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show comparison of rain rates at high and low rain rates. At high rain rate some discrepancyis observed and this could be due to time lag between the two instruments or due to the highrain rate Rajopadhyaya et al. (1998) and at low rain rate a comparison is fairly good. Figure 6shows time-height cross section of the retrieved rainfall rate of UHF radar in the high and lowrain rate conditions.Conclusions:Theoretical model spectra of both clear air and precipitation are derived from theobserved spectra. Derived precipitation spectra from UHF radar are in agreement with that ofthe observed spectra. Rain rate and water content estimates from UHF radar spectra anddisdrometer are compared. A fairly good comparison is seen between the two and there is adiscrepancy between the two at high rain rates.References:Beard. K.V., 1976: Terminal velocity and shape of cloud and precipitation drops aloft.J. Atmos. Sci., 23, 851-864.Beard. K.V., 1977; Terminal velocity adjustment for cloud and precipitation drops aloft. J.Atmos. Sci., 34, 1293-1298.Currier, P.E., S.K. Avery, B.B. Balsely, K.S. Gage, and W.L. Ecklund, 1992: combined useof 50 MHz and 915 MHz wind profilers in the estimation of raindrop sizedistributions. Geo-phys.Res. Lett., 19, 1017-1020.Doviak, R.J., and D.S. Zrnic, 1984: Doppler radar and weather observations. Academic Press,458 pp.Gossard, E.E., 1988: Measuring drop-size distributions in cloud with a clear-air-sensingDoppler radar. J. Atmos. Oceanic Technol., 5, 640-649.Kishore, P., Atmospheric studies using Indian MST radar – winds and turbulence parameters,Ph. D. thesis, Sri Venkateswara Univ. Tirupati, India, 1995.Maguire, W.B.,II and S.K. Avery, 1994: Retrieval of raindrop size distributions using twoDoppler wind profilers: Model sensitivity testing. J. Appl. Meteor., 33, 1623-1635.Narayana Rao, T., D. Narayana Rao, K. Mohan and S. Raghavan 2001: Classification oftropical precipitating systems and associated Z-R relationships. J.Geo-phys. Res., 106,17,699-17,771.Rajopadhyaya, D.K., P.T. May and R.A. Vincent, 1993: A general approach to the retrievalof rain drop size distributions from wind profiler Doppler spectra: Modelling results.J. Atmos. Oceanic Technol., 10,710-717.Rajopadhyaya, D.K., P.T. May, R.C. Cifelli, S.K. Avery, C.R. Williams, W.L. Ecklund, andK.S. Gage1998: The effect of vertical air motions on rain rates and median volumediameter determined from combined UHF and VHF wind profiler measurements andcomparisons with rain gauge measurements, J. Atmos. Oceanic Technol., 15, 1306-1319.Rao, P.B., A.R. Jain, P. Kishore, P. Balamuralidhar, S.H. Damle, and G.Viswanathan, 1995:Indian MST radar, 1, system description and sample vector wind measurements in STmode, Radio Sci.,30,1125-1138.Wakasugi ,K., A. Mizutani, M.Matsuo, S.Fukao, and S. Kato. 1986: A direct method forderiving drop-size distribution and vertical air velocities from VHF Doppler radarspectra. J. Atmos. Oceanic Technol., 3,623-629.Williams, C.R., W.L. Ecklund, and K.S. Gage, 1995: Classification of precipitating clouds inthe tropics using 916-MHz wind profilers, J. Atmos. Oceanic Technol., 12, 996-1012.280
22 June 2000 23:22:23 - 23:24:20 at 1.8 kmNormalized Doppler Spectrum1.00.80.60.40.20.0Observed SpectrumDerived SpectraN0 = 12828 lambda = 2.63gamma = 1.1-9 -8 -7 -6 -5 -4 -3Vertical Velocity (m/s)Figure 2: Derived Spectra Versus Observed Spectra8 07 0R a in ra te (m m /h r)6 0Rain Rate (mm/hr)5 04 03 02 01 0022:00 23:00 00:00 01:00 02:00 03:00 04:00 05:00 06:00Figure 1: (a) SNR in dB (b) Vertical Velocity (m/s) (c) Spectral width (m/s) Taken from LAWP and (d) Rain rate from Disdrometer5022-23 June 20003.022-23 June 2000 at 1.8 km40302010LAWPDisdrometerLiquid Water content (gm/m 3 )2.52.01.51.00.5DisdrometerLAWP022:00 23:00 00:00 01:00 02:00 03:00 04:00 05:00 06:00Time (LT)Figure 3a : Comparison plot of time series of retrieved rain rate(mm/hr) from LAWP at 1.8 km and Disdrometer on groundobserved on during 22 –23 June 20000.022:00 23:00 00:00 01:00 02:00 03:00 04:00 05:00 06:00Time (LT)Figure 3a : Comparison plot of time series of retrieved Liquid watercontent (gm/m 3 ) from LAWP at 1.8 km and Disdrometer on groundobserved on during 22 –23 June 2000504022-23 June 2000LAWPDisdrometerHigh rain rate2022-23 June 2000Low Rain Rate (mm/hr)LAWPDisdrometer15301020510023:00 23:30 00:00Time (LT)Figure 4: Time series of retrieved rainfall rates from LAWP andin comparison with that of the Disdrometer at the time of high rain rate002:00 03:00 04:00 05:00 06:00Time (LT)Figure 5: Time series of retrieved rainfall rates from LAWP andin comparison with that of the Disdrometer at the time of low rain rate3.002.001.001.51.00.50.0LTFigure 6: Time series of water content during the period of22 – 23 june 2000281
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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
Page 235 and 236: Figure 1. Diurnal variation of Turb
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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 and 250: latitudinal dependence of the seaso
Page 251 and 252: APPLICATION OF THE DUAL-BEAMWIDTH M
Page 253 and 254: Figure 2: Mean zonal and meridional
Page 255 and 256: JLKLLK/ILIL6II/G/II/G/LEODFLK/LO/DD
Page 257 and 258: The monthly diurnal mean of horizon
Page 259 and 260: Session I.4: Meteorological Phenome
Page 261 and 262: Integration of the VHF wind profile
Page 263 and 264: Figure 1 : Map of the Lago Maggiore
Page 265 and 266: precipitating clouds, the cyclonic
Page 267 and 268: Eyewall(a)(b)(c)(d)Fig. 3: Radius-h
Page 269 and 270: as low as 0.55. The Piura 50-MHz ra
Page 271 and 272: place features in the profile with
Page 273 and 274: • Period 1 (June 1-10): SCCs exis
Page 275 and 276: Sumatera occurs by stratiform cloud
Page 277 and 278: very interesting to note the double
Page 279 and 280: 20(a) Convective Region(b) Transiti
Page 281 and 282: Typhoon LekimaFig. 2 Typhoon Lekima
Page 283 and 284: Fig. 5 Passage of typhoon Hayan on
Page 285: the 50 cm 2 sensor head, enabling t
Page 289 and 290: the time-height section of a convec
Page 291 and 292: Thurai, M., T.Iguchi,T. Kozu, J.D.E
Page 293 and 294: There are two main mechanisms which
Page 295 and 296: Horel, J.D. and Cornejo-Garrido, A.
Page 297 and 298: estimating two independent and redu
Page 299 and 300: RASS THETA (K) RASS v-component (m/
Page 301 and 302: Surface winds usually range from 10
Page 303 and 304: weak (maximum of 5 m s -1 ) and the
Page 305 and 306: The vertical component from the VTB
Page 307 and 308: Figure 8 shows the profile of virtu
Page 309 and 310: 2 3D ( , ) ( ) ( ) ˆ ( ) ˆp∆ xm
Page 311 and 312: presented in Praskovsky et al. (200
Page 313 and 314: In Fig. 2 a sketch of a mountain le
Page 315 and 316: In Fig. 8 the lamina is aligned on
Page 317 and 318: Figure 1: composite day (13 days) o
Page 319 and 320: virtual sensible heat fluxes ( Wm-2
Page 321 and 322: 3. Characteristics of precipitation
Page 323 and 324: Fig. 3: Horizontal distribution of
Page 325 and 326: 3. Results and discussionUHF profil
Page 327 and 328: Figure 4. Monthly variation of slop
Page 329 and 330: system with two receiving antennae,
Page 331 and 332: cycle of precipitation. Figure 3(a)
Page 333 and 334: Histogram of Zonal Velocityh=5.13 K
Page 335 and 336: 5. Summary of results and concludin
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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
Page 467 and 468:
THE STRUCTURE FUNCTION-BASED APPROA
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{ Ui( t), Vi( t), Wi( t)} = { Ui ,
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161). Assumption 2H: the instantane
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Only the second order SF are consid
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fluctuations umk( t ) along the bas
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VHF PARASITIC RADAR INTERFEROMETRYF
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• All the costs of transmitter pr
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Figure 2: Example of range-azimuth
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Target Altitude, km1009080706050403
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ReferencesGriffiths, H. D., A. J. G
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Participants ListAvery, James P.Uni
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Hysell, David L.EAS/Cornell Univers
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Silva, Robert R.ATRADAustraliarsilv
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AAdachi, A. .......................
Page 495:
TTabary, P. .......................
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