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Characteristics of 0.3 - 6 hr IGWs at Shigarakiz,km Total r.m.s. Amplitude, m/s309206103030Zonal r.m.s. Amplitude, m/s09.0206.0103.0030Meridional r.m.s. Amplitude, m/s0.09.0206.0103.000 3 6 9 12Months of Year0.0Fig. 3. Calculated standard deviations of horizontal wind (top), zonal(middle) and meridional (bottom) wind components produced by theIGW spectrum and calculated for Shigaraki.IGW Energy Characteristics at Shigarakiz,km Turbulent Diffusivity, m2/s30820104030201003020100Zonal Wave Acceleration, m/s2Zonal Wave Momentum Flux, m2/s20 3 6 9 12Months of Year060300-30-600.0-1.5-3.0Fig. 4. Coefficient of turbulent diffusion (top), zonal waveacceleration of the mean flow (middle) and the zonal component ofvertical wave momentum flux (bottom) produced by the IGWspectrum and calculated for the Issyk-Kul station.The presence of turbulence in the atmosphere produces the mixing, which leads, inparticular, to the fluxes of atmospheric admixtures from the troposphere to the stratosphere orback depending on the vertical distribution of the particular admixture. In particular,turbulence may lead to descend of ozone from the stratosphere to the troposphere. Thevertical flux of an admixture can be described by the following formulae:F = −Kncdln c / dz , (1)where K is the turbulent diffusion coefficient; n is the number density of the atmosphere; c isthe mixing ratio of the considered admixture. Using the values of c for the altitudes 12 – 17km from the model of vertical ozone profile [Zuev and Komarov, 1986] for the values of K ~1 – 10 m 2 /s shown in Figures 2 and 4 we may obtain the estimate F ~ (1–10)×10 14 m -2 s -1 . Itis comparable with usually assumed downward ozone transport by the general circulation ofthe atmosphere.236
The main recently assumed mechanism of penetration of stratospheric ozone into thetroposphere is its transport by the general atmospheric circulation from equatorial latitudesand descending of the air in the middle latitudes [Holton, 1990]. The mean downward ozoneflux due to the circulation transport is estimated to be about F ~ 7×10 14 м -2 s -1 [Ebel et al.,1993], while the estimations of tropospheric ozone require the fluxes of stratospheric ozone ofthe order of (4-8)×10 14 м -2 s -1 [e.g. Crutzen, 1988]. Comparison of these values with theestimations of the ozone diffusion flux obtained above show the comparability of thesevalues. Therefore, the turbulence generation by gravity waves near the tropopause mayproduce substantial transport of ozone from the stratosphere to the troposphere.One can estimate the time scale characteristic for the transport into the troposphere of allstratospheric ozone (in the absence of its sources): τ ~ N/F, where N is the total ozone contentin the atmospheric column above considered altitude. Described above estimations of Ktogether with the model of vertical ozone distribution [Zuev and Komarov, 1986] lead to thevalues of τ ~ 0,3 – 3 day -1 . These values show that the changes of IGW intensity andturbulence near the tropopause may relatively fast lead to the changes of stratospheric ozoneconcentration and to a shift in the photochemical equilibrium. Therefore, local enhancementsof IGW intensity and turbulence at tropospheric altitudes over mountains due to theirorographic excitation may lead to the changes in total ozone over mountain regions. This mayexplain observed TO anomalies over mountain regions [Kazimirovsky and Matafonov, 1998].3. ConclusionA numerical simulation was used to verify the hypothesis about the influence of sharpchange of vertical temperature gradient at the tropopause on the increase of the amplitudes ofIGWs propagating upwards from the troposphere. Estimations of vertical ozone flux from thestratosphere to the troposphere are comparable with usually supposed ozone downwardtransport with the general atmospheric circulation.Acknowlegement. This study was partly supported by the Russian Basic ResearchFoundation and by the International Science and Technology Center.References.Crutzen, P. J., Tropospheric ozone: An overview, In I.S.A Isaken (ed.), TroposphericOzone, D. Reidel Publ. Company, Dordrecht, 3-32, 1988.Ebel, A., H. Elbern, and A. Oberreuter, Stratosphere-troposphere air mass exchange andcross-tropopause fluxes of ozone. In Coupling processes in the lower and middle atmosphere,eds. Thrane, ER. V. et al., Kluner, Dortrecht, pp. 49-65, 1993.Fukao, S., M. D. Yamanaka, N. Ao, W. K. Hocking, T. Sato, M. Yamamoto, T. Nakamura,T. Tsuda, and S. Kato, Seasonal variability of vertical eddy diffusivity in the middleatmosphere, 1. Tree-year observations by the middle and upper atmosphere radar, J. Geophys.Res., 99, 18,973-18,987, 1994.Gavrilov N. M., Parameterization of momentum and energy depositions from gravitywaves generated by tropospheric hydrodynamic sources. Ann. Geophys.,15, 1570-1580, 1997.Gavrilov N. M., Yudin V.A. Model for Coefficients of Turbulence and Effective PrandtlNumber Produced by Breaking Gravity Waves in the upper Atmosphere, J. Geophys. Res.,97, 7619 -7624, 1992.Holton, J. R., On the global exchange of mass between the stratoshere and troposphere, J.Atmos. Sci., 47, 392–395, 1990.Kazimirovsky, E. S., and G. K. Matafonov, Continental scale and orographic structures inthe global distribution of the total ozone, J. Atmos. Solar-Terr. Phys., 60, 993-996, 1998.Zuev, V. E., and V. S. Komarov, Statistical models of temperature and gas components ofthe atmosphere, Hydrometeoizdat Press, Leningrad, 1986.237
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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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Page 201 and 202: These two last relations are the on
Page 203 and 204: 3.2.1 From v ′2 to ɛ kThe questi
Page 205 and 206: 5.2 Frequency distributionsSeveral
Page 207 and 208: ReferencesAlisse J.-R. and C. Sidi.
Page 209 and 210: Röttger J. and C.H. Liu. Partial r
Page 211 and 212: Specular reflection is negligible f
Page 213 and 214: −0.5C n2 Distribution (PROUST & S
Page 215 and 216: the beamwidth, α is the zenith ang
Page 217 and 218: this latitude in late April). Surfa
Page 219 and 220: Fig. 1. Median (upper) winds and (l
Page 221 and 222: Fig.1. Lines of constant radial vel
Page 223 and 224: which have not yet been considered
Page 225 and 226: is calculated from the radiosonde t
Page 227 and 228: Figure 3: Time-altitude cross-secti
Page 229 and 230: Absorption of cosmic noise is cause
Page 231 and 232: Incoherent scatter spectracompared
Page 233 and 234: variations of spectral widths, refr
Page 235 and 236: Figure 1. Diurnal variation of Turb
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Page 245 and 246: Figure 2. Statistics of numbers of
Page 247 and 248: LIDAR OBSERVATIONS OF MIDDLE ATMOSP
Page 249 and 250: latitudinal dependence of the seaso
Page 251 and 252: APPLICATION OF THE DUAL-BEAMWIDTH M
Page 253 and 254: Figure 2: Mean zonal and meridional
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Page 257 and 258: The monthly diurnal mean of horizon
Page 259 and 260: Session I.4: Meteorological Phenome
Page 261 and 262: Integration of the VHF wind profile
Page 263 and 264: Figure 1 : Map of the Lago Maggiore
Page 265 and 266: precipitating clouds, the cyclonic
Page 267 and 268: Eyewall(a)(b)(c)(d)Fig. 3: Radius-h
Page 269 and 270: as low as 0.55. The Piura 50-MHz ra
Page 271 and 272: place features in the profile with
Page 273 and 274: • Period 1 (June 1-10): SCCs exis
Page 275 and 276: Sumatera occurs by stratiform cloud
Page 277 and 278: very interesting to note the double
Page 279 and 280: 20(a) Convective Region(b) Transiti
Page 281 and 282: Typhoon LekimaFig. 2 Typhoon Lekima
Page 283 and 284: Fig. 5 Passage of typhoon Hayan on
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Page 287 and 288: 22 June 2000 23:22:23 - 23:24:20 at
Page 289 and 290: the time-height section of a convec
Page 291 and 292: Thurai, M., T.Iguchi,T. Kozu, J.D.E
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There are two main mechanisms which
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Horel, J.D. and Cornejo-Garrido, A.
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estimating two independent and redu
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RASS THETA (K) RASS v-component (m/
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Surface winds usually range from 10
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weak (maximum of 5 m s -1 ) and the
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The vertical component from the VTB
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Figure 8 shows the profile of virtu
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2 3D ( , ) ( ) ( ) ˆ ( ) ˆp∆ xm
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presented in Praskovsky et al. (200
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In Fig. 2 a sketch of a mountain le
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In Fig. 8 the lamina is aligned on
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Figure 1: composite day (13 days) o
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virtual sensible heat fluxes ( Wm-2
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3. Characteristics of precipitation
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Fig. 3: Horizontal distribution of
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3. Results and discussionUHF profil
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Figure 4. Monthly variation of slop
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system with two receiving antennae,
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cycle of precipitation. Figure 3(a)
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Histogram of Zonal Velocityh=5.13 K
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5. Summary of results and concludin
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the two nearby major cities, Chenna
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Boundary layer height, km32.521.5(a
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Figure 1:Data from the MST radar at
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spectral processing. In this partic
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3. Results and discussionIn the pre
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4. SummaryAn attempt has been made
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The purpose of this study is to exa
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Figure1. Three-day average of momen
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3. The improved method to estimate
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But in case of period until 1800 UT
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Session I.5: Operational Aspects an
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The profilers of WINDAS weredesigne
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NOAA, 1994 : Wind profiler assessme
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FIRST RESULTS OF THE BOUNDARY LAYER
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Figure 3. Pulse Design Diagram to s
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MOVEABLE UHF/S-BAND PROFILER/DISDRO
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one-minute Z values determined from
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TOWARD A MULTISENSOR GROUND BASED R
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3. Cloud Evolution Case StudyOn the
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DEVELOPMENT OF A DIGITAL RECEIVER F
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Experiment 1 Experiment 2IPP 999Km
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ELECTRONIC DIGITAL BEAMFORMING IMPL
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The main element of the unit (figur
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.ON-LINE ADAPTIVE DC-GROUND-CLUTTER
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esulting in a widening of the bandw
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ON THE RADIATION EFFICIENCY OF COCO
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Table 2: Experiment #1 results, Tra
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A NEW NARROW BEAM MF RADAR AT 3 MHZ
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Off-zenith beams towards N, S, E, W
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95ALWIN VHF radar: signal powerdB80
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ANTENNA BEAM VERIFICATION USING COS
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Figure 2: A 45 MHz reference sky te
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AN ATTEMPT TO CALIBRATE THE UHF STR
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is at 4.7 km, but in the first 4-ga
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QUALITY CONTROL FOR DOPPLER WIND PR
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The resulting moments are subjected
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SOUSY RADAR AT JICAMARCA: SYSTEM DE
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NEControl andcomputer roomCompCoute
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THE EQUATORIAL ATMOSPHERE RADAR:SYS
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Table 1: Specifications of the EAR
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VHF ATMOSPHERIC AND METEOR RADAR IN
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ased upon a geotechnical engineerin
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VORTICAL MOTIONS OBSERVED WITH THE
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interpolation from the original gri
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A NEW MINIRADAR TO INVESTIGATE URBA
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e eliminated to analyze correctly t
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Session PWG 1: System Calibrations
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Session PWG 2: Data Analysis, Valid
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• the time series vectors x(k) of
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Fig. 4: reflectivity of the hydrome
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Session PWG 3: Accuracies and Requi
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Session PWG 4: International Collab
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Session II.E: NOVEL PERSPECTIVES AN
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2 Proposed AlgorithmReceived signal
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N#4E-1-16E1A1#1#2A-1-1C1#3C-1-19Fig
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of conventional DCMP, with which th
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applying the directional constraint
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while for a beam of finite width, t
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In order to make the process more q
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WHAT IS TURBULENCE SEEN BY VHF RADA
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Enhanced resolution applyingpulse s
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Beckmann, Spizichino, 1964Fig. 8 Po
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Fig. 11 Plots of temporal variation
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Fig. 14 Distributions of phase cent
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Hocking, W.K., Radar studies of sma
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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. .......................
Page 495:
TTabary, P. .......................
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