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3. Results and discussionThe LAWP observations [Figure 2(a)] show the top of CBL as a distinctive signaturein a time-height plot of reflectivity. Figure 2(b) shows diurnal variations of ozone observed atGadanki on 18 April 1999. The distribution of ozone in the CBL is irregular due to localizedproduction zones and the dynamic processes of the region. The summer afternoon periodsthat are most conducive to ozone production and also periods of intense convective mixing inthe CBL. Precursor gases are drawn into turbulent eddies from localized sources and fromhorizontally advected sources located near the top of the boundary layer or folded into theboundary layer by meteorological processes. The irregular nature of the summer afternoonozone distribution could observed in vertical profiles and time sequences of ozonemeasurements. At other times of the day, the stable nocturnal boundary layer may exhibitalmost constant ozone values. Ozone can be produced during the day by photo oxidation ofprecursor gases (Crutzen et al., 1999, and references therein). Mixing ratios of ozone startincreasing gradually after sunrise, attaining maximum values during near local noontime.Figure 2(c) shows the diurnal variations of ozone observed at Gadanki from 01-30 April1999 (DOY 90-120). Boundary layer processes and meteorology influences the ozonevariability at rural site, Gadanki. Daytime production of ozone is observed throughout themonth except during cloudy and rain days. At Gadanki, near to the UV analyzer, LAWP isused to obtain three dimensional wind speed measurements up to about 4000 m with avertical resolution of 150 m, with a precision of 1 m/s for the wind speed and 10 degree forthe wind direction (Reddy et al. 2002). The wind patterns are clearly dominated by thediurnal thermal regime. The daytime winds in the valley were typically from 7 to 10 m/snortheasterly wind regime which developed up to 1800 m between 08:00–09:00 LT (localtime) and 19:00–20:00 LT, while the night time winds are rather weak, 1–2 m/s, blowingfrom the south. A Northeasterly stable wind regime could be noticed [Figure 2(d)] above1500 m msl during one-month observations. Our results indicate that the diurnal cycle ofozone production is controlled by local thermal winds. In the nighttime, for several days (13-15 & 27-30 April 1999) high Ozone concentrations are noticed when the boundary layerwinds are Westerly/northwesterly. Figure 2(c) and (d) show that important aspects of highOzone concentration patterns are due to the local circulations and sensitive to the interactionof synoptic, regional, and local influences.The month of April is dry period/pre-monsoon and also the beginning of summer-hotand very humid in southern India. During this period, maturation of the crops and consequentcessation of evapo-transpiration occur. No measurable rain fell during dry season; so soilmoisture was probably quite low. It is an ideal situation to form the convective boundarylayer at Gadanki region. The depth of the boundary layer is one of the fundamental propertiesthat influences on fluctuating trace gases mixing ratios. The evolution of surface ozone,dynamics and the estimation of the CBL height are shown in Fig.3(a). From the figure it canbe inferred that the surface averaged Ozone and CBL height are reasonably in goodagreement. Fig.3 (c) and (d) one can notice that the boundary layer winds during 27-29 April1999 were strong, a shift in wind direction in the middle of the boundary layer, discernabledespite in mixing height at Gadanki after 1830 LT. The shift to westerly/southwest windssimply results in the ozone transport from nearby city (Bangalore) that is being advectedtowards Gadanki region.The data collected during one-month experiment should prove useful for a wide rangeof modeling and analytical studies. The data are now being analyzed to obtain a detaileddescription and understanding of the nighttime ozone transportation from the urban region.332
Boundary layer height, km32.521.5(a)CBL_heightAverage_ ppbv60 6040Ozone (ppbv)Ozone (ppbv)204020(c)1090April’99 019506100111051611021115261203000 12 24 36 48 60 72April’99 27 28 29160(b)Day of year (April 1999)CBL(d)120Ozone% deviation8040090April’99 0195061001110516110211152612030Day of the year (April 1999)Height, kmApril’99 27 28 29Local Time, hrsFigure 3. (a) Average convective boundary layer heights and (b) averaged surface Ozone ( average over 1200-1500 hrs LT for each day) from 01-30 April1999. (c) Diurnal variation of suface Ozone and (d) horizonal winds observed from 27-29 April 1999.ReferenceAngevine, W.M., A.B.White, C.j.Senff, M.Trainer, R.M.Banta, and M.A.Ayoub, Urban-ruralcontrasts in mixing height and cloudiness over Nashville in 1999, J. Geophy. Res., 108, 4092,doi:10.1029/2001JD001061, 2003.Cohn, S.A., and W.M.Angevine, Boundary layer height entrainment zone thicknessmeasured by Lidars and Wind profiling radars, J. Appl. Meteorol., 39, 1233-1247, 2000.Crutzen, P. J., M. G. Lawrence and U. Poschl, On the background photochemistry oftropospheric ozone, Tellus Ser. A, 51, 123–146, 1999.Jacob, D. J., Logan, J.A., and Murti, P.P., Effect of rising Asian emissions on surface ozonein the United States, Geophys. Res. Lett., 26, 2175–2178, 1999.Lal, S., M.Naja and B.H.Subbaraya, Seasonal variations in surface ozone and its precursorsover an urban site in India, Atmos. Environ., 34, 2713–2724, 2000.Naja, M., and S. Lal, Changes in surface ozone amount and its diurnal and seasonal patterns,from 1954– 1955 to 1991– 1993, measured at Ahmedabad (23 o N), India, Geophys. Res.Lett., 23, 81– 84, 1996.Reddy, K.K., T.Kozu, Y.Ohno, K.Nakamura, A.Higuchi, K.M.C.Reddy, P.Srinivasulu,V.K.Anandan, A.R.Jain, P.B.Rao, R.Ranga Rao, G.Viswanthan, and D.N.Rao, Planetaryboundary layer and precipitation studies using Lower atmospheric wind profiler overTropical India, Radio Sci., 37, 14, doi: 10.1029/2000RS002538, 2002.333
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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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Page 289 and 290: the time-height section of a convec
Page 291 and 292: Thurai, M., T.Iguchi,T. Kozu, J.D.E
Page 293 and 294: There are two main mechanisms which
Page 295 and 296: Horel, J.D. and Cornejo-Garrido, A.
Page 297 and 298: estimating two independent and redu
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Page 301 and 302: Surface winds usually range from 10
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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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Page 311 and 312: presented in Praskovsky et al. (200
Page 313 and 314: In Fig. 2 a sketch of a mountain le
Page 315 and 316: In Fig. 8 the lamina is aligned on
Page 317 and 318: Figure 1: composite day (13 days) o
Page 319 and 320: virtual sensible heat fluxes ( Wm-2
Page 321 and 322: 3. Characteristics of precipitation
Page 323 and 324: Fig. 3: Horizontal distribution of
Page 325 and 326: 3. Results and discussionUHF profil
Page 327 and 328: Figure 4. Monthly variation of slop
Page 329 and 330: system with two receiving antennae,
Page 331 and 332: cycle of precipitation. Figure 3(a)
Page 333 and 334: Histogram of Zonal Velocityh=5.13 K
Page 335 and 336: 5. Summary of results and concludin
Page 337: the two nearby major cities, Chenna
Page 341 and 342: Figure 1:Data from the MST radar at
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
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
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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
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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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