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adars at the site of the Indian MST radar at Gadanki. The observation showed precipitationstructure seen in both the Indian MST radar and the Lower Atmospheric Wind Profiler(LAWP). Vertical velocity and turbulence structure was shown in addition to reflectivity.J. Röttger made a presentation on behalf of C. Pan, M. Hsu and L. Chung who could notattend the meeting. The observations from the Chung-Li radar on Taiwan showed VHFradar reflectivity and rainfall rate during a Typhoon passage. The third paper was an invitedpaper by Dr. C. Williams and K. Gage. This work was concerned with profiler retrievals ofdrop-size distributions. Dr. Gage presented profiler observations that focussed on thevertical structure of convective and stratiform systems. Precipitation parameters such asreflectivity, rain rate and drop diameter have been retrieved using boundary layer radarsalone. The drop-size retrieval methodology was applied to observations taken over manymonths at Kwajalein. The results were summarized statistically and showed a very differentbehavior for convective precipitation compared to stratiform precipitation. Prof. D. N. Raowith co-authors K. Kumar and V. S. Reddy et al. presented DSD retrievals obtained usingthe collocated VHF and UHF profilers at Gadanki. Christopher Lukas presented work usingan FFT-based deconvolution which seems to have a 10-35% relative error in DSD retrievalwith less error on the larger drop end. The methodology uses an exponential distributionand the results are calibrated with rain gages. Dr. Krishna Reddy with co-authors T. Kozuand Y. Ohno presented climatological studies of DSD obtained from several locations. Dr.T. Shimomai with co-authors T. Kozu, H. Hashiguchi, F. Renggonno and S. Fukaopresented retrievals of drop-size distributions obtain using the EAR in Indonesia. J.Furomoto with co-authors K. Kurimoto and T. Tsuda presented new results on the retrievalof humidity profiles using MU Radar and RASS. Considerable progress was reported onthe ability to retrieve humidity profiles from radar reflectivity and to use GPS precipitablewater as a constraint influencing the choice of sign of the gradient of reflectivity.The third part of Session 1.4 was held on Saturday morning. The session was chaired byDr. K. Gage. The first presentation was made by K. Takahashi who talked about Piura windmeasurements and the relationship between sea breeze circulations and the occurrence ofextreme precipitation events. Most heavy rain events are initiated in the afternoon. Dr. S.Vogt with co-author G. Jaubert presented results of the use of a wind profiler-RASS duringthe MAP campaign. The work concerned the occurrence of Foehn winds and the use of theprofiler equipped with RASS to study the Foehn circulation. Dr. J. Caccia with colleaguesV. Guenard, B. Benech et al. presented the results of another study related to the MAPcampaign. Caccia and colleagues studied the Mistral with a network of UHF wind profilers.The occurrence of the Mistral is related to topography and the presence of an inversion. Theauthors reported a large diurnal variation in the Mistral. Dr. P. Hoffmann with colleaguesD. Peters, A. Serafimovich and Volker Lehmann presented examples of radar observationsof inertia-gravity waves observed over northern Germany. The inertia-gravity waves hadvertical wavelengths of 2-3 km and horizontal wavelengths on the order of 1000km. Theoccurrence of these waves was discussed in relation to jet streams.Mr. Wallace Clark with co-authors A. Adachi and K. Gage et al. presented the results of astudy of a gravity current and solitary wave observed at MRI using a wind profiler and ameteorological tower. The gravity current was initiated as part of nocturnal katabatic flowassociated with the terrain to the west of the MRI profiler and tower. Dr. A. Praskovsky andE. Praskovskya presented a paper on first results of measurements of atmosphericturbulence with spaced antenna profiling radars. The observations were from the NCAR28
Multiple Antenna Profiling Radar (MAPR) and used the novel UCAR-STARS method ofretrieving horizontal velocities and turbulence characteristics observed by MAPR. JürgenRöttger reviewed our current understanding of inclined layers and their implications forvertical velocity measurement. He suggested three scenarios for the tilted layer structureand its relationship to ‘horizontal’ velocities and isentropic surfaces. He tentativelyconcluded that it was likely that horizontal motions follow isentropic surfaces whilescattering layers are not aligned with the isentropic surfaces. Dr. Röttger stressed, however,that more research is needed to substantiate these tentative conclusions.Session 1.4 contained a number of novel results and demonstrated the overall progressbeing made in the meteorological application of profiling radars. In follow-up discussionsissues concerned with assimilation of data into models and vertical velocity measurementwere extensively discussed. Assimilation of data into models is seen to be a critical issuefor the future for radar observations to achieve their full potential utility to themeteorological community. Further research on vertical velocities is needed to understandfully what is being measured especially in complex terrain where isentropic layers can betilted substantially by mountain lee waves. Furthermore there is a need to assess morecompletely the precision of measurements of quantities related to turbulence such as eddydissipation and diffusion.29
Page 1 and 2: MST10Tenth InternationalWORKSHOPOn
Page 3 and 4: MST 10 Group PictureMay 15 th , 200
Page 5 and 6: TENTH INTERNATIONAL WORKSHOP ON TEC
Page 7 and 8: Table of ContentsPREFACE ..........
Page 9 and 10: I.2.18 FURTHER OBSERVATIONS OF PMSE
Page 11 and 12: I.3.27 NEW MST RADAR METHODS FOR ME
Page 13 and 14: I.4.19 STUDY OF A MESOSCALE LAND-TO
Page 15 and 16: I.5.502 AN ATTEMPT TO CALIBRATE THE
Page 17 and 18: PrefaceMST10The Tenth International
Page 19 and 20: and the local organizing committee,
Page 21 and 22: The operational aspects and recent
Page 23 and 24: To improve the understanding of dyn
Page 25 and 26: Improving MST radar resolution by u
Page 27 and 28: latitudes, arguing that the former
Page 29 and 30: Report on Session I.3 “Winds, Wav
Page 31 and 32: Turbulence.The session then moved i
Page 33: Report on Session I.4 “Meteorolog
Page 37 and 38: Report on Session II “Novel Persp
Page 39 and 40: synchronized by GPS and connected v
Page 41 and 42: The highly positive response of the
Page 43 and 44: 10th International Workshop on Tech
Page 45 and 46: 10th International Workshop on Tech
Page 47 and 48: Session I.1: Radar scattering proce
Page 49 and 50: ⎡7800 ∂q⎤(3)⎢ 15500q⎥M =
Page 51 and 52: Figure 2 compares profiles of ω B
Page 53 and 54: Figure 1: Data from the MST radar a
Page 55 and 56: Ri =shear2ωB22⎛ ∂u⎞ ⎛ ∂v
Page 57 and 58: Meridional (deg)1050−5−10Echo P
Page 59 and 60: Subarray Configuration, Capon Metho
Page 61 and 62: Fig. 2 PMSE plot (SOUSY Svalbard Ra
Page 63 and 64: VHF radar interferometry had shown
Page 65 and 66: turbulence. From Figures 1 and 2, i
Page 67 and 68: SummaryFrom the aspect sensitivity
Page 69 and 70: a specific range. In this work, syn
Page 71 and 72: P C(dB)(a) Echo Power60504030200.70
Page 73 and 74: most occidental area of South Ameri
Page 75 and 76: Quegan, 1992). It should be useful
Page 77 and 78: measurements, is shown in figure 1(
Page 79: The present observations thus empha
Page 82 and 83: RECENT OBSERVATIONS OF E REGION FIE
Page 84 and 85:
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
Page 96:
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
Page 103 and 104:
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
Page 109 and 110:
The Artigas and Machu-Picchu Statio
Page 111 and 112:
Arguments against the second altern
Page 113 and 114:
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
Page 129 and 130:
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
Page 161 and 162:
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
Page 195 and 196:
189
Page 197 and 198:
191
Page 199 and 200:
193
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These two last relations are the on
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3.2.1 From v ′2 to ɛ kThe questi
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5.2 Frequency distributionsSeveral
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ReferencesAlisse J.-R. and C. Sidi.
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Röttger J. and C.H. Liu. Partial r
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Specular reflection is negligible f
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−0.5C n2 Distribution (PROUST & S
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the beamwidth, α is the zenith ang
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this latitude in late April). Surfa
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Fig. 1. Median (upper) winds and (l
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Fig.1. Lines of constant radial vel
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which have not yet been considered
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is calculated from the radiosonde t
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Figure 3: Time-altitude cross-secti
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Absorption of cosmic noise is cause
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Incoherent scatter spectracompared
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variations of spectral widths, refr
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Figure 1. Diurnal variation of Turb
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further experimental test of the ST
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waves can be observed more clearly
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winter and a minimum in summer near
Page 243 and 244:
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
Page 259 and 260:
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
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.
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estimating two independent and redu
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RASS THETA (K) RASS v-component (m/
Page 301 and 302:
Surface winds usually range from 10
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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
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2 3D ( , ) ( ) ( ) ˆ ( ) ˆp∆ xm
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presented in Praskovsky et al. (200
Page 313 and 314:
In Fig. 2 a sketch of a mountain le
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In Fig. 8 the lamina is aligned on
Page 317 and 318:
Figure 1: composite day (13 days) o
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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)
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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
Page 367 and 368:
MOVEABLE UHF/S-BAND PROFILER/DISDRO
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one-minute Z values determined from
Page 371 and 372:
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
Page 391 and 392:
A NEW NARROW BEAM MF RADAR AT 3 MHZ
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Off-zenith beams towards N, S, E, W
Page 395 and 396:
95ALWIN VHF radar: signal powerdB80
Page 397 and 398:
ANTENNA BEAM VERIFICATION USING COS
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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
Page 409 and 410:
SOUSY RADAR AT JICAMARCA: SYSTEM DE
Page 411 and 412:
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
Page 423 and 424:
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
Page 449 and 450:
applying the directional constraint
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while for a beam of finite width, t
Page 453 and 454:
In order to make the process more q
Page 455 and 456:
WHAT IS TURBULENCE SEEN BY VHF RADA
Page 457 and 458:
Enhanced resolution applyingpulse s
Page 459 and 460:
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
Page 469 and 470:
{ Ui( t), Vi( t), Wi( t)} = { Ui ,
Page 471 and 472:
161). Assumption 2H: the instantane
Page 473 and 474:
Only the second order SF are consid
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fluctuations umk( t ) along the bas
Page 477 and 478:
VHF PARASITIC RADAR INTERFEROMETRYF
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• All the costs of transmitter pr
Page 481 and 482:
Figure 2: Example of range-azimuth
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Target Altitude, km1009080706050403
Page 485 and 486:
ReferencesGriffiths, H. D., A. J. G
Page 487 and 488:
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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