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the upper region are similar to those observed at other radars [Yamamoto et al, 1991; Pan etal., 1998; Tsunoda et al., 1998] and the maximum occurrence period is between 23 and 05LT.The lower region echoes consists of QP and continuous features just like thoseobserved in the daytime ones. Again, we find that there is 45 % characterized QP featuresthat is the night LQP echoes [Pan and Rao, 2002]. The occurrence ranges of the night timeLQP echoes are slightly lower than the daytime LQP echoes. We note that 57 % of themappeared between 95 to 97 km ranges, 24 % between 92 and 94 km ranges and 13 % of themoccurred at other ranges. The periodicity features are similar to those of the daytime LQPechoes that the majority is around 2 minutes period. Unlike the horizontally distributeddaytime LQP echoes, most of the nighttime LQP present significant descending rate withabout 1.5 km/hour.Figure 3 presents the histograms of the mean radial velocity of the echoes for threecategories: (left) daytime echoes at 90-110 km ranges (central) nighttime echoes at 90 to 105km ranges, and (right) nighttime echoes at 105 to 140 km ranges. We notice the figure 3presents wider ranges of value from the left to the right plots. The mean radial velocities atthe lower E region vary between –30 and +30 m/s for daytime and –50 to +50 m/s during thenighttime and the values may vary from –100 to +100 m/s during the nighttime upper Eregion. Furthermore, the mean radial velocities of the lower E region echoes are close to zerofor both daytime and nighttime but a downward velocity is noticed at the upper E region.Figure 4 shows the histograms of the spectral widths of the similar regions as inFigure 3. It is clearly shown in Figure 4 that the daytime and the nighttime (for both upperand lower regions) echo present different distributions. The mean spectral widths in thedaytime lower E region present a bell shape distribution with the mean value of about 30 m/s.On the other hand, nighttime echoes are non-symmetric and are wider than those detected inthe daytime. The majority of the spectral width in the lower region is narrower (about 50 to60 m/s) than the one in the upper region (about 70 m/s).Figure 3. The histograms of the mean radial velocity of the echoes.Figure 4. The histograms of the spectral widths of the echoes.Summary and DiscussionsOver all, the following characteristics of the E region FAI observed by the Gadankiradar based on this data set are notified:(1) There are two echoing regions: the lower region between 90 and 100 km ranges and theupper region between 105 and 120 km ranges.(2) Echoes observed in both the upper and lower regions are similar to type 2 echoes reportedby other radars in the mid-latitudes.(3) Echoes of the lower region may occur in daytime as well as in nighttime. Although thereis an observation break between 06 and 09 LT, noontime (11 to 14 LT) seems to be theminimum period of occurrence. QP echoes are commonly detected at the lower region no116
matter daytime or nighttime and are the so-called “LQP echoes”.(4) The spectral characteristics of the lower region echoes differ from daytime and nighttime.The mean Doppler velocities are more variant than those of the daytime and the spectralwidths are broader in the nighttime.(5) The upper region echoes appeared only in the nighttime with a maximum period between23 and 05 LT. Typical QP echoes detected here are similar to those observed atmid-latitudes.(6) Unlike the value close to zero of the mean radial velocities of the lower E region echoes,a downward velocity is noticed at the upper E region. Both the mean Doppler velocitiesand the spectral widths are found larger than those of the lower regions.Concluding remarksBy examining the 15-day data set gathered in the summer of 1998 and 1999, wepresent the morphological features of the E region FAI observed by the Gadanki radar. Wealso compare the features of the FAI echoes between Gadanki and Piura radars since thegeomagnetic latitude of these two radars are close. Although the morphological distributionand spectral characteristics are very similar for those FAI echoes, daytime echoes and theLQP echoes are rarely reported by Piura. It is suggested that the neutral winds may play arole in this discrepancy since those echoes usually occur at the altitudes below 100 km. It willbe very interesting to study how the neutral winds affect the lower region FAI echoes in thecoming communication.References:Chau, J.L. and R.F. Woodman, Low-latitude quasiperiodic echoes observed with the PiuraVHF radar in the E region, Geophys. Res. Lett, 26, 2167-2170, 1999.Choudhary,R.K., and K.K.Mahajan, Tropical E region field aligned irregularities:Simultaneous observations of continuous and QP echoes, J. Geophys. Res., 104, 2613-2619,1999.Fukao, S., M. Yamamoto, R.T.Tsunoda, H. Hayakawa,and T. Mukai, The SEEK (Sporadic EExperiment over Kyushu)campaign, Geophys. Res. Lett, 25, 1761-1764, 1998.Pan, C.J., and P.B.Rao, Low altitude quasi-periodic radar echoes observed by the GadankiVHF radar, Geophys. Res. Lett, 29, 25-1, 2002.Rao P B , A R Jain , P Kishore, P Balamuralidhar, S H Damle and G Viswanathan, IndianMST radar, 1, System description and sample wind measurements in ST mode, Radio Sci.,30, 1125, 1995.Tsunoda, R.T., S. Fukao, and M. Yamamoto, On the origin of quasi-periodic radarbackscatter from midlatitude sporadic E, Radio Sci, 29, 349-365, 1994.Woodman, R.F., M. Yamamoto, and S. Fukao, Gravity wave modulations of gradient driftinstabilities in midlatitude sporadic-E irregularities, Geophys. Res. Lett., 18, 1197-1200,1991.Yamamoto, M., S. Fukao, R.F. Woodman, T. Ogawa, T. Tsuda, and S. Kato, MidlatitudeE-region field aligned irregularities observed with the MU radar, J. Geophys. Res., 96,15943-15949, 1991Woodman R F, Spectral moment estimation in MST radars, Radio Sci.,20, 1185, 1985.117
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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
Page 71 and 72: P C(dB)(a) Echo Power60504030200.70
Page 73 and 74: most occidental area of South Ameri
Page 75 and 76: Quegan, 1992). It should be useful
Page 77 and 78: measurements, is shown in figure 1(
Page 79: The present observations thus empha
Page 82 and 83: RECENT OBSERVATIONS OF E REGION FIE
Page 84 and 85: measured spectra in order to separa
Page 86 and 87: drifts at E and F regions heights b
Page 88 and 89: • Are characterized by type II ec
Page 90 and 91: The main parameters that could be o
Page 92 and 93: THE ROLE OF UNSTABLE SPORADIC-E LAY
Page 94 and 95: (σ H / σ P )E y (where σ H and
Page 96: STUDY OF A LOW E-REGION QUASI-PERIO
Page 99 and 100: 100 m/syrFigure 4: Geometry of the
Page 101 and 102: Where the notations carry same mean
Page 103 and 104: Where dx/dt and dy/dt are the veloc
Page 105 and 106: non-negativity of the image is prio
Page 107 and 108: spectrum corresponding to the backs
Page 109 and 110: The Artigas and Machu-Picchu Statio
Page 111 and 112: Arguments against the second altern
Page 113 and 114: Extension of the Kolmogorov spectru
Page 115 and 116: volumeESRvolumeSSRSSR SSRESR ESRSSR
Page 117 and 118: individual particles in a statistic
Page 119 and 120: Anomalous spectraTalkner [4] studie
Page 121: To observe the E region FAI echoes,
Page 125 and 126: two sub-arrays, each sub-array made
Page 127 and 128: 4. SummaryHere we describe a radio
Page 129 and 130: Figure 1. E-region DPS4 spectra, ri
Page 131 and 132: effects. It is therefore plausible
Page 133 and 134: 1996 and high in 2002). The electri
Page 135 and 136: electric fields map along the geoma
Page 137 and 138: SNR condition is always difficult a
Page 139 and 140: Figure-4 Power spectrum plots of a
Page 141 and 142: As we show below, Jicamarca offers
Page 143 and 144: particularly during daytime counter
Page 145 and 146: where ˆδ nm = (δ l − δ m )
Page 147 and 148: PMSE is more easily interpreted as
Page 149 and 150: ResultsTemperature climatology• s
Page 151 and 152: Simultaneous PMSE and NLC observati
Page 153 and 154: ResultsSeasonal variationMSE are no
Page 155 and 156: Figure 2: MSE parameters as functio
Page 157 and 158: Session I.3: Winds, waves and turbu
Page 159 and 160: poor. It was shown that poor perfor
Page 161 and 162: The use of diffraction pattern simi
Page 163 and 164: F 13 (ξ x ′) = (1 − cos 2ψ N)
Page 165 and 166: Figure 3: (a) Baseline length depen
Page 167 and 168: 3. ResultsFigure 1 shows the amplit
Page 169 and 170: variability.Figure 4 shows the aver
Page 171 and 172: 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
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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
Page 493 and 494:
AAdachi, A. .......................
Page 495:
TTabary, P. .......................
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