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1823. Results and discussion3.1 Diurnal variation of horizontal windsFigure 1 (a) shows height- time contour of single day observations of zonalwinds in different seasons in the altitude region of 0.6 km to 3.3 km. During summer,zonal winds are eastward (westerlies) up to an altitude of 1.0 km and prevail up to1000 hours LT and then changed to westward (easterlies) over the entire altituderegion and then increasing with height. During monsoon season below 2 km altitude,eastward winds of ~ 10 ms -1 are found starting from 0100 hours LT and grow towardsthe day until 1300 hours LT (noon-time). Strong westward winds are found from alower altitude starting from 0000 hours LT to 1200 hours LT of that day, from thenonwards there is a sudden decrease in the magnitude of wind to a value of~5ms -1 . The dominant winds are found to be westward during summer, post- monsoonand winter, whereas eastward in monsoon season.3.2 Diurnal variation of momentum fluxVertical flux of horizontal momentum is calculated using the method given byVincent and Reid, (1983). Figure 2(a) shows diurnal variation of vertical flux of zonalmomentum observed on typical days in different seasons. During summer season,downward flux of westward momentum is showing a maximum negative value of~ 7 m 2 s -2 at around 1000 hours LT and at 1100 hours LT at an altitude of 0.6 km and1.2 km. During monsoon season, at an altitude of 0.9 km, a maximum value ofdownward flux of westward momentum of ~ 22 m 2 s -2 is observed at around 1200hours LT and then decreasing. During post-monsoon, downward flux of westwardmomentum of 5 m 2 s -2 at around 0300 hours LT and 2000 hours LT at an altitude of0.6 km and 1.5 km is observed. During winter season, the downward flux of westwardmomentum of 6 m 2 s -2 around 1400 hours LT at an altitude of 0.6 km is observed.Figure 2(b) shows vertical fluxes of meridional momentum in differentseasons at four altitude regions. During summer season, vertical fluxes are low atearly hours of the day and then increase negatively with a maximum downward fluxof southward momentum of 10 m 2 s -2 at around 1100 hours LT at an altitude region of0.6 km and then decreasing towards the night time. Above this altitude a slightly lowvalue of 9m 2 s -2 is observed around 1200 hours LT at an altitude of 0.9 km. Duringmonsoon season, vertical fluxes are increasing up to 0.9 km with a maximumdownward flux of southward moment um of 13m 2 s -2 at around 1800 hours LT. Duringthe post- monsoon season fluxes are very much low, slight downward flux ofsouthward momentum of ~1.5 m 2 s -2 is observed around 1200 hours LT at an altitudeof 0.9 km. During winter season, at 0.6 km altitude region, a variation of 7 m 2 s -2 to 9m 2 s -2 in between local time of 0200 hours LT to 1300 hours LT is observed.3.3 Monthly variation of horizontal windsFigures 3 (a) and 3 (b) show height-time contour diagram of monthly averagedclear air days of zonal and meridional winds for a period of one year (April 1999 toMarch 2000). From the figure it is clear that zonal winds are eastward with amaximum of ~10 ms -1 in the months of May to September. After September there is achange in the direction from eastward to westward with a maximum of 5 ms -1 in themonths of October to January. From figure 3 (b) meridional winds are northward upto an altitude of 1.5 km in the month of June. Above this altitude there is a slightchange in the direction from northward to southward. Southward winds are observedover the entire altitude region from the months of July to January with a maximum of6 ms -1 in the months of post-monsoon season.
3.4 Monthly variation of momentum fluxFigures 4 (a) and 4 (b) show monthly variation of vertical flux of zonal andmeridional momentum averaged over ten days from the afternoon hours (1200-1400LT) in a month for a period of one year. From the month of April, flux isdecreasing with time and show maximum downward flux of westward momentum ofvalue ~2.0 m 2 s -2 at an altitude of 0.6 km in the month of July. From July it increasesto August with altitude. From the month of August it increases with altitude, but inthe downward direction. Maximum downward flux of westward momentum isobserved in the month of July and upward flux of eastward momentum of 0.5m 2 s -2 inthe month of April. Figure 4(b) shows maximum downward flux of southwardmomentum of ~1.0 m 2 s -2 in the months of July, August and November.4. Summary and conclusionsDiurnal and seasonal variation of horizontal winds, momentum fluxes arestudied in different seasons using typical clear air days. Seasonal variations arestudied using ten day clear air day averages in each month for a period of one year.Zonal winds are found to be westward in summer, post- monsoon and winter andeastward in monsoon season. Meridional winds are found to be northward in summerand southward in post- monsoon and winter seasons. Diurnal variation of vertical fluxof zonal and meridional momentum indicates maximum downward fluxes in monsoonseason. From the monthly mean values, zonal winds show eastward in pre- monsoonand monsoon seasons and westward in post-monsoon and winter seasons. Momentumfluxes around noon time indicate upward fluxes in summer and downward fluxes inwinter seasons.183
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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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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
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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
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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 and 186: 1100-1200 hours. From this plot 6.3
Page 187: STUDIES ON WINDS AND MOMENTUM FLUXE
Page 191 and 192: DEEP PENETRATIVE CONVECTION AND GEN
Page 193 and 194: ly changes direction with time with
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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
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
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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
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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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 ,
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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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