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A/Ds. All timing signals for EAR operation are generated by the timing generator inthe RC. The RC sends parameters of operation to the receiver and TRX.The SP performs a series of signal processing operations (pulse decoding, coherent integration,fast Fourier transform (FFT), incoherent integration), and sends the processeddata to the host computer (HC). The digitized I and Q signals are stored in the FIFO(First-In/First-Out) memory (double-buffered memory) in the A/Ds. The output is sentto the pulse decoding and coherent integration units with header data added. After pulsedecoding the digitized I and Q signals are coherently integrated for each beam and range.The coherent integration unit adds a specified number of I and Q signals and outputs32-bit data to double-buffered memory. The data from the ranges to be processed areselected and sent to the digital signal processing (DSP) unit. The integrated I and Qsignals are stored in the buffered memory of the DSP unit, and rearranged into timeseries at respective ranges. The DSP then performs complex FFT and power spectrumcalculations on these time series. The DSP also performs a specified number of incoherentintegrations of the power spectra. After incoherent integration the power spectra aresent to the HC. The HC sends operating parameters to the RC and controls start/stopof operation of the entire system. It also receives observed data from the SP and storethem to digital data storage (DDS) tape.ConclusionThe EAR has been continuously operated since July 2001, with some intermittentshort-term data gaps. The EAR is usually operated with a standard observation modeto observe the whole troposphere and the lower troposphere (2–20 km) with the time andvertical resolution of ∼90 sec and 150 m, respectively. The equatorial cross-tropopauseprocess is considered to play an important role on global stratosphere-troposphere exchange(STE). Observations by the EAR in the tropical tropopause layer (TTL) havebeen reported [Fujiwara et al., 2003; Yamamoto et al,, 2003]. The EAR is also capable ofviewing the ionosphere in directions perpendicular to the geomagnetic field, and it is thefirst one established in the Indonesian-Thai longitude sector (10.63 ◦ S, 171.93 ◦ E). Studieson field-aligned irregularities (FAIs) in the ionospheric E and F regions also have beenreported [Fukao et al., 2003b]. Additionally, the EAR has the capability to observe thinatmospheric structures by the frequency domain interferometry (FDI) or the frequencydomain interferometric imaging (FII) techniques. Many phenomena that remains to beuncovered in the equatorial atmosphere will be clarified by the EAR.ReferencesFukao, S., H. Hashiguchi, M. Yamamoto, T. Tsuda, T. Nakamura, M. K. Yamamoto,T. Sato, M. Hagio, and Y. Yabugaki, The Equatorial Atmosphere Radar (EAR): Systemdescription and first results, Radio Sci., 38(3), 1053, doi:10.1029/2002RS002767, 2003a.Fukao. S., Y. Ozawa, T. Yokoyama, M. Yamamoto, and R. T. Tsunoda, Firstobservations of spatial structure of 3-m-Scale field-aligned irregularities with theEquatorial Atmosphere Radar in Indonesia, In revision, J. Geophys. Res., 2003b.Fujiwara, M., M. K. Yamamoto, H. Hashiguchi, T. Horinouchi, and S. Fukao,Turbulence at the tropopause due to breaking Kelvin waves observed by the EquatorialAtmosphere Radar, Geophys. Res. Lett., 30(4), 1171, doi:10.1029/2002GL016278, 2003.Yamamoto, M. K., M. Fujiwara, T. Horinouchi, H. Hashiguchi, and S. Fukao,Kelvin-Helmholtz instability around the tropical tropopause observed with theEquatorial Atmosphere Radar, Geophys. Res. Lett., 30(9), 1476,doi:10.1029/2002GL016685, 2003.408
Table 1: Specifications of the EAR system (from Fukao et al., 2003a)ItemSpecificationLocation:0.20 ◦ S, 100.32 ◦ E, 865 m above sea levelGeomagnetic latitude and longitude 10.63 ◦ S, 171.93 ◦ ERadar system:Monostatic pulse Doppler radarOperating frequency:47.0 MHzAntenna: Quasi-circular antenna array of 560 threeelement Yagi antennasAperture:110 m in diameterBeam width:3.4 ◦ (half power width; one way)Beam direction in azimuth: 0–360 ◦ in 0.1 ◦ stepsBeam zenith angle:0–30 ◦ in 0.1 ◦ steps (no grating lobe)Gain:33 dBiTransmitterPeak power:100 kW (sum of all TR modules)Average power:5 kW (max; sum of all TR modules)Number of TR modules:560 units (same as Yagi antennas)Single TR module’s power: 180 W/unitPulse width: 0.5–256 µsIPP:200 µs–10 ms (variable in 200µs steps)ReceiverType:Single super heterodyneNoise figure:5 dB (TR modules)Pulse compression:Barker, complementary and Spano codes (1 to16 bits)Subpulse width:0.5, 1.0, 2.0, 4.0, 8.0, 16.0 µs (variable)Dynamic range:70 dBA/D converter:14 bitsNumber of range gates:256 (max.)409
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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
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
Page 385 and 386: esulting in a widening of the bandw
Page 387 and 388: ON THE RADIATION EFFICIENCY OF COCO
Page 389 and 390: Table 2: Experiment #1 results, Tra
Page 391 and 392: A NEW NARROW BEAM MF RADAR AT 3 MHZ
Page 393 and 394: Off-zenith beams towards N, S, E, W
Page 395 and 396: 95ALWIN VHF radar: signal powerdB80
Page 397 and 398: ANTENNA BEAM VERIFICATION USING COS
Page 399 and 400: Figure 2: A 45 MHz reference sky te
Page 401 and 402: AN ATTEMPT TO CALIBRATE THE UHF STR
Page 403 and 404: is at 4.7 km, but in the first 4-ga
Page 405 and 406: 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
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Page 413: THE EQUATORIAL ATMOSPHERE RADAR:SYS
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 and 458: Enhanced resolution applyingpulse s
Page 459 and 460: Beckmann, Spizichino, 1964Fig. 8 Po
Page 461 and 462: Fig. 11 Plots of temporal variation
Page 463 and 464: 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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