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monsoon, monsoon, post monsoon and winter. The momentum flux for short - period motionsduring 16-18 October 2000 shows direction towards north for meridional momentum flux and eastward direction for zonal momentum flux. For longer-period motions meridional momentum flux istowards north and zonal momentum flux is towards east except in the altitude range of 11-15 km forall the frequency bands. Especially in the lower stratosphere, both long and short-period motions aretowards north and east ward directions. During 09-11 April 2001 zonal momentum flux is towardswestward in the troposphere and lower stratosphere except in the altitude range of ~ 15-16.5 km forboth short and long-period motions (figure not shown). Meridional momentum flux is towardssouthward in the troposphere and lower stratosphere for both short and long-period motions. During17-19 July 2001 zonal momentum flux of short and long-period motions is towards westward,meridional momentum flux is towards northward in the altitude range of ~13-16.7km for both shortand long-period motions(figure not shown). During 22-24 January 2002 zonal momentum flux ofshort and long - period motions are towards east in the altitude range of 11-19 km, meridionalmomentum fluxes are towards south in the altitude range of ~11-19km for both short and longperiodmotions (figure not shown).ConclusionsThe excitation source of the short period gravity waves was suggested to be located nearthe peak of the mean zonal wind. The vertical flux of zonal momentum for waves with periods of 2-24 hours showed westward bias in the 14-17 km. while the zonal flux showed no significantseasonal cycle in the middle troposphere implying that the upward propagating gravity waves in thelower stratosphere mostly travelled westward relative to the background wind. The long periodgravity waves which caused these wind fluctuations were generated in the lower troposphere, theobserved results suggest that the horizontal propagation of gravity waves is azimuthally isotropicnear the wave source and the eastward travelling waves seem to be filtered out during their upwardpropagation, which might result in the observed westward bias of momentum flux. The overallresults suggest that, due to their persistent southward direction of propagation, long-period wavesmake a contribution to the momentum flux in the lower stratosphere which is comparable to that ofshort-period waves.AcknowledgementsThe Authors are thankful to National MST Radar Facility (NMRF), Gadanki for providing MST Radar dataduring the campaign period and UGC-SVU center for MST Radar Applications, S. V. University, Tirupati for providingnecessary facilities for carrying out the studies. One of the authors (I. V. Subba Reddy) is thankful to Advanced Centrefor Atmospheric Sciences and CSIR for providing Junior Research Fellowship and Senior Research Fellowshiprespectively.ReferencesChang, J.L., S. K. Avery, A. C. Riddle, First results of tropospheric gravity wave momentum flux measurements overChristmas Island, Radio Sci., Vol. 32, No. 2, 727-748, 1997.Fritts, D. C., T. Tsuda, T. E. Vanzandt, S. A. Smith, T. Sato, S. Fukao, S. Kato, Studies of velocity fluctuations in thelower atmosphere using the MU radar. Part II. Momentum fluxes and energy densities, J. Atmos. Sci., 47, 51-66,1990.Fukao, S., T. Sato, T. Tsuda, S. Kato, M. Inaba, I. Kiruna, VHF Doppler radar determination of the momentum flux inthe upper troposphere and lower stratosphere: comparison between the three-and four-beam methods, J.Atmos. Oceanic Technol., 5, 57-69, 1988.Hines, C. O., Momentum deposition by atmospheric waves, and its effects on thermospheric circulation, Space Res.,12, 1157-1161, 1972.Lilly, D. K., Wave momentum flux- G.A.R.P. problem, Bull. Am. Meteorol. Soc., 53, 17-23,1972.Manson, A. H., C. E. Meek, Characteristic of gravity waves (10 min-6 hours) at Saskatoon (52 0 N,107 0 E): observationsby the phase coherent medium frequency radar, J. Geophys. Res., 98, 20,357-20,367, 1993.Newton, C. W., Mountain torques in the global angular momentum balance, J. Atmos. Sci., 28, 623-628, 1971.Thomas, I., I. T. Prichard, I. Astin, Radar observations of an inertia-gravity wave in the troposphere and lowerstratosphere, Ann. Geophysicae, 10, 690-697, 1992.Vincent, R. A., D. C. Fritts, A morphology of gravity waves in the mesosphere and lower thermosphere overAdelaide. Australia, J. Atmos. Sci., 44, 748-760, 1987.Vincent, R. A., I. M. Reid, HF Doppler measurements of mesospheric gravity wave momentum fluxes, J. Atmos.Sci., 40, 1321-1333, 1983.344
Figure1. Three-day average of momentum flux andvariance of wind fluctuations determined from theMST radar data during 1000-1600 LT from 16-18October 2000 (upper panel), 09-11 April 2001(Lower panel). Thick and thin solid lines in third panelof both the lower and upper part shows the zonal andmeridional variances respectivelyFigure 2. Same as figure 1 but for 17-19 July 2001(Upper panel) and 22-24 January 2002 (Lower panel)Figure 3. Momentum flux vertical profiles are determined by the four-beam and three-beammethod using Indian MST radar windsFigure 4. Vertical profiles of zonal and meridional momentum flux determined by the four beam methodfor different frequency bands during 16-19 October 2000. The solid line represents zonal momentum fluxand dotted line represents meridional momentum flux345
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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
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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
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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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Page 313 and 314: In Fig. 2 a sketch of a mountain le
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Page 325 and 326: 3. Results and discussionUHF profil
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Page 333 and 334: Histogram of Zonal Velocityh=5.13 K
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Page 343 and 344: spectral processing. In this partic
Page 345 and 346: 3. Results and discussionIn the pre
Page 347 and 348: 4. SummaryAn attempt has been made
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Page 353 and 354: 3. The improved method to estimate
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Page 363 and 364: FIRST RESULTS OF THE BOUNDARY LAYER
Page 365 and 366: Figure 3. Pulse Design Diagram to s
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Page 373 and 374: 3. Cloud Evolution Case StudyOn the
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Page 377 and 378: Experiment 1 Experiment 2IPP 999Km
Page 379 and 380: ELECTRONIC DIGITAL BEAMFORMING IMPL
Page 381 and 382: The main element of the unit (figur
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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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