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43.0Height (km)32CBL height from Wind profiler(Km)2.52.01.51305 310 315 320 -15.5 -15.0 -14.5 -14.0Virtual potential temperature (K)C 2 n(m -2/3 )Figure2: Height profiles of Virtual potential2temperature and C n as observed on 27July1999.1.01.0 1.5 2.0 2.5 3.0CBL h e i g h t f r o m r a d i o s o n d e(Km)Figure 3: Scatter plot of CBLheights derived from the radiosondeand the wind profiler observations.The striking feature in the present case is that the CBL is continuously growing after 1200 hrsalso. The CBL heights are also very high with an increasing trend up to 1500 hrs, after whichprecipitation was observed over the wind profiler site. The deepening of the CBL is observedin the late afternoon in the present case, whereas it is observed exactly at the midday on thenon-convective days. Figure 4 (c) shows the evolution of CBL on four convective daysduring the monsoon period. On these days, a different picture has been observed. A shallowCBL confined to ~1.5 km is observed on all the days. It is well known that during themonsoon, boundary layer will be rich in moisture. So, most of the radiation from the surfacewill be utilized for the evaporation process, which results in a shallow CBL. Enhanced soilmoisture probably contributes to increase the latent heat fluxes and thus decreasing thesurface sensible flux locally and suppress the CBL growth, as compared to the deeper CBLthat develops with reduced soil moisture level on pre-monsoon days. One more cause for theshallow CBLs during the monsoon days may be due to the increased upper level clouds thatcan reduce the incoming solar radiation. Similar features have been observed on most of thedays in each category during the campaign period.3.02.51 May 19995 May 19996 May 199916May 19997 May 19998 May 19999 May 199910 May 199906 July 199912 July 199902 August 199904 August 1999CBL H e i g h t (Km)2.01.51.00.58 9 10 11 12 13 14 15 16 17 18Local Time (hrs)8 9 10 11 12 13 14 15 16 17 188 9 10 11 12 13 14 15 16 17 18(a) (b) (c)Figure 4: Evolution of CBL on four (a) non-precipitating days, (b) pre-monsoonconvective days and (c) monsoon convective days340
4. SummaryAn attempt has been made to study the evolution of the CBL in non-precipitating, premonsoonand monsoon convective days. A well-distinguishable feature is observed in thepre-convective environments, which can be used as precursor for the convection triggering.In the non-precipitating environments, the CBL has peaked in the mid-day and suddenlydescended to lower altitudes and showed decreasing trend thereafter. In the pre-monsoonconvective environments, the CBL has continued to grow after mid-day also and shallowCBL has been observed during the monsoon convective days. The intriguing result fromthese studies is the distinguishable CBL evolution observed in the pre-convectiveenvironments of pre-monsoon and monsoon periods. These observations are preliminary innature and a detailed study using various boundary layer observational facilities likeautomatic weather station, kytoons and radiation measurements are planed in near future.AcknowledgementsThe National MST Radar Facility (NMRF) is operated as an autonomous facilityunder Department of Space with partial support from Council of Scientific and IndustrialResearch. The authors are grateful to the NMRF technical staff whose dedicated efforts madepossible the observations reported here. UHF radar setup and being operated at NMRF underjoint collaborate programme between India and Japan.ReferencesBalsley, B.B., and K.S. Gage, on the use of radars for operational wind profiling, Bull. Amer.Meteorol. Soc. 63, 1009-1018, 1982.Davis, K.J., D.H. Lenschow, S.P. Oncley, C. Kiemle, G. Ehret, A. Giez, and J. Mann, Role ofentrainment in surface-atmosphere interactions over the boreal forest, J. Geophys. Res,102, 29219–29230, 1997.Fairall, C.W., The Humidity and Temperature sensitivity of clear-air radars for the cloud freeconvective boundary layer, J. Appl. Meteorol. 8, 1064-1074, 1991.Grimsdell, A.W., and W.M Angevine, Observations of the afternoon transition of theconvective boundary layer, J. Appl. Meteorol., 41, 3-11, 2002.Krishna Reddy, K., Kozu, T., Ohno, Y., Nakamura, K., Srinivasulu, P., Anandan, V. K., Jain,A.R., Rao, P.B., Ranga Rao, R., Viswanathan, G., and Rao, D.N., Lower atmosphericwind profiler at Gadanki, Tropical India: initial result, Meterologische Zeitschrift, 10,457-466, 2001.White, A.B., Fairall, C.W., and Thompson, D.W., radar observations of humidity variabilityin and above the marine atmospheric boundary layer, J. Atmos. Oceanic. Technol., 8, 639-658, 1991a.Wyngaard, J.C., and M.A. LeMone, Behavior of the refractive index structure parameter inthe entraining convective boundary layer, J. Atmos. Sci., 37,1573-1585, 1980.341
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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
Page 295 and 296: Horel, J.D. and Cornejo-Garrido, A.
Page 297 and 298: estimating two independent and redu
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Page 301 and 302: Surface winds usually range from 10
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Page 307 and 308: Figure 8 shows the profile of virtu
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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
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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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Page 339 and 340: Boundary layer height, km32.521.5(a
Page 341 and 342: Figure 1:Data from the MST radar at
Page 343 and 344: spectral processing. In this partic
Page 345: 3. Results and discussionIn the pre
Page 349 and 350: The purpose of this study is to exa
Page 351 and 352: Figure1. Three-day average of momen
Page 353 and 354: 3. The improved method to estimate
Page 355 and 356: But in case of period until 1800 UT
Page 357 and 358: Session I.5: Operational Aspects an
Page 359 and 360: The profilers of WINDAS weredesigne
Page 361 and 362: NOAA, 1994 : Wind profiler assessme
Page 363 and 364: FIRST RESULTS OF THE BOUNDARY LAYER
Page 365 and 366: Figure 3. Pulse Design Diagram to s
Page 367 and 368: MOVEABLE UHF/S-BAND PROFILER/DISDRO
Page 369 and 370: one-minute Z values determined from
Page 371 and 372: TOWARD A MULTISENSOR GROUND BASED R
Page 373 and 374: 3. Cloud Evolution Case StudyOn the
Page 375 and 376: DEVELOPMENT OF A DIGITAL RECEIVER F
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
Page 383 and 384: .ON-LINE ADAPTIVE DC-GROUND-CLUTTER
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Page 387 and 388: ON THE RADIATION EFFICIENCY OF COCO
Page 389 and 390: Table 2: Experiment #1 results, Tra
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Page 393 and 394: Off-zenith beams towards N, S, E, W
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ANTENNA BEAM VERIFICATION USING COS
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Figure 2: A 45 MHz reference sky te
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AN ATTEMPT TO CALIBRATE THE UHF STR
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is at 4.7 km, but in the first 4-ga
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QUALITY CONTROL FOR DOPPLER WIND PR
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The resulting moments are subjected
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SOUSY RADAR AT JICAMARCA: SYSTEM DE
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NEControl andcomputer roomCompCoute
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THE EQUATORIAL ATMOSPHERE RADAR:SYS
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Table 1: Specifications of the EAR
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VHF ATMOSPHERIC AND METEOR RADAR IN
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ased upon a geotechnical engineerin
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VORTICAL MOTIONS OBSERVED WITH THE
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interpolation from the original gri
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A NEW MINIRADAR TO INVESTIGATE URBA
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e eliminated to analyze correctly t
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Session PWG 1: System Calibrations
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Session PWG 2: Data Analysis, Valid
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• the time series vectors x(k) of
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Fig. 4: reflectivity of the hydrome
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Session PWG 3: Accuracies and Requi
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Session PWG 4: International Collab
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Session II.E: NOVEL PERSPECTIVES AN
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2 Proposed AlgorithmReceived signal
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N#4E-1-16E1A1#1#2A-1-1C1#3C-1-19Fig
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of conventional DCMP, with which th
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applying the directional constraint
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while for a beam of finite width, t
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In order to make the process more q
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WHAT IS TURBULENCE SEEN BY VHF RADA
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Enhanced resolution applyingpulse s
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Beckmann, Spizichino, 1964Fig. 8 Po
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Fig. 11 Plots of temporal variation
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Fig. 14 Distributions of phase cent
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Hocking, W.K., Radar studies of sma
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THE STRUCTURE FUNCTION-BASED APPROA
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{ Ui( t), Vi( t), Wi( t)} = { Ui ,
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161). Assumption 2H: the instantane
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Only the second order SF are consid
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fluctuations umk( t ) along the bas
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VHF PARASITIC RADAR INTERFEROMETRYF
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• All the costs of transmitter pr
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Figure 2: Example of range-azimuth
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Target Altitude, km1009080706050403
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ReferencesGriffiths, H. D., A. J. G
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Participants ListAvery, James P.Uni
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Hysell, David L.EAS/Cornell Univers
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Silva, Robert R.ATRADAustraliarsilv
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AAdachi, A. .......................
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TTabary, P. .......................
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