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to perform simulations for a wide variety of V mag values. We actually produce parameters V off(offset), P V0 (peak power) and V 1/2 (half-width). Then it is necessary to perform the integralshown above for a wide variety of different wind speed directions, layer ranges (R), rangeoffsets from the pulse-peak (R-R 0 ), radar pulse lengths, and polar diagram parameters, andproduce empirically fitted functions for each of these dependencies. Often polynomial fits,Gaussians and exponentials are suitable fitting-functions. As an example, sample graphs ofthe dependence of the frequency offset and spectral width as a function of (R-R 0 ) were shownin the insets of figs. 8 and 9 of Hocking (1983). Due to lack of space, we cannot specify thedependencies determined in detail, but all of the variables V off , P V0 and V 1/2 depend on θ t (theradar zenithal tilt angle), V perp /V mag and V par /V mag (normalized components of the windparallel and perpendicular to the azimuthal direction of beam tilt), R, R-R 0 , θ 1/2 (the radarbeam half-power half-width), the sub-layer depth, and θ s .Fig. 2. Diagram showing the dependencies of the spectra produced from thin layers as afunction of various atmospheric and radar parameters.The key parameters V off , V 1/2 and P V0 should be parameterized, and stored as computersubroutines. Sometimes such computer subroutines are called “look-up tables”. Then, forany realistic wind profile, the scattering region can be considered to be composed of manysub-layers, each with different wind speeds, as shown in fig. 2. For a VHF radar, a sub-layerdepth of 50 m (less than the normal buoyancy scales for turbulence) might be typical. The“look-up tables” described above can be used to determine appropriate values for V off , V 1/2and P V0 for each sub-layer, and then these can be converted to matching parameters f off , P 0and f 1/2 . Care is required to ensure that an appropriate Jacobian is used in the conversion. Theconversion will be different for each sub-layer, depending on the value of V mag within eachsub-layer. The parameters f off , P 0 and f 1/2 now describe the spectrum as a function of trueDoppler frequency for each sub-layer. Once the parameters P 0 , f off and f 1/2 have been deducedfor each sub-layer, the spectrum can be explicitly calculated as a function of frequency.Then the spectral values from each sub-layer are added together at user-specified frequenciesvarying from some reasonable minimum to a reasonable maximum value, to produce thefinal spectrum. It is quite possible that the resultant spectrum is asymmetric, and largenumbers of numerical experiments have demonstrated that this procedure quite closelyproduces the true spectrum determined from the full integral. Spectral half-power half-widthvalues may now be found by simple search algorithms applied to the final spectrum. Theprocedure properly considers pulse-length dependencies, and anisotropic scatter – factors216
which have not yet been considered in the more simplistic models which have followed theformalism of Hocking (1983). In addition, it is possible to deal with layers that only partiallyfill the radar volume, or are offset from R 0 (producing artificial wind shears, as discussed byHocking (1983), and later by May et al., (1988)).When this “look-up table” is used, computational times decrease by over 100 times and more(relative to performing a full integration). Thus the process, which is fast and accurate, can beused in real-time. The procedure is currently used on-line with the McGill VHF radar(Campos and Hocking, this issue), and the Clovar radar (Hocking 1997). It was also used byHocking (1988) for MF radar measurements, and also by Hocking et al., (1988). As anexample, fig. 4 shows dissipation rates measured during the passage of the remnants ofHurricane Isabel over the McGill radar between 1200 on 19 Sept. and 1200 on 20 Sept.,2003.Fig. 4. Sample energy dissipation rates measured with the McGill VHF radar near Montreal,Canada. Times are UT.References:Campos, E., and W. Hocking, Vortical Motions observed with the new McGill VHF radarand associated dynamical characteristics, this issue.Chu, Y.-H, Beam broadening effect on oblique MST radar Doppler spectrum, J. Atmos.Ocean. Tech., 19, 1955, 2002.Hocking, W.K. On the extraction of atmospheric turbulence parameters from radarbackscatter Doppler spectra -I: theory, J. Atmos. Terr. Phys., 45, 89-102, 1983.Hocking, W.K. Two years of continuous measurements of turbulence parameters in the uppermesosphere and ..., J. Geophys. Res., 93, 2475-2491, 1988.Hocking, W., K. Lawry and D. Neudegg, Radar measurements of atmospheric turbulence...,MAP (Middle Atmosphere Program) Handbook,Scostep Secretariat, 27, 443-446, 1989.Hocking, W.K., System design, signal processing procedures and preliminary results for theCanadian (London, Ontario) VHF Atmospheric Radar, Radio Sci., 32, 687-706, 1997.May, P.T., S. Fukao, T. Tsuda, T. Sato and S. Kato, The effect of thin scattering layers on thedetermination of wind by Doppler radars, Radio Sci., 23, 83-94, 1988Nastrom, G.D., Doppler radar spectral width broadening due to beamwidth and wind shear,Ann. Geophys., 15, 786, 1997.VanZandt, T.E., et al., A dual-beamwidth radar method for measuring atmospheric turbulentkinetic energy density, Geophys. Res. Letts., 29, 10.1029/2001GL014283, 2002.217
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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
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 and 186: 1100-1200 hours. From this plot 6.3
Page 187 and 188: STUDIES ON WINDS AND MOMENTUM FLUXE
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
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Page 197 and 198: 191
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Page 201 and 202: These two last relations are the on
Page 203 and 204: 3.2.1 From v ′2 to ɛ kThe questi
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: Fig.1. Lines of constant radial vel
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
Page 237 and 238: further experimental test of the ST
Page 239 and 240: waves can be observed more clearly
Page 241 and 242: winter and a minimum in summer near
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
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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
Page 467 and 468:
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
Page 489 and 490:
Hysell, David L.EAS/Cornell Univers
Page 491 and 492:
Silva, Robert R.ATRADAustraliarsilv
Page 493 and 494:
AAdachi, A. .......................
Page 495:
TTabary, P. .......................
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