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4. SummaryThe high resolution (250s and 300m in time and height) Rayleigh lidar measurementsmade on two representative days during summer and wither is presented in this paper. Thelidar observations revealed significant gravity wave activity over the entire observed heightrange of 30-70 km. The wave activity is seen to be distinctly different from stratosphere tomesosphere. From the high-resolution temperature profiles, revealing waves with verticalwavelength of the order of 5 – 10 km and downward phase descent of 0.2 – 0.4 ms -1 , it isinferred that long periods (~7 hrs) characterize the wave activity at stratospheric heights.These modes with low rate of vertical phase propagation, referred to as quasi-stationarymodes, are found to be similar to that observed over midlatitudes [e.g., Wilson et al., 1990]. Incontrast, the wave activity in the mesosphere is dominated by the relatively shorter periods,covering the observed range of ~16 – 270 min. The gravity wave activity is found to bemaximum during summer and minimum during winter, a behavior much different from that ofmid- and high latitudes where the maximum occurs in winter and minimum in summer.AcknowledgementThe National MST Radar facility (NMRF) is operated by the Department of Spacewith partial support from Council of Scientific & Industrial Research, Government of India.ReferencesAllen, S.J., and R.A.Vincent, Gravity wave activity in the lower atmosphere: Seasonal andlatitudinal variations, J. Geophys. Res., 100, 1327-1350, 1995.Beatty, T.J., C.A. Hostetler, and C.S.Gardner, Lidar observations of gravity waves and theirspectra near the Mesopause and Stratopause at Arecibo, J. Geophys. Res., 49, 472-497, 1992.Chanin, M.L., and A. Hauchecorne, Lidar observation of gravity and tidal waves in thestratosphere and mesosphere, J. Geophys. Res., 86, 9715-9721, 1981.Fritts, D.C., Gravity wave saturation in the middle atmosphere: A review of theory andobservations, Rev. Geophys. Space Phys., 22, 275-308, 1984.Fritts, D.C., and P.K. Rastogi, Convective and dynamical instabilities due to gravity wavemotions in the lower and middle atmosphere: Theory and observations, Radio Sci., 20, 1247-1277, 1985.Fritts, D.C., and T.E. vanZandt, Spectral estimates of gravity wave energy and momentumfluxes, 1. Energy dissipation, acceleration, and constraints, J. Atmos. Sci., 50, 3685-3694, 1993.Gardner, C.S., M.S. Miller, and C.H.Liu, Rayleigh lidar observations of gravity wave activityin the upper stratosphere at Urbana, Illonois, J. Atmos. Sci., 46, 1838-1854, 1989.Gavrilov, N.M., S. Fukao, T. Nakamura., Gravity wave intensity and momentum fluxes in themesosphere over Shigaraki, Japan (35°N ; 136°E) during 1987-1997, Ann. Geophys., 18, 834-843, 2000.Hauchecorne, A., and M.L. Chanin, Density and temperature profiles obtained by lidarbetween 35 and 70 km, Geophys. Res. Lett., 7, 565-568, 1980.Wilson, R., A. Hauchecorne and M.L. Chanin, Gravity waves in the middle atmosphereobserved by Rayleigh lidar, Part 2: Climatology, J. Geophys. Res., 96, 5169-5183, 1990.244
APPLICATION OF THE DUAL-BEAMWIDTH METHOD TO ANARROW BEAM MF RADAR FOR ESTIMATION OF TURBULENTSPECTRAL WIDTHAbstractR. Latteck, W. Singer, N. EnglerLeibniz-Institut für Atmosphärenphysik, Schloss-Str. 6D-18225 Kühlungsborn, GermanySpectral widths observed by narrow beam VHF/UHF Doppler radars can be used toestimate turbulent energy dissipation rates. In case of broader beams, the observed spectralwidths have to be corrected for the influence of beam and shear broadening causedby the background wind field. VanZandt et al. (2002) developed a new dual-beamwidthmethod to estimate the turbulent component of spectral width from MST radar observationswithout additional knowledge of the wind field and tested it successfully for thetroposphere. In summer 2002 a new MF radar was put into operation at Saura on theAndøya island in Norway. The system has high flexibility in antenna beam forming allowingoff-zenith beams with different beam widths. Experiments with different beamwidths have been carried out with the MF radar to test the dual-beam width method atmesospheric altitudes. We compare spectral width estimates from both the single-beamwidth and the dual-beam width method on a case study basis.IntroductionThe spectral width σ 2 obs of an observed radar Doppler signal is related to the velocityvariance due to turbulence σ 2 turb what can be used to estimate turbulent energy dissipationrates. If a relative wide radar beam is used σ 2 obs is also influenced by variances due to theinteraction with the background wind and shear σ 2 beam+shear and of waves σ 2 wave with theradar beam (Hocking, 1983)σobs 2 = σturb 2 + σbeam+shear 2 + σwave 2 (1)σobs 2 = σturb 2 + σcorr 2 (2)which have to be removed from the observed spectral width to get σturb. 2 The standardor traditional single-beamwidth method (1BW) consists of estimating σwave, 2 evaluatingσbeam+shear 2 and substracting σcorr 2 from σobs 2 (VanZandt et al., 2002). This traditionalmethod works well as long as the horizontal wind is small enough to let the correctionterm σcorr 2 be smaller then the total observed spectral width σobs. 2 The dual-beam-widthmethod(2BW) considers that the dominant terms in σbeam+shear 2 are proportional to thebeam width θ 2 (Half-Power-Half-Width) what means that σcorr 2 is also approximatelyproportional to θ 2 .Ifσobs 2 is measured simultaneously in nested volumes with radar beamscharacterized by a narrow beam width θ n and a wide beam width θ w two simultaneousequations for σobs,n 2 and σobs,w 2 can be solved (VanZandt et al., 2002) what results inσturb 2 = θ2 w · σobs,n 2 − θn 2 · σobs,w2 (3)θw 2 − θn2with the advantage, that neither the wind speeds and shears nor the exact pointing angleof the radar beam are required for the correction. The dual-beam width method assumesthat for both beam widths the same fraction of the pulse volume is filled with turbulenceand require the beam widths only.245
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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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Page 201 and 202: These two last relations are the on
Page 203 and 204: 3.2.1 From v ′2 to ɛ kThe questi
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Page 207 and 208: ReferencesAlisse J.-R. and C. Sidi.
Page 209 and 210: Röttger J. and C.H. Liu. Partial r
Page 211 and 212: Specular reflection is negligible f
Page 213 and 214: −0.5C n2 Distribution (PROUST & S
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Page 217 and 218: this latitude in late April). Surfa
Page 219 and 220: Fig. 1. Median (upper) winds and (l
Page 221 and 222: Fig.1. Lines of constant radial vel
Page 223 and 224: which have not yet been considered
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Page 227 and 228: Figure 3: Time-altitude cross-secti
Page 229 and 230: Absorption of cosmic noise is cause
Page 231 and 232: Incoherent scatter spectracompared
Page 233 and 234: variations of spectral widths, refr
Page 235 and 236: Figure 1. Diurnal variation of Turb
Page 237 and 238: further experimental test of the ST
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Page 243 and 244: The main recently assumed mechanism
Page 245 and 246: Figure 2. Statistics of numbers of
Page 247 and 248: LIDAR OBSERVATIONS OF MIDDLE ATMOSP
Page 249: latitudinal dependence of the seaso
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
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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
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Surface winds usually range from 10
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weak (maximum of 5 m s -1 ) and the
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The vertical component from the VTB
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Figure 8 shows the profile of virtu
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2 3D ( , ) ( ) ( ) ˆ ( ) ˆp∆ xm
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presented in Praskovsky et al. (200
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In Fig. 2 a sketch of a mountain le
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In Fig. 8 the lamina is aligned on
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Figure 1: composite day (13 days) o
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virtual sensible heat fluxes ( Wm-2
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3. Characteristics of precipitation
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Fig. 3: Horizontal distribution of
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3. Results and discussionUHF profil
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Figure 4. Monthly variation of slop
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system with two receiving antennae,
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cycle of precipitation. Figure 3(a)
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Histogram of Zonal Velocityh=5.13 K
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5. Summary of results and concludin
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the two nearby major cities, Chenna
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Boundary layer height, km32.521.5(a
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Figure 1:Data from the MST radar at
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spectral processing. In this partic
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3. Results and discussionIn the pre
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4. SummaryAn attempt has been made
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The purpose of this study is to exa
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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
Page 489 and 490:
Hysell, David L.EAS/Cornell Univers
Page 491 and 492:
Silva, Robert R.ATRADAustraliarsilv
Page 493 and 494:
AAdachi, A. .......................
Page 495:
TTabary, P. .......................
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