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Finally, in Figure 3 we show an example of scatter plots comparing Z observed by the2835 MHz profiler versus that from the JWD. These data comprise all the stratiform eventsobserved during the Brazilian TRMM-LBA campaign (about 2 months). Looking at thelower panel, where the difference in observed Z 2835 - Z JWD is shown, we see that there isapparently still some slight bias from clear-air echo at low Z. More importantly, there is aninteresting change in character of the relationship starting about 30 dBZ, wherein Z JWDappears to get progressively larger than Z 2835 as Z gets larger. This effect remains to beexplained, but has caused us to limit the calibration region to Z values between 15 and 30dBZ. The effect has appeared in all of the profiler systems we have tried, though the samedisdrometer, which has been moved from site to site, has been used in all cases.Table 1.Profiler SpecsConclusionAlthough there was not room to demonstrate them all here, we have the followingfindings. A collocated disdrometer is an effective way to calibrate and check S-band andUHF profilers. The calibration is statistical and requires at least hours of data to achieve anadequate and reliable precision. This ability to field calibrate small, moveable wind profilersprovides the opportunity to use such systems as transfer standards to other types of radar orremote sensors.References:Gage, K. S., C. R. Williams, P. E. Johnston, W. L. Ecklund, R. Cifelli, A. Tokay, andD. A. Carter, 2000: Doppler radar profilers as calibration tools for scanning radars. Journalof Applied Meteorology, 39, 2209-2222.Jameson, A. R. and A. B. Kostinski, 2001: What is a raindrop size distribution?Bulletin of the American Meteorological Society, 82, 1169-1177.Joss, J. and A. Pittini, 1991: Real-Time Estimation of the Vertical Profile of RadarReflectivity to Improve the Measurement of Precipitation in an Alpine Region. Meteorologyand Atmospheric Physics, 47, 61-72.Williams, C. R., A. Kruger, K. S. Gage, A. Tokay, R. Cifelli, W. F. Krajewski, and C.Kummerow, 2000: Comparison of simultaneous rain drop size distributions estimated fromtwo surface disdrometers and a UHF profiles. Geophysical Research Letters, 27, 1763-1766.364
TOWARD A MULTISENSOR GROUND BASED REMOTE SENSINGSTATIONCatherine Gaffard 1 , Tim Hewison, John NashMet OfficeMeteorology Building, PO Box 243, Earley Gate, University of Reading, RG6 6BB, UK1. IntroductionFuture UK operations require several sites using ground based remote sensing techniques toprovide an upper air network with better spatial and temporal resolution than currently exists.There is currently a network of 5 wind profilers that cover the UK and winds areoperationally assimilated in our global and mesoscale model. Our goal is to get a continuousmonitoring of the lowest 3-km of the troposphere to improve the humidity field and theboundary layer description for numerical weather prediction (NWP). We investigate how asynergy between different ground based remote sensing instruments, like wind profiler,radiometer cloud radar and lidar ceilometer could meet our user needs. A 12-channelmicrowave radiometer is being trialed and a low cost cloud radar is under development.A wind profiler and a ceilometer are operationally operated at Camborne in the southwest ofEngland. At present only the wind and the cloud base information obtained from theseinstruments are used operationally. As it will be illustrated in this paper more informationabout the vertical structure of temperature and humidity is available in the return signal of thewind profiler and of the ceilometer. The main cause of wind profiler radar returns is due to aBragg scattering by turbulent inhomogeneities in the refractive index. Therefore there is aclose link between the return signal and the gradient of the temperature and the humidityprofile. Some studies (Stankov, 2003,1998) have shown that a wind profiler can be used inassociation with other instruments as RASS, radiometer, GPS, humidity profiles could beretrieved at the vertical resolution of the radar.Three intensive observation periods have been conducted, when radiosondes were launchedhourly. These cover three different situations: development of the convective boundary layer,cloud evolution and clear air situation.2. Development of the Convective Boundary Layer Case StudyFigure 1 shows the time-height evolution of the wind profiler signal to noise ratio (SNR).Superimposed in white circles are the cloud bases detected by the ceilometer, which show alot of broken cloud. The cloud base is in the middle of a wide layer of high wind profilersignal to noise ratio, except for a couple of clouds which are just at the edge of the windprofiler signal. For these clouds, the cloud base appears to be more steady. The altitude rangecovered by the wind profiler with a high SNR increases from 1000 m at 08:00 to itsmaximum (2150 m) at around 11:30. During this period, the vertical distribution of the strongwind profiler SNR’s and cloud bases become more spread. This is likely to be due to1 Corresponding Author:Catherine Gaffard, catherine.gaffard@metoffice.com, phone: +44 118 937831, fax: +44 118 3788791365
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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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very interesting to note the double
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20(a) Convective Region(b) Transiti
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Typhoon LekimaFig. 2 Typhoon Lekima
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Fig. 5 Passage of typhoon Hayan on
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the 50 cm 2 sensor head, enabling t
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22 June 2000 23:22:23 - 23:24:20 at
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the time-height section of a convec
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Thurai, M., T.Iguchi,T. Kozu, J.D.E
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There are two main mechanisms which
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Horel, J.D. and Cornejo-Garrido, A.
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estimating two independent and redu
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RASS THETA (K) RASS v-component (m/
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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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Page 325 and 326: 3. Results and discussionUHF profil
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Page 333 and 334: Histogram of Zonal Velocityh=5.13 K
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Page 339 and 340: Boundary layer height, km32.521.5(a
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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
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Page 351 and 352: Figure1. Three-day average of momen
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Page 359 and 360: The profilers of WINDAS weredesigne
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Page 363 and 364: FIRST RESULTS OF THE BOUNDARY LAYER
Page 365 and 366: Figure 3. Pulse Design Diagram to s
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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
Page 379 and 380: ELECTRONIC DIGITAL BEAMFORMING IMPL
Page 381 and 382: The main element of the unit (figur
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Page 387 and 388: ON THE RADIATION EFFICIENCY OF COCO
Page 389 and 390: Table 2: Experiment #1 results, Tra
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Page 393 and 394: Off-zenith beams towards N, S, E, W
Page 395 and 396: 95ALWIN VHF radar: signal powerdB80
Page 397 and 398: ANTENNA BEAM VERIFICATION USING COS
Page 399 and 400: Figure 2: A 45 MHz reference sky te
Page 401 and 402: AN ATTEMPT TO CALIBRATE THE UHF STR
Page 403 and 404: is at 4.7 km, but in the first 4-ga
Page 405 and 406: QUALITY CONTROL FOR DOPPLER WIND PR
Page 407 and 408: The resulting moments are subjected
Page 409 and 410: SOUSY RADAR AT JICAMARCA: SYSTEM DE
Page 411 and 412: NEControl andcomputer roomCompCoute
Page 413 and 414: THE EQUATORIAL ATMOSPHERE RADAR:SYS
Page 415 and 416: Table 1: Specifications of the EAR
Page 417 and 418: VHF ATMOSPHERIC AND METEOR RADAR IN
Page 419 and 420: 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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