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Height (km)Height (km)09-11 April 200120182018201816161614141412121210101088866644422-16-12-8 -4 0 4 8 12 -5 0 5 10 2 -0.2 -0.1 0.0 0.1 0.2Zonal Velocity(m/s) Meridional Velocity(m/s) Vertical Velocity(m/s)26-28 november 200120182018201816161614141412121210101088866644-10 -5 0 5 -5 0 5 10 15 20 -0.15 4 0.00 0.15Zonal Velocity(m/s) Meridional Velocity(m/s) Vertical Velocity(m/s)Height (km)17-19 July 2001201820182018161616141414121212101010888666444-40 -30-20 -10 0 10 20 -8 -4 0 4 8 -0.6-0.3 0.0 0.3 0.6 0.9Zonal Velocity(m/s) Meridional Velocity(m/s) Vertical Velocity(m/s)Height (km)201816141210864-20-15 -10 -5 0 5Zonal Velocity(m/s)22-24 january 200220201818161614141212101088664-9 -6 -3 0 3 6 9 1215 4 -0.2 -0.1 0.0 0.1 0.2Meridional Velocity(m/s) Vertical Velocity(m/s)Figure 1. Mean vertical profiles of zonal, meridional and vertical velocities during (a)09-11 April 2001, (b)17-19 July 2001, (c)16-18 October 2001, (d)22-24 January 2002. Average for the entire 03 days time period ofobservation from 1000-1600 hours(LT) in each day has been taken.Figure 3. Frequency spectra for zonal velocity ontypical day during 18 th July 2001Figure 2. Represents the time series of zonal, meridional and verticalwind components during 06 hour period of observation on a typical dayin different seasons starting at 1000-1600 LT (local time)..180Figure 5. Momentum flux and variance of wind fluctuations determinedfrom the MST radar data during 1000-1600 LT from 18 th July 2001. Forthis total 06 hours of observations were averaged. Dotted line representsmeridional variance and solid line represents zonal variance.Figure 4. Hodograph for 18 th July 2001 from10.2 -20.1 km at 11-12 hours.
STUDIES ON WINDS AND MOMENTUM FLUXES USING UHF RADAROBSERVATIONS OVER GADANKI (13.5 0 N, 79.2 0 E)D. Narayana Rao 1 , B. Vasantha 2 , N.V.P. Kiran Kumar 2 and I.V. Subba Reddy 21. National MST Radar Facility, P.B. No.: 123, Tirupati – 517 502, India2. Department of Physics, Sri Venkateswara University, Tirupati - 517 502, IndiaEmail: profdnrao2001@yahoo.comABSTRACTWind information obtained from UHF radar observations at Gadanki (13.5 0 N,79.2 0 E) are utilized for the present study. These studies are related to ten clear airecho days in each month for the observation period of one year i.e. from April 1999 toMarch 2000. Diurnal, monthly and seasonal variations of horizontal winds andmomentum fluxes are studied. Zonal winds are found to be westward in summer, postmonsoon and winter seasons, eastward in monsoon season. Meridional winds arefound to be northward in summer and southward in post monsoon and monsoonseasons. Zonal and meridional momentum fluxes show upward around noon time insummer and downward in winter seasons.1. IntroductionThese Doppler radar observations have provided detailed three-dimensionalwind measurements which have enabled large advancement in the understanding ofconvective storms, Planetary Boundary Layer (PBL), frontal surfaces and othermeteorological phenomena (Kropfli and Hildebrand, 1980).Several inter comparisons were made between wind profiles of wind profilerand Doppler radar (Weber and Wuertz,1990; Luce et al., 2001; Krishna Reddy et al.,2000) found good agreement. Radar derived three dimensional wind measurementswere made in the optically clear planetary boundary layer by Kropfli and Hildebrand,(1980) and concluded that wind fluctuations are in good agreement with anemometricdata. Kallistratova et al., (2001) have compared turbulent momentum fluxes derivedfrom Sodar and Sonic anemometer measurements and determined turbulent kineticenergy (TKE) from measurements of three wind components by Doppler radar,momentum flux from the density of turbulent kinetic energy. They showed a goodcomparison of the results. Peters and Kirtzel, (1994) have measured momentum fluxin boundary layer and from radar measurements by Kropfli, (1986).2 Data baseThese studies are related to ten clear air echo days in each month for theobservation period of one year. LAWP gives continuous measurement of wind overthe entire diurnal cycle (24 hours). The available data in an hour is averaged torepresent hourly data. So 24-hourly averages are available on all the days. Seasons areclassified as summer (March, April and May), monsoon (June, July, August andSeptember), postmonsoon (October, November and December) and winter (Januaryand February). Diurnal variation of winds and momentum fluxes are representedchoosing a typical day in each season. They are 19 th April 1999 (summer), 11 th July1999 (Monsoon), 24 th November 1999 (Post- monsoon) and 25 th January 2000(Winter). Results and discussion is presented in section 3. Diurnal variation of winds,momentum fluxes in different seasons are presented in section 3.1. Monthly variationof horizontal winds, momentum fluxes, are presented in section 3.2. Summary andresults is presented in section 4.181
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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
Page 135 and 136: electric fields map along the geoma
Page 137 and 138: SNR condition is always difficult a
Page 139 and 140: Figure-4 Power spectrum plots of a
Page 141 and 142: As we show below, Jicamarca offers
Page 143 and 144: particularly during daytime counter
Page 145 and 146: where ˆδ nm = (δ l − δ m )
Page 147 and 148: PMSE is more easily interpreted as
Page 149 and 150: ResultsTemperature climatology• s
Page 151 and 152: Simultaneous PMSE and NLC observati
Page 153 and 154: ResultsSeasonal variationMSE are no
Page 155 and 156: Figure 2: MSE parameters as functio
Page 157 and 158: Session I.3: Winds, waves and turbu
Page 159 and 160: poor. It was shown that poor perfor
Page 161 and 162: The use of diffraction pattern simi
Page 163 and 164: F 13 (ξ x ′) = (1 − cos 2ψ N)
Page 165 and 166: Figure 3: (a) Baseline length depen
Page 167 and 168: 3. ResultsFigure 1 shows the amplit
Page 169 and 170: variability.Figure 4 shows the aver
Page 171 and 172: Figure 1. Period-time amplitude wav
Page 173 and 174: the 12-h and 24-h periodicities in
Page 175 and 176: winds and variances at altitudes 70
Page 177 and 178: similar correlation with larger mag
Page 179 and 180: of the refraction index are not equ
Page 181 and 182: Fig. 8. Zonal wind (top) and temper
Page 183 and 184: STUDIES ON ATMOSPHERIC GRAVITY WAVE
Page 185: 1100-1200 hours. From this plot 6.3
Page 189 and 190: 3.4 Monthly variation of momentum f
Page 191 and 192: DEEP PENETRATIVE CONVECTION AND GEN
Page 193 and 194: ly changes direction with time with
Page 195 and 196: 189
Page 197 and 198: 191
Page 199 and 200: 193
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
Page 205 and 206: 5.2 Frequency distributionsSeveral
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
Page 215 and 216: the beamwidth, α is the zenith ang
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
Page 225 and 226: is calculated from the radiosonde t
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
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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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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 ,
Page 471 and 472:
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
Page 491 and 492:
Silva, Robert R.ATRADAustraliarsilv
Page 493 and 494:
AAdachi, A. .......................
Page 495:
TTabary, P. .......................
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