East Asia and Western Pacific METEOROLOGY AND CLIMATE

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411 REFERENCES Haimbach, S. P. and Jin Wu, "Directional slope distributions of winddisturbed water surface", Radio Sci., 21, 73-79 (1986). Papadimitrakis, Y. A., Y.-H. L. Hsu and Jin Wu, "Thermal stability effects on the structure of the velocity field above the sea surface", J. Geophys. Res. 92, 8277-8292 (1987). Wu, Jin, "Laboratory studies of wind-wave interaction", J. Fluid Mech. 34, 91-112 (1968). Wu, Jin, "Wind-induced drift currents", J. Fluid Mech. £8, 49-70 (1975). Wu, Jin, "Wind—stress coefficient over sea surface near neutral conditions - A revisit", J. Phys. Oceanogr. 10, 727-740 (1980). Wu, Jin, "Wind-stress coefficients over sea surface from breeze to hurricane", J. Geophys. Res. .87, 9704-9706 (1982). Wu, Jin, "Viscous sublayer below wind-disturbed water surface", J. Phys. Oceanogr. 14, 138-144 (1984). Wu, Jin, "Parameterization of wind-stress coefficients over the sea surface", J, Geophys. Res. £0, 9069-9072 (1985a). Wu, Jin, "On the cool skin of the ocean", Bound-Layer Meteorol. 31, 203-207 (1985b). Wu, Jin, "Stability parameters and wind-stress coefficients under various stability conditions", J. Atmos. Oceanic Tech. 1, 333-339 (1986). Wu, Jin, "Momentum flux from wind to aqueous flows at various wind velocities and fetches", J. Phys. Oceanogr. 18, 140-144 (1988). Wu, Jin, "Dependence of microwave sea returns on wind-friction velocity under varied atmospheric stability condition 11 , I.E.E.E. J. Oceanic Eng. 14, 254-258, (1989a). Wu, Jin, "Suppression of oceanic ripples by surfactant - Spectral effects deduced from sun-glitter, wave-staff and microwave measurement", J. Phys. Oceanogr. 19, 238-245 (1989b).
412 THE VARIATIONS OF THE SST IN THE EASTERN AND WESTERN TROPICAL PACIFIC AND THEIR RELATIONSHIP WITH THOSE IN THE WORLD OCEAN Pan Yi-Hang (NRCMEF/SOA,China) Oort Abraham H. (GFDL/NOAA, USA) and Richardson William (NOS/NOAA, USA) ABSTRACT The seasonal change of the connections between the SST in the EEP with those in the world ocean are given by 12 correlation maps of the 12 calendar months for the period of 1950-1979. The standard deviation map calculated from these 12 correlation maps has shown that the areas with larger values also located in the western Pacific but mainly in the tropical regions of south-western Pacific and south-eastern Indian oceans. Discussions about the seasonal change of the SST in the EEP as well as those in the world ocean will be given. I. INTRODUCTION In previous papers, the high correlation between the SST in the eastern equatorial Pacific (EEP) with those in the world oceans has been shown by the similarities of the spatial distribution between the 11 correlation maps for 11 decades of 1870-1979 [ Pan and Oort 1989]. The independence of the SST in the western equatorial Pacific (WEP) from those in the EEP has been shown by the standard deviation map of the 11 correlation maps [Pan and et al 1989], In this paper, we'll further investigate how the connections between SST in the EEP with those in the world ocean change with the seasons. II. DATA BASE The data base for this study is Comprehensive Ocean- Atmosphere Data Set (GOADS.) , the most extensive surface marine data set in existence today. These data were observed mainly from the international ships over the world ocean containing various parameters as sea surface temperature (SST), surface air temperature (SAT) and et al. Under a joint project in the United State, they were collected for the period of 1854 to 1979 and edited monthly into 2°*2° boxes by ERL, CIRE, NCDC/NOAA and NCAR [Woodruff etal 1987], Then; the global monthly fields of SST, as weil Q as other parameters were objectively analyzed onto a 1*1 grid at GFDL/NOAA by using Levitus scheme [Lev!tus 1982].
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UNIVERSITY OF HONG KOHG LlBEAEY
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International Conference on East As
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FOREWORD The International Conferen
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VHI LIST OF PARTICIPANTS IN THE PHO
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45 LIM, Hock National University of
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XIII INTERNATIONAL ORGANIZING COMMI
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XV! The mean heat sources over Asia
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XVIII , Jhe impact of urbanization
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XX The East Asia heavy rainfall num
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THE THERMAL STRUCTURE AND CONVECTIV
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THE COUPLING OF UPPER-LEVEL AND LOW
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Q \ ed atmospheric processes * 2. M
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2) DH Experiment The horizontal flo
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of the orography, establishing a na
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11 a o 12 21 36 4$ 60 fZ Pig.3. Nea
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14 OVERVIB/V CF MEI-YU RESEARCH IN
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16 Fig.l Climatological daily rainf
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18 showed a marked contrast between
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20 3. SWDPTiC ^mLYSIS WD DIA^DSTIC
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22 and Chang (27). It was also foun
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24 triggering mechanisms. In additi
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26 important mechanism for creating
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28 mature convections. Satellite pi
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30 States included 70 scientists an
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1-4 M-H C CO *+-« C CD 4-9 C o •
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34 19.Chen, G.T. J., "A study on sy
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36 complexes: 27-28 May 1981 case",
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38 On Temporal Variations of Low Le
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40 low-level flows of the Asian sum
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42 the northern part of the Pacific
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44 cycle is observed for the amplit
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46 SUMMER (6-85 : 12 2 M979 P:850 M
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Observed Structure and Propagation
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50 southeasterly current in the wes
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40°N 30°N 15°N Equator 90°E 105
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54 The pattern of arrows in Fig. 3
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56 Figure 5. Vertical cross-section
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58 TOE MEAN HEAT SOURCES OVER ASIAN
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60 over tost parts of India, Southe
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62 inctly different types. One is t
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64 60 70 too no 120 00
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Fig.2.The 7-month mean values of (a
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68 A NUMERICAL SIMULATION OF THE ME
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70 Synoptic circulation patterns fo
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72 (iii) The mid-latitude westerlie
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74 and the temperate latitude weste
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76 O 1 - (b) Total I Rainf a" 4 0
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78 LONGITUDE TIME WINOCROS5 SECTION
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A simulation of Lee-Cyclogenesis ov
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82 implemented to the global model
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84 In all three experiments, a deep
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86 References: Ballish, A.B., 1980:
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93 1.2-a I2.S 120. 127,5 US. 11.5 7
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95 2. Climatology of East Asian mon
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97 850 MB WIND (U*. V) S. 0 30N i~^
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99 120 ISO ISO 210 2VJ 770 ISO 180
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Figure 6 (a) Time-longitude section
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103 Monsoon cyclones /-~N I Subtrop
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105 INFLUENCE OF VARIATIONS OF THE
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surface during the rainy period of
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located at the position of the firs
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egion of western Australia. These t
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115 Fig.^57 Characteristics of vari
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119 Some Dynamic Aspects of the Equ
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121 equatorial zonal plane. In this
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123 where N is nondimensional Newto
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125 moisture concentration graduall
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127 boundary layer frictional conve
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129 000 - 20 30 WAVELENGTH (10 3 KM
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131 CHINESE POLAR ORBITING METEOROL
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some middle and small receiving sta
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135 local meteorology units through
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140 The Mesoscale Monitoring System
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142 The weather radar network is co
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144 where V and L are in centimeter
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146 PRF: 80-2000 Hz Minimum detecta
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148 [UHF Doppler RadaT] ^Pibalk ' Z
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150 STRUCTURAL FEATURES OF A SQUALL
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152 25 2200L 16 MAY 0000 L 17 MAY X
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154 0*73 KN 0,73 KM TAMEX IOF2 00*1
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156 4.2 East-west Cross Section The
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158 KM -20 EAST OF TOGA -10 0043 28
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160 Radar Observation of Precipitat
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162 Fig. 2. A triple doppler networ
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164 for this presentation Fig. 5a(0
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166 near the northern tip of Taiwan
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168 In order to understand the inte
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170 REMOTE SENSING OF ATMOSPHERIC C
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172 In the meantime, with the incre
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174 method (scanning frequency) and
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176 For sharp absorption lines, the
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178 [10]* Sun Jinhui, Qiu Jinhuan e
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180 COMPARISION OF RADAR ESTIMATES
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182 of 29 %). The Ra/Rg and the rel
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184 under 1) errors in estimating r
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186 Table 1. Summary of Ra/Rg for t
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188 FIGURE 3. CORRELATION COEFFICIE
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190 DOPPLER WEATHER RADAR OBSERVATI
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192 which are concerned about by th
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194 fly on schedule, take off and l
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196 and minus value. Fig. 4 is the
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198 REFERENCES 1. Donald Turnbull e
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200 evaporation, condensation, wind
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202 control valve which permits amp
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204 Table 1 Rainfall Records of a T
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206 various rainfall intensity shou
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208 c 400-- £ o "5 350 H — A —
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210 IMPACT OF HOURLY S-VISSR SATELL
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212 Fig. 1. Daily 1.200 UTC • 500
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I Fig. 2. GMS-3 IR picture taken at
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216 110E 20 115E 30. 20" X J 4o*N'\
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218 Fig. 7. Provisional best track
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220 PREDICTABILITY OF LOW FREQUENCY
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222 expressions that invoke the Mon
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224 b) A low frequency mode experim
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226 A CLOUD WAVE THEORY AND ITS APP
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228 heating indicating a substantia
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230 If N Fig. I, A schematic diagra
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232 2. A Quasi-Diabatic Geostrophic
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234 X can be q, £ c, v, or T. The
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236 On the basis of the preceding d
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238 west of the maximum cloud cover
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240 NORMAL MODES OF CLIMATOLOGICAL
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242 (1983) pointed out that simulat
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244 reach the top of model atmosphe
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246 is not clear in the tropics. Th
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248 Wang, J.-T., J.-W. Kim and W.L.
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250 (a) 30°N-30°S (January) (b) 3
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252 An Important element of the ear
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254 IOCS I02S 3SN Fig. 1 A general
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256 staion of LID (farmland in the
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258 start from October 1990 and end
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260 The measurements of surface rad
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262 Secular trends in urban tempera
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264 LONGTERM TEMPERATURE TRENDS AT
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266 Using these data sources It has
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268 (3) a nearly static phase where
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270 greater rate of increasing mini
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272 consistent with accepted theory
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274 RECENT APPLICATIONS OF THE PENN
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276 upward motion (Fig. Ib) of air
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278 Stauffer and Warner (1987) used
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280 observed precipitation rates fo
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282 coupled model system show that
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284 Baroclinic Instability of Modif
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286 Eq (2.4) corresponds to the con
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288 conventional Eady waves, except
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290 perturbations in Mode I remains
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292 5: Summary And Remarks Two diff
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294 INFLUENCES OF OROGRAPHY ON FLOW
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296 (13) The next step is to determ
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298 where „ = 1 - R a = - R 2>x c
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300 — -~ 1, thus the above relati
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302 The vertical velocity at the to
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304 THE MIGEOPHYSICS OF A MEI-YU CA
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306 O.Qg-m" 3 , which is probably d
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308 snowflakes aggregation generate
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310 (a) TRP.CK - 2 (1652 0 - 1711 0
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312 1987 6/16 17QSSO U 0.9 C 2 = 1.
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314 2. Heavy Rainfall Upstream of a
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316 accumulated rainfall amount on
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318 Figures 11 and 12 demonstrate t
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320 DEGREE K IT ( M/S ) QC (G/KG) -
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322 270 290 310 330 350 370 POTJEMP
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324 A primitive equation model was
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326 had already been affected by so
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328 I .011 I 1...J/1 l\l l-L-l L I
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330 «'.. Fig. 11 Same as Fig. 9 ex
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332 Mathiar, M. B., 1983: A quasi-L
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334 Long (1985), the maximum occure
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336 February 1979. It clearly indic
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338 Jiang H. M. and Jeng H. N., "Nu
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TEMP.GRAD.(C/100KM3 1979/2/04/OOZ 1
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TKANS.C1R. 9 1979/2/04/OE2 •; J97
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344 however, the sharp decrease in
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346 00 " XD 3 b D 3 aD b dD = [ N.
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348 heights. The median diameter an
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350 going on within the melting lay
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352 TRFICK - I (HIS 0 - H31 0J PR0B
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354 MONTHLY AND SEASONAL FORECASTS
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356 In another experiment, the heat
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358 4. CONCLUSION The forecasting e
Page 383 and 384: 360 TABLE 1. COMPARISONS OF THE COR
Page 385 and 386: 362 Fig. 3. Map of the correlation
Page 387 and 388: 364 THE TELECONNECTION OF EQUATORIA
Page 389 and 390: 366 3-*-j-] dag grid % ^Showing eve
Page 391 and 392: 368 oBE (6) fl(uP) , fl(vP) ... 0(w
Page 393 and 394: 370 the major tidal components over
Page 395 and 396: 372 one meter. Most of the water le
Page 397 and 398: 374 and Technology Advisory Group,
Page 399 and 400: 376 INTRODUCTION In 1%6, Bjerknes,
Page 401 and 402: 378 THE INTERANNUAL VARIABILITIES O
Page 403 and 404: 380 current between 127° E—128°
Page 405 and 406: 382 El Nino and Southern Oscillatio
Page 407 and 408: 384 Fig.5. The ADCP measurements (s
Page 409 and 410: 386 I. Introduction Climate is one
Page 411 and 412: 388 specifically at the modeling an
Page 413 and 414: 390 Even during the warm phase of t
Page 415 and 416: 392 (iv) To investigate the morphol
Page 417 and 418: 394 Change program under IGBP is a
Page 419 and 420: 396 TABLE 1: PROCESSES TO BE STUDIE
Page 421 and 422: 398 w / / / / / / / / /-"V / / Z Fi
Page 423 and 424: 400 CHINA-JAPAN JOINT RESEARCH PROG
Page 425 and 426: 402 eastward. In addition to mainta
Page 427 and 428: 404 Processes of Hicroscale Air-Sea
Page 429 and 430: 406 phase velocity; both ratios, th
Page 431 and 432: T i l l ! o I • GO 00 J Wind Velo
Page 433: 410 Concluding Remarks In order to
Page 437 and 438: 414 maps, there is an extensive are
Page 439 and 440: 416 Flg.1. Time series of the annua
Page 441 and 442: 418 90 N 90 S|. . . 20E 20E Fig.3c.
Page 443 and 444: 420 ON LABORATORY SIMULATION OF SEA
Page 445 and 446: 422 EXPERIMENT: Only simple and eas
Page 447 and 448: 424 With the ability to simulate co
Page 449 and 450: 426 (5) Meroney, R.N., Cermak, J.E.
Page 451 and 452: 428 Fig. 3 Composite Photograph of
Page 453 and 454: 430 A detailed description of the m
Page 455 and 456: 432 However, the schemes failed to
Page 457 and 458: 434 REFERENCES Anderson, E. and A.
Page 459 and 460: 436 Figure 2 Vertical structure of
Page 461 and 462: 438 36 HOUR FORECAST MEAN SEA LEVEL
Page 463 and 464: 440 al.,1984). In this paper, a gen
Page 465 and 466: 442 where subscript x denotes u, v,
Page 467 and 468: 444 AM AM PO- N3 A/i + N3' and NH--
Page 469 and 470: 446 there is only a minor differenc
Page 471 and 472: 448 Guo X.R.,Yan Z.H.,Zhang Y.L. an
Page 473 and 474: 450 THE EAST ASIA HEAVY RAINFALL NU
Page 475 and 476: 452 (described in section 2) carrie
Page 477 and 478: 454 Fig. . 2. Validation of Tempera
Page 479 and 480: 456 simulate the partly cloudy cond
Page 481 and 482: 458 3.3 Nesting Run with 2 km Grids
Page 483 and 484: 460 REFERENCES Bhumralker, C. M., 1
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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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