has been ve
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187 FIGURE 1. LOCATION OF RADAR AND
Page 212 and 213:
iU 9 FIGURE 5. REGRESSION RELATION
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were mainly focused on predicting f
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193 following two kinds: (a) Macrob
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195 Case 1: Squall line Fig. 1 is t
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197 radar's data makes the weather
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799 Revival of the Tipping-bucket R
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201 rainfall, (2) Donnelly ' introd
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203 at Holt, Missori is just barely
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205 Table 2 Rainfall Intensity and
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207 valve micro adjustment valve wa
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9 10 11 12 - 25 - _ n A . _ _ _ _
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211 In the final section, the paper
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213 2.2 Observation From Satellite
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215 To ascertain the activity of th
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217 the west-northwest and swept ac
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was found that instead of slowing d
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221 1. OBSERVATIONAL ASPECTS Observ
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223 and i) They receive a substanti
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225 factor for the rapid collapse o
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227 clouds. These clouds trap the I
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229 W/m 2 . It can be seen that the
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231 Fig. 3. The vertical distributi
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233 equatorial region, the meridion
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235 Using a stable leap-frog scheme
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237 the form d& BS. —£ „ _ n
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239 Knutson, T. R. , K. M. Weickman
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241 A Study On The Radiative Balanc
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243 The net downward solar radiatio
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245 space. This effect is the green
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247 are downward. REFERENCES Arakaw
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249 data from ERBE 31 / 18.4 Fig. 3
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251 INTRODUCTION TO HEIHE BASIN FEI
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crop growth, and desert) and climat
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Rainfall station Well for measuring
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over desert area and its possible e
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discontinously in addition to the m
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261 THE IMPACT OF URBANIZATION ON C
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263 TABLE 2. Longterm Temperatures
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265 TABLE 3. Trends in 10 Year Runn
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267 The change in estimated buildin
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269 TABLE 4. Commonly Hypothesized
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271 an effort to minimize the impac
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273 detailed study of changes in th
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0: O O o S E S 1 - I • £ o ° £
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277 2100 GMT 9 MAY 5 104 J03 IO2 10
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279 It is interesting to note that
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281 climatology of the MM4 precipit
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283 Kuo, Y.-H., D.O. Gill and L. Ch
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285 has been investigated by Eady 6
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287 with the classical Eady waves,
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289 Figs. 7-8 (for case 2e) show th
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291 generate more positive kinetic
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293 6] Eady, E. T., 1949: Long wave
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295 But, for wind and geopotential
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297 dary layer in z-coordinate to a
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299 As R -*0> 0=1, U T = u , V T ~
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301 Cb) CO Fig. la shows the orogra
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2 y -f -5 * b* The numerical result
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305 expense of smaller droplets and
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307 low value of 0.4g-irT . The ver
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309 Parrish, J. ^ L. , and A. J. He
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31 1987 6/16 165310 T= -1.7 C Z = 5
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ON DYNAMICAL STUDIES OF ORO GRAPHIC
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315 lateral boundaries. The model i
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317 air sounding, over Panchiao (al
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319 Fig.l Satellite imagery for May
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321 -ISO -50 X-AXIS C KM Fig,7 The
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323 Numerical Simulations of topogr
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325 The physical processes of the o
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327 Fig. 3 The east-west cross sect
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329 0500 LST the next morning, the
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331 (Walker and Rowntree, 1977). Mo
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Study on the Frontal Cyclone System
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Fig.9 indicates the ageostrophic co
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337 £ * ,- (6) dp dy where u g is
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339 100 110 120 130 Fig.3 The synop
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•= 1979/2/04/002 VORTICITY KE-S/S
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343 The Microphysics of a Mei-Yu Ca
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345 1. Introduction Observational r
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347 where V(x) = terminal fallspeed
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349 3.2 Results with Figs. 1 height
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351 Srivastava, E.G., 1978: Paramet
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353 TRRCK - 1 (1115 Q - 1131 QJ PR0
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355 filtered from model because it
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357 The dispersion relationship is
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359 REFERENCE Chao Jiping and Ji Zh
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361 Pig. 1. Anomalous fields of the
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363 Fig. a. Ac the coupling coeffic
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365 A THREE-DIMENSIONAL MODEL OF TH
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367 HYDRODYNAMIC MODELING The hydro
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369 grid, and time level respective
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Model verification with only astron
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Rank DESIGN TYPHOON SURGE HEIGHT NE
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INTERAiWAL VARIABILITIES OF THE WES
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10° N), the strength index is the
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warm water of the upper WEPO west o
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the NWPO and the data obtained from
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383 UO V E ISO' 160 170' 18CT 0 15U
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385 Large Scale Air-Sea Interaction
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387 expands, more and more interact
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389 On ENSO time scales, the pertur
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I. The principal processes responsi
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determine their influence on SST va
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395 References Hsiung, J., 1985: Es
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397 Modeling Piiot Studies Enhanced
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399 THE RELATIONSHIP BETWEEN CURREN
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401 2. THE PROGRAM The objectives o
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403 INFLUENCE OF MICROSCALE AIR-SEA
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405 The results shown In Fig. 1 are
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407 laboratory, momentum flux to wa
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some of the problems, which are bac
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411 REFERENCES Haimbach, S. P. and
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413 The climatology of global SST f
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415 Reference Berlage H.P., "The So
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417 90 N IE' 120' ' 'iio' ' ' ' '12
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Fig.4. Map of the standard deviatio
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421 the rugged coastline terrain. A
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423 The experiment was repeated man
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425 CONCLUSIONS: The use of wind-tu
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427 80 60 U mm/s. 40 * 20 0:02 0.04
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429 THE IMPLEMENTATION AND OPERATIO
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437 42 Physical Processes The physi
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433 time cross-section at two grid-
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435 55 70 75 80 85 90 95 100 105 11
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437 Nanling Figure 4 Topography (TG
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439 BMC LIMITED AREA MODEL: OPERATI
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1 - 00 (P S V -j mV- — JQ.4-6 m w
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443 and caused severe flood. Local
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445 forecast. Based on a nested ver
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447 Fig.5. 24-hour forecasts of RT
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449 THE OPERATIONAL GLOBAL FORECAST
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451 Numerical Simulation of Mesosca
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453 closure model (1974). Radiation
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455 prone to boundary contamination
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457 RMS errors for RO is relatively
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459 Comparison of the surface tempe
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461 AN OVERVIEW OF PRESENT TYPHOON
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; 463 and intensity estimation. How
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465 a. 24-hour forecast errors The
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467 compared with previous years. S
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469 Table 1. Initial position error
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471 Table 5. 48-hour forecast error
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473 48-hour Forecast Errors Rel. to
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4/5 tegration scheme basically foll
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477 '' / » where 1 d . ..... wher
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ainy season of Yangtze valley (bai-
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Fig. 1 ECMWF -FGGE analysis of 500
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483 40} Fig.4 Daily position of the
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485 THE ROYAL OBSERVATORY LONG RANG
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487 (2) Based on possible relations
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489 CONCLUSIONS Seasonal rainfall f
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491 (verifying against the actual M
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YEAR 1975 1976 1977 1978 1979 1980
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495 computational trajectories are
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497 Substituting Eq. (5) into Eqs.
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499 These curves divide the plane (
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501 REFERENCES (1] .Fua,D. ,Chimona
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503 1. INTRODUCTION The earth topog
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505 In this study, the following pa
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507 equations. The 18 ordinary diff
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509 To investigate the statistical
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511 0 ^^S08%#g!%J!J#^ a), T, Q 3 Ap
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FREQUENCY DISTRIBUTION OF 30 DAY RU
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515 EFFECTS OF VERTICAL WIND-SHEAR
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517 ANALOGOUS RHYTHM PHENOMENON OF
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519 layers of the earth's crust) sh
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521 where r 4j is the correlation c
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the equations and so on. Then perfo
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525 An Inquiry into the Nature of R
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527 (1) - 2F 0 ( + %,0) + JCF.9)) +
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529 4.a Dependence of the instabiii
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531 4.b Properties of the unstable
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the jet core. The maximum value is
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535 Frederiksen. J., and R. C. Bell
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537 DYNAMICS OF VORTEX MOTION ON TR
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In Fiorino and Elsberry (1989), the
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541 vortex. Solutions obtained by p
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543 the present linear model, the s
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545 Figure 3, Steady-state asymmetr
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547 EFFECT OF THERMAL AND DYNAMIC F
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549 where b=g(T-Tr)/Tr buoyance for
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from the center of cyclone. Tn addi
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553 typhoon, indi rating the primar
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555 the center at 200 hPa and the m
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557 vertical turbulent flux of mome
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559 RECENT RESULTS IN LIMITED-AREA
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561 PEL scheme consists of a simila
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563 divergence, vorticity and gener
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565 Fig. 1. Observations and 24 hou
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567 62. S 56.5 -70.0 -60.0 58.5 or
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LIN,Y.J. Structural features of a s
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572 WANG, Bin WANG, Jough-Tai WU, J
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East Asia and Western Pacific METEOROLOGY AND CLIMATE

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