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WIND PROFILER FOR MONITORING OF MEIYU PRECIPITATIONIN THE DOWNSTREAM OF YANGTZE RIVERK.Krishna Reddy 1 , Biao Geng 1 , Hiroyuki Yamada 1 and Hiroshi Uyeda 1,21Frontier Observational Research System for Global Change, 3173-25 Showa-machiKanazawa-ku, Yokohama, Kanagawa 236-0001, Japan2 Hydrospheric-Atmospheric Research Center, Nagoya University, Furocho, Chikusaku, Nagoya 464-8601,Japan1. IntroductionIn the Yangtze River Valley, the rain period from mid-June to mid-July is widelyknown as Meiyu (or Baiu in Japan, Changma in Korea) or Plum rain (Akiyama, 1989). Theseheavy rainfall systems play a major role not only in the energy and water cycle of the Asianmonsoon regions, but also causes flood disasters in the East Asia region. Elucidating thebehavior of the systems is important for understanding and predicting regional climatechanges, as well as global climate changes (Ninomiya, 2000). For the first time loweratmospheric wind profiler (LAWP) with radio acoustic sounding system (RASS) was used tostudy the three-dimensional wind field associated with mesoscale precipitating cloudsystems. In particular, LAWP can directly measure the vertical wind component within aconvective environment. The objective of this paper is to investigate coherent structures inthe boundary layer and interaction between the boundary layer and clouds observed duringMeiyu seasons.2. Experimental location and data collectionA joint field experiment by the Frontier observational Research System for GlobalChange, Japan and Chinese Academy of Meteorological Sciences (CAMS), China on heavyrainfalls in the downstream of the Yangtze River was conducted during 2001 and 2002.Yangtze RiverDoppler RadarAWSTaihu LakeLAWP AntennaRASS shield322Figure.1 (a) Map showing the topography around experimental site and (b) Lower atmospheric wind profilerwith radio acoustic sounding system, X-band Doppler radar and automatic weather station at Dongshan, ChinaTo examine the detailed three-dimensional structure of the mesoscale convectivesystems (MCS) in the downstream of the Yangtze River [Fig.1 (a)] an observational networkof meteorological instruments were deployed. Three X-band Doppler radars, a bistatic radar
system with two receiving antennae, one lower atmospheric profiler with radio acousticsounding system, and three automatic weather stations (AWS) were deployed for theintensive observational period. However, for the present study, the data collected fromLAWP/RASS and AWS were used. The LAWP/RASS was installed [as shown in Figure1(b)] along with an automatic weather station (AWS), the Institute of Low TemperatureSciences, Hokkaido Universitys’ Doppler radar and micro rain radar in the premises of theDongshan Meteorological Observatory, Jiangsu province, about 80 km west to Shanghai, PRChina. Dongshan (31 o 4′47″ N; 120 o 26′3″ E) site is ideal because of the surroundingvegetation and some rural houses. The site is in the peninsula of the Taihu Lake, which is thelargest in China about 2425 sq km. About 3 km on the west side of the site there are fewhills of about 200 m high. Two intensive observational campaigns were conducted duringMeiyu period between June and July 2001 and 2002. In this presentation we analysed theLAWP/RASS data from 15 June – 15 July during intensive observation period 2001(hereafter, IOP-2001) and 2002 (hereafter, IOP-2002).3. Results and DiscussionThe weather map remains one of the key tools for the study of atmospheric processesand the prediction of the weather. Regional objective analyses from JMA on 24 June 2001 at0020 LST is shown in Figure 2(d). On 24 June 2001, a medium scale disturbance (Meiyufront) was generated near East China Sea and propagated to south of the wind profiler site.Typhoon Chebi (0102), located at South China Sea was traveling towards northward. FromFig.2(d) it could be noticed that the Meiyu front was stationary around the experimental site.The Tropical Cyclone (0102) Chebi was downgraded from Typhoon and became extratropicallow at 24.8 o N 119.4 o E at Taiwan Strait, moved northward. A time-height crosssectionof reflectivity (SNR) obtained from 23 and 24 June 2001 during Meiyu frontal systemand influence of the Typhoon Chebi (0102) are shown in Figure 2(a). Several different typesTaihu Lakeof the vertical structures are evident in this figure during periods of rainfall recorded at thesurface [Fig.2(c)] by the influence of Typhoon and Meiyu frontal system. Likewise, thebright-band (layer of enhanced reflectivity) near 4.5 km reveals a time-varying intensity andsmall fluctuation in height. During the passage of typhoon Chebi, the heavier rain episodesoccurred between 15:30 hrs and 22:30 hrs on the 23 rd June illustrated a mixture of convectionwith stratiform rain. The Doppler vertical velocity field W d [W d = w + W T , where w isvertical air motion and W T is the particle terminal fall speed] in Fig. 2(b) reveals a largelystratiform structure, with primarily – 1 to –2 m/s (downward) velocities characteristic ofsnowfall speeds above the melting region. The LAWP suits for the present study because itcan observe the wind profile preceding to the development of Meiyu precipitation. Vectorsare directed upward for a northward (southerly) component, and towards the right for aneastward (westerly) component. On 23 and 24 June 2001 a mesoscale convective system(MCS) passed over the lower atmospheric wind profiler (LAWP) site. LAWP revealed aneasterly jet stream in the boundary layer bringing a cold air mass from the East China Seaprior to the occurrence of the heavy rainfall about 110 mm within two hours in a limitedarea. The lifting of the unstable air in the vertical column of the atmosphere by the low-levelnortherly inflow and horizontal convergence could aid the rapid development of the MCSand the heavy rainfall. Figure 2(e) demonstrates impressively the response of a threedimensionalboundary-layer wind field of the typhoon and Meiyu frontal mesoscaleconvective system. During the passage of the typhoon (22 and 23 June 2001) thepredominant winds were blowing from easterly or southeasterly and above 1 kmsoutherly/southwesterly winds predominant. Another interesting observation was a lowlevelconvergence on 24 June around 0300 LT during the passage of Meiyu precipitatingclouds system. Surface (AWS) measurements [Fig.2(f)] also show that the low-level flowchanged from northeasterly direction to southwesterly direction.323
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MST10Tenth InternationalWORKSHOPOn
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MST 10 Group PictureMay 15 th , 200
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TENTH INTERNATIONAL WORKSHOP ON TEC
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Table of ContentsPREFACE ..........
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I.2.18 FURTHER OBSERVATIONS OF PMSE
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I.3.27 NEW MST RADAR METHODS FOR ME
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I.4.19 STUDY OF A MESOSCALE LAND-TO
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I.5.502 AN ATTEMPT TO CALIBRATE THE
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PrefaceMST10The Tenth International
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and the local organizing committee,
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The operational aspects and recent
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To improve the understanding of dyn
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Improving MST radar resolution by u
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latitudes, arguing that the former
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Report on Session I.3 “Winds, Wav
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Turbulence.The session then moved i
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Report on Session I.4 “Meteorolog
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Multiple Antenna Profiling Radar (M
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Report on Session II “Novel Persp
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synchronized by GPS and connected v
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The highly positive response of the
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10th International Workshop on Tech
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10th International Workshop on Tech
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Session I.1: Radar scattering proce
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⎡7800 ∂q⎤(3)⎢ 15500q⎥M =
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Figure 2 compares profiles of ω B
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Figure 1: Data from the MST radar a
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Ri =shear2ωB22⎛ ∂u⎞ ⎛ ∂v
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Meridional (deg)1050−5−10Echo P
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Subarray Configuration, Capon Metho
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Fig. 2 PMSE plot (SOUSY Svalbard Ra
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VHF radar interferometry had shown
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turbulence. From Figures 1 and 2, i
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SummaryFrom the aspect sensitivity
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a specific range. In this work, syn
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P C(dB)(a) Echo Power60504030200.70
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most occidental area of South Ameri
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Quegan, 1992). It should be useful
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measurements, is shown in figure 1(
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The present observations thus empha
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RECENT OBSERVATIONS OF E REGION FIE
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measured spectra in order to separa
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drifts at E and F regions heights b
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• Are characterized by type II ec
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The main parameters that could be o
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THE ROLE OF UNSTABLE SPORADIC-E LAY
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(σ H / σ P )E y (where σ H and
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STUDY OF A LOW E-REGION QUASI-PERIO
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100 m/syrFigure 4: Geometry of the
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Where the notations carry same mean
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Where dx/dt and dy/dt are the veloc
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non-negativity of the image is prio
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spectrum corresponding to the backs
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The Artigas and Machu-Picchu Statio
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Arguments against the second altern
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Extension of the Kolmogorov spectru
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volumeESRvolumeSSRSSR SSRESR ESRSSR
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individual particles in a statistic
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Anomalous spectraTalkner [4] studie
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To observe the E region FAI echoes,
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matter daytime or nighttime and are
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two sub-arrays, each sub-array made
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4. SummaryHere we describe a radio
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Figure 1. E-region DPS4 spectra, ri
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effects. It is therefore plausible
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1996 and high in 2002). The electri
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electric fields map along the geoma
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SNR condition is always difficult a
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Figure-4 Power spectrum plots of a
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As we show below, Jicamarca offers
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particularly during daytime counter
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where ˆδ nm = (δ l − δ m )
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PMSE is more easily interpreted as
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ResultsTemperature climatology• s
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Simultaneous PMSE and NLC observati
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ResultsSeasonal variationMSE are no
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Figure 2: MSE parameters as functio
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Session I.3: Winds, waves and turbu
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poor. It was shown that poor perfor
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The use of diffraction pattern simi
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F 13 (ξ x ′) = (1 − cos 2ψ N)
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Figure 3: (a) Baseline length depen
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3. ResultsFigure 1 shows the amplit
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variability.Figure 4 shows the aver
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Figure 1. Period-time amplitude wav
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the 12-h and 24-h periodicities in
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winds and variances at altitudes 70
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similar correlation with larger mag
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of the refraction index are not equ
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Fig. 8. Zonal wind (top) and temper
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STUDIES ON ATMOSPHERIC GRAVITY WAVE
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1100-1200 hours. From this plot 6.3
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STUDIES ON WINDS AND MOMENTUM FLUXE
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3.4 Monthly variation of momentum f
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DEEP PENETRATIVE CONVECTION AND GEN
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ly changes direction with time with
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189
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191
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193
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These two last relations are the on
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3.2.1 From v ′2 to ɛ kThe questi
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5.2 Frequency distributionsSeveral
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ReferencesAlisse J.-R. and C. Sidi.
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Röttger J. and C.H. Liu. Partial r
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Specular reflection is negligible f
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−0.5C n2 Distribution (PROUST & S
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the beamwidth, α is the zenith ang
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this latitude in late April). Surfa
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Fig. 1. Median (upper) winds and (l
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Fig.1. Lines of constant radial vel
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which have not yet been considered
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is calculated from the radiosonde t
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Figure 3: Time-altitude cross-secti
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Absorption of cosmic noise is cause
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Incoherent scatter spectracompared
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variations of spectral widths, refr
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Figure 1. Diurnal variation of Turb
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further experimental test of the ST
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waves can be observed more clearly
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winter and a minimum in summer near
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The main recently assumed mechanism
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Figure 2. Statistics of numbers of
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LIDAR OBSERVATIONS OF MIDDLE ATMOSP
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latitudinal dependence of the seaso
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APPLICATION OF THE DUAL-BEAMWIDTH M
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Figure 2: Mean zonal and meridional
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JLKLLK/ILIL6II/G/II/G/LEODFLK/LO/DD
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The monthly diurnal mean of horizon
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Session I.4: Meteorological Phenome
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Integration of the VHF wind profile
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Figure 1 : Map of the Lago Maggiore
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precipitating clouds, the cyclonic
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Eyewall(a)(b)(c)(d)Fig. 3: Radius-h
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as low as 0.55. The Piura 50-MHz ra
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place features in the profile with
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• Period 1 (June 1-10): SCCs exis
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Sumatera occurs by stratiform cloud
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Page 281 and 282: Typhoon LekimaFig. 2 Typhoon Lekima
Page 283 and 284: Fig. 5 Passage of typhoon Hayan on
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Page 287 and 288: 22 June 2000 23:22:23 - 23:24:20 at
Page 289 and 290: the time-height section of a convec
Page 291 and 292: Thurai, M., T.Iguchi,T. Kozu, J.D.E
Page 293 and 294: There are two main mechanisms which
Page 295 and 296: Horel, J.D. and Cornejo-Garrido, A.
Page 297 and 298: estimating two independent and redu
Page 299 and 300: RASS THETA (K) RASS v-component (m/
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Page 307 and 308: Figure 8 shows the profile of virtu
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Page 311 and 312: presented in Praskovsky et al. (200
Page 313 and 314: In Fig. 2 a sketch of a mountain le
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Page 317 and 318: Figure 1: composite day (13 days) o
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Page 321 and 322: 3. Characteristics of precipitation
Page 323 and 324: Fig. 3: Horizontal distribution of
Page 325 and 326: 3. Results and discussionUHF profil
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Page 333 and 334: Histogram of Zonal Velocityh=5.13 K
Page 335 and 336: 5. Summary of results and concludin
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Page 339 and 340: Boundary layer height, km32.521.5(a
Page 341 and 342: Figure 1:Data from the MST radar at
Page 343 and 344: spectral processing. In this partic
Page 345 and 346: 3. Results and discussionIn the pre
Page 347 and 348: 4. SummaryAn attempt has been made
Page 349 and 350: The purpose of this study is to exa
Page 351 and 352: Figure1. Three-day average of momen
Page 353 and 354: 3. The improved method to estimate
Page 355 and 356: But in case of period until 1800 UT
Page 357 and 358: Session I.5: Operational Aspects an
Page 359 and 360: The profilers of WINDAS weredesigne
Page 361 and 362: NOAA, 1994 : Wind profiler assessme
Page 363 and 364: FIRST RESULTS OF THE BOUNDARY LAYER
Page 365 and 366: Figure 3. Pulse Design Diagram to s
Page 367 and 368: MOVEABLE UHF/S-BAND PROFILER/DISDRO
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Page 371 and 372: TOWARD A MULTISENSOR GROUND BASED R
Page 373 and 374: 3. Cloud Evolution Case StudyOn the
Page 375 and 376: DEVELOPMENT OF A DIGITAL RECEIVER F
Page 377 and 378: Experiment 1 Experiment 2IPP 999Km
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ELECTRONIC DIGITAL BEAMFORMING IMPL
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The main element of the unit (figur
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.ON-LINE ADAPTIVE DC-GROUND-CLUTTER
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esulting in a widening of the bandw
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ON THE RADIATION EFFICIENCY OF COCO
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Table 2: Experiment #1 results, Tra
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A NEW NARROW BEAM MF RADAR AT 3 MHZ
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Off-zenith beams towards N, S, E, W
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95ALWIN VHF radar: signal powerdB80
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ANTENNA BEAM VERIFICATION USING COS
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Figure 2: A 45 MHz reference sky te
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AN ATTEMPT TO CALIBRATE THE UHF STR
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is at 4.7 km, but in the first 4-ga
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QUALITY CONTROL FOR DOPPLER WIND PR
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The resulting moments are subjected
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SOUSY RADAR AT JICAMARCA: SYSTEM DE
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NEControl andcomputer roomCompCoute
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THE EQUATORIAL ATMOSPHERE RADAR:SYS
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Table 1: Specifications of the EAR
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VHF ATMOSPHERIC AND METEOR RADAR IN
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ased upon a geotechnical engineerin
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VORTICAL MOTIONS OBSERVED WITH THE
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interpolation from the original gri
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A NEW MINIRADAR TO INVESTIGATE URBA
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e eliminated to analyze correctly t
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Session PWG 1: System Calibrations
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Session PWG 2: Data Analysis, Valid
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• the time series vectors x(k) of
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Fig. 4: reflectivity of the hydrome
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Session PWG 3: Accuracies and Requi
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Session PWG 4: International Collab
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Session II.E: NOVEL PERSPECTIVES AN
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2 Proposed AlgorithmReceived signal
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N#4E-1-16E1A1#1#2A-1-1C1#3C-1-19Fig
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of conventional DCMP, with which th
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applying the directional constraint
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while for a beam of finite width, t
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In order to make the process more q
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WHAT IS TURBULENCE SEEN BY VHF RADA
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Enhanced resolution applyingpulse s
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Beckmann, Spizichino, 1964Fig. 8 Po
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Fig. 11 Plots of temporal variation
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Fig. 14 Distributions of phase cent
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Hocking, W.K., Radar studies of sma
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THE STRUCTURE FUNCTION-BASED APPROA
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{ Ui( t), Vi( t), Wi( t)} = { Ui ,
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161). Assumption 2H: the instantane
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Only the second order SF are consid
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fluctuations umk( t ) along the bas
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VHF PARASITIC RADAR INTERFEROMETRYF
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• All the costs of transmitter pr
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Figure 2: Example of range-azimuth
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Target Altitude, km1009080706050403
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ReferencesGriffiths, H. D., A. J. G
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Participants ListAvery, James P.Uni
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Hysell, David L.EAS/Cornell Univers
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Silva, Robert R.ATRADAustraliarsilv
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AAdachi, A. .......................
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TTabary, P. .......................
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