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2003). They are related to the evolution of the upstream synoptic wind speed and directionconditions during the event, from west to northwest, in the first part of the event, and north, inthe second part. The progressive descent of the upstream inversion layer height (measured byradiosounding at Lyon), associated with the the upstream mountain elevation and the strongacceleration of the air masses along the Rhône-valley axis when the synoptic wind direction isnorth, are the causes of the passage from a “deep” to “shallow” Mistral situation. Then, thecessation of the Mistral at TLN, several hours before STC, is due to the blocking of this lowlevelflow by the Alps to the north of TLN (maximum upstream elevation around 3000 m),whereas STC still observed air masses directly exiting from the Rhône valley. This resultillustrates the important role played by the upstream orography to determine wether or not agiven site is under the influence of the Mistral.The vertical velocity field is presented here for the first time. Our results are consistentwith our basic knowledge of the Mistral, that is, the cold air masses arriving from the northtoward the Mediterranean sea are globally subsident. This is particularly true in Novemberwhere there is no significant ground heating. The right panels of Fig. 2 clearly show such abehaviour, i.e. quasi-systematic negative vertical velocities in the height-time regionconcerned by the Mistral episode with maximum values between –1 and –1.5 m s -1 aboveSTC and between –1.5 and –2 m s -1 , above TLN. The values have been temporally smoothedusing a 2h-width moving-averaging window in order to remove short period orographicallyinducedwavesFigure 2: Height-time diagrams of the horizontal wind speed (left panels), wind direction(middle panels) and 2h-averaged vertical velocity (right panels), obtained at STC(upper panels) and TLN (bottom panels), during the 6/8 November Mistral episode..Fig. 3 shows STC (top panels) and AIX (bottom panels) UHF-profiler observationsmade during the 21-to-23 June 2001 (ESCOMPTE). The maximum wind speed values arebetween 12 and 15 m s -1 below 1500 m.This event is a typical summer Mistral event, featured by WNW synoptic upstreamconditions (quasi-stationary during the whole event), weaker wind speeds and interactionswith thermal circulations. The left panels of Fig. 3 clearly show that the Mistral blows atlower levels during the nights and is “lifted up” during daytimes, especially the afternoonswhere the ground heating is maximum. Right panels of Fig. 3 show the turbulent dissipationrate ε which reveals the installation of the convective boundary layer at the same periodswhere the Mistral is “lifted up”. Moreover, still for the same periods, the near-surface wind is296
weak (maximum of 5 m s -1 ) and the direction reaches WSW (middle panels of Fig. 3). Thisresult is consistent with the presence of sea-breeze circulations.Figure 3 : Height-time diagrams of the horizontal wind speed (left panels), wind direction(middle panels) and turbulent dissipation rate (right panels), obtained at STC (upperpanels) and AIX (bottom panels), during the 21/23 June Mistral episode.ConclusionsSome mesoscale and seasonal aspects of the Mistral in coastal area have beeninvestigated for the first time thanks to UHF profiler data. In fall, when the ground is cool, theMistral has a synoptically and orographically forced low-level jet structure. The wind speedcan be strong, the depth strongly depends on the upstream conditions and on the observationsites (wind fields observed above two places 90 km apart may be very different) and the airmasses are globally subsident when approaching the sea. In summer, the Mistral winds areweaker and diurnal variations are observed. During daytimes, the installation of convectiveboundary layer, revealed by the turbulent dissipation rate, and the sea-breeze circulations tendto weaken and “lift up” the Mistral. During nighttimes, because of the ground cooling, theMistral recovers its low-level jet structure.ReferencesBougeault, P., P. Binder, A. Buzzi, R. Dirks, R. Houze, J. Kuettner, R.B. Smith, R.Steinacker, and H. Volkert, The MAP Special Observing Period, Bull. Amer. Meteor. Soc.,82, 433-462, 2001.Cros, B., P. Durand, H. Cachier, P. Dobrinski, E. Fréjafon, C. Kottmeier, P.E. Perros, V.H.Peuch, J.L. Ponche, D. Robin, F. Saïd, G. Toupance, and H. Wortham, The ESCOMPTEProgram: An overview, Atmos. Res., in press, 2003.Drobinski, P., O. Reitebuch, A.M. Dabas, P. Delville, C. Werner, A. Delaval, C. Boitel, H.Hermann, E. Nagel, B. Romand, J. Streicher, S. Bastin, J.L. Caccia, P. Durand, and V.Guénard, Characterization of the 28 June 2001 Mistral event during the ESCOMPTE fieldexperiment, 10 th AMS Conf. on Mountain Meteorology, Park City, Utah, USA, 3-15, 2002..Guénard V., P. Drobinski, J.L. Caccia, B. Campistron, and B. Benech, Experimental study ofthe mesoscale dynamics of the Mistral, Bound.-Layer Meteor., submitted, 2003.Jacoby-Koaly S., B. Campistron, S. Bernard, B. Bénech, F. Ardhuin-Girard, J. Dessens, E.Dupont, and B. Carissimo, Turbulent dissipation rate in the boundary layer via UHF windprofiler Doppler spectral width measurements, Bound.-Layer Meteor., 103, 361-389, 2002.Pettré P., On the problem of violent valley wind, J. Atmos. Sci., 39, 542-554, 1982.297
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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
Page 251 and 252: APPLICATION OF THE DUAL-BEAMWIDTH M
Page 253 and 254: Figure 2: Mean zonal and meridional
Page 255 and 256: JLKLLK/ILIL6II/G/II/G/LEODFLK/LO/DD
Page 257 and 258: The monthly diurnal mean of horizon
Page 259 and 260: Session I.4: Meteorological Phenome
Page 261 and 262: Integration of the VHF wind profile
Page 263 and 264: Figure 1 : Map of the Lago Maggiore
Page 265 and 266: precipitating clouds, the cyclonic
Page 267 and 268: Eyewall(a)(b)(c)(d)Fig. 3: Radius-h
Page 269 and 270: as low as 0.55. The Piura 50-MHz ra
Page 271 and 272: place features in the profile with
Page 273 and 274: • Period 1 (June 1-10): SCCs exis
Page 275 and 276: Sumatera occurs by stratiform cloud
Page 277 and 278: very interesting to note the double
Page 279 and 280: 20(a) Convective Region(b) Transiti
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/
Page 301: Surface winds usually range from 10
Page 305 and 306: The vertical component from the VTB
Page 307 and 308: Figure 8 shows the profile of virtu
Page 309 and 310: 2 3D ( , ) ( ) ( ) ˆ ( ) ˆp∆ xm
Page 311 and 312: presented in Praskovsky et al. (200
Page 313 and 314: In Fig. 2 a sketch of a mountain le
Page 315 and 316: In Fig. 8 the lamina is aligned on
Page 317 and 318: Figure 1: composite day (13 days) o
Page 319 and 320: virtual sensible heat fluxes ( Wm-2
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
Page 327 and 328: Figure 4. Monthly variation of slop
Page 329 and 330: system with two receiving antennae,
Page 331 and 332: cycle of precipitation. Figure 3(a)
Page 333 and 334: Histogram of Zonal Velocityh=5.13 K
Page 335 and 336: 5. Summary of results and concludin
Page 337 and 338: the two nearby major cities, Chenna
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
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3. The improved method to estimate
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But in case of period until 1800 UT
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Session I.5: Operational Aspects an
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The profilers of WINDAS weredesigne
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NOAA, 1994 : Wind profiler assessme
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FIRST RESULTS OF THE BOUNDARY LAYER
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Figure 3. Pulse Design Diagram to s
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MOVEABLE UHF/S-BAND PROFILER/DISDRO
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one-minute Z values determined from
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TOWARD A MULTISENSOR GROUND BASED R
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3. Cloud Evolution Case StudyOn the
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DEVELOPMENT OF A DIGITAL RECEIVER F
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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. .......................
Page 495:
TTabary, P. .......................
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