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In the following (Figs. 5, 6, and 7) we repeat some more models, which all base on theoriginal idea of Bolgiano (1968). We note in all these models that the horizontal dimensionsof refractivity variations are mostly larger than the vertical ones, in particular close to theedges of turbulent layers. The corresponding vertical gradients, which characterize thisstructure, can be quite steep as in-situ temperature measurements have shown (Luce et al.,1995). Nothing is really known about their horizontal extent other than the deduction of scaleestimates, which follow from VHF radar observations. It is prudent that these sheets withsmall vertical extent and much larger horizontal extent, which are corrugated by surroundingturbulence, can be regarded as rough surfaces. Again, Beckmann and Spizzichino (1963) havetreated the corresponding reflection and scattering, which we show in Fig. 8.Hocking, 1987Fig. 5 Refractive index shaping (Hocking, 1987)Woodman and Chu, 1989Fig. 6 A turbulence layer containing large- and small-scale eddies(Woodman and Chu, 1989).From Hocking and Röttger, 2001Fig. 7 Velocity, temperature and refractive index inhomogeneities in a turbulentlayer, proposed by Hocking and Röttger (2001) following Klaasen and Peltier(1985), and Dalaudier and Sidi (1987) and others.452
Beckmann, Spizichino, 1964Fig. 8 Polar diagrams of forward scatter from refractive index surfaces ofdifferent roughness (a) very smooth surface to (d) very rough surface. FromBeckmann and Spizzichino (1964).The models of Beckmann and Spizzichino show the two extremes, namely specular-typereflection and diffuse scattering from a very rough surface. They did their models for obliqueincidence, which we immediately can revert into partial (specular-type) reflection at verticalincidence and monostatic backscatter as well, which determines the signals detected by VHFMST radars. Experience over the past two decades directs us to interpret our observations notin terms of pure backscatter from isotropic homogeneous turbulent refractive index variations,described by a Gaussian process, as is the condition for determining the turbulence refractiveindex structure constant C n 2 , as adequately developed by Ottersten (1969). The following newtype of radar observations and data representation should manifest this presumption.This method bases on the combination of spatial-domain-interferometry(SDI) and frequency-domain-interferometry(FDI), as itwas applied by Röttger (2000) for studyingthe three-dimensional motions of scatteringlocations on lightning channels. These are regardedas small-extent localized radar targets.The standard range gating allows only thelocalization within (the beam width and) therange gate r 0 ± r / 2 (see Fig.9). Additionalspatial-domain-interferometry allows thedetermination of position x 0 * in the horizontalplane, and a simultaneous frequency-domaininterferometryallows to position z 0 * withinthe range gate (with unknown initial position).Tracking of the target area as function of timeis possible by combining :Fig. 9 Geometry of positions determinedby the SDI and FDI technique.x 1 * = x 0 * + ∆x (from SDI)z 1 * = z 0 * + ∆z (from FDI).This can be extended into the y-plane as well.453
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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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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
Page 407 and 408: The resulting moments are subjected
Page 409 and 410: SOUSY RADAR AT JICAMARCA: SYSTEM DE
Page 411 and 412: NEControl andcomputer roomCompCoute
Page 413 and 414: THE EQUATORIAL ATMOSPHERE RADAR:SYS
Page 415 and 416: Table 1: Specifications of the EAR
Page 417 and 418: VHF ATMOSPHERIC AND METEOR RADAR IN
Page 419 and 420: ased upon a geotechnical engineerin
Page 421 and 422: VORTICAL MOTIONS OBSERVED WITH THE
Page 423 and 424: interpolation from the original gri
Page 425 and 426: A NEW MINIRADAR TO INVESTIGATE URBA
Page 427 and 428: e eliminated to analyze correctly t
Page 429 and 430: Session PWG 1: System Calibrations
Page 431 and 432: Session PWG 2: Data Analysis, Valid
Page 433 and 434: • the time series vectors x(k) of
Page 435 and 436: Fig. 4: reflectivity of the hydrome
Page 437 and 438: Session PWG 3: Accuracies and Requi
Page 439 and 440: Session PWG 4: International Collab
Page 441 and 442: Session II.E: NOVEL PERSPECTIVES AN
Page 443 and 444: 2 Proposed AlgorithmReceived signal
Page 445 and 446: N#4E-1-16E1A1#1#2A-1-1C1#3C-1-19Fig
Page 447 and 448: of conventional DCMP, with which th
Page 449 and 450: applying the directional constraint
Page 451 and 452: while for a beam of finite width, t
Page 453 and 454: In order to make the process more q
Page 455 and 456: WHAT IS TURBULENCE SEEN BY VHF RADA
Page 457: Enhanced resolution applyingpulse s
Page 461 and 462: Fig. 11 Plots of temporal variation
Page 463 and 464: Fig. 14 Distributions of phase cent
Page 465 and 466: Hocking, W.K., Radar studies of sma
Page 467 and 468: THE STRUCTURE FUNCTION-BASED APPROA
Page 469 and 470: { Ui( t), Vi( t), Wi( t)} = { Ui ,
Page 471 and 472: 161). Assumption 2H: the instantane
Page 473 and 474: Only the second order SF are consid
Page 475 and 476: fluctuations umk( t ) along the bas
Page 477 and 478: VHF PARASITIC RADAR INTERFEROMETRYF
Page 479 and 480: • All the costs of transmitter pr
Page 481 and 482: Figure 2: Example of range-azimuth
Page 483 and 484: Target Altitude, km1009080706050403
Page 485 and 486: ReferencesGriffiths, H. D., A. J. G
Page 487 and 488: Participants ListAvery, James P.Uni
Page 489 and 490: Hysell, David L.EAS/Cornell Univers
Page 491 and 492: Silva, Robert R.ATRADAustraliarsilv
Page 493 and 494: AAdachi, A. .......................
Page 495: TTabary, P. .......................
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