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In addition, there is an excellent agreement between the radar winds over Piura andwinds obtained from the NCEP Reanalysis model [Kalnat et at., 1996]. In Figure 5 we showNCEP data for every 6 hours while BLT data are shown for every 1 hour for both Piura (left)and Porcuya (right). At Porcuya the agreement is not as good. We think this is because themodel does not have any input data from close by stations and therefore it does not representwell the winds over this part of the Andes. The assimilation of the Porcuya winds will help themodel outputs of the NCEP model around these areas.4. ConclusionsFigure 5. BLT-NCEP Comparison. Left: Piura (Apr, 2002). Right: Porcuya (Dec, 2002)The winds obtained with the newly installed BLT system at Piura are in very goodagreement with winds obtained with the collated ST radar and pilot balloon system. In addition,there is excellent agreement with the winds from NCEP Reanalysis model. The discrepancyobserved at Porcuya between the BLT and NCEP could be due the poor representation of thispart of the Andes by the NCEP model. The assimilation of the Porcuya data will help improvethe model outputs.Currently the BLT winds from Piura are available in real time at the IGP web page andat the NOAA Forecast Laboratory web page. Winds from Porcuya are made available via thesame web pages once a month, but we are working on a solution to send them in real timethrough the GOES system.5. BibliographyBriggs, B. H., The analysis of spaced sensor records by correlation techniques, in Handbookfor the Middle Atmospheric Program, pp. 166-186, SCOSTEP Secr. Univ. of Ill., Urbana,1984.Chau, J.L., R.F. Woodman, and L. A. Flores. Statistical characteristics of low-latitudeionospheric field-aligned irregularities obtained with the Piura VHF radar, AnnGeophysicae, 20(8), 1203-1212, 2002.Gage, K. S., B. B. Balsley, W.L. Ecklund, D. A. Carter, and J. R. McAfee, Wind profilerrelatedresearch in tropical Pacific, J. Geophys. Res., 96, 3209-3220, 1991.Kalnay et al., The NCEP/NCAR 40-year Reanalysis Project, Bull. Amer. Meteor. Soc. 77, 437-471, 1996Palo, S.E. , J. L. Chang, S. K. Avery, A. C. Riddle, and K. S. Gage, Detection of Outliers inStratospheric / Tropospheric Wind Velocity Estimates, Seventh Workshop on Scientificand Technical Aspects of MST Radar, 237-240, 1996IGP Database : http://jro.igp.gob.pe/database/blt_cns/bltrdata.htmlNOAA Forecast Lab Database: http://www.profiler.noaa.gov/jsp/profiler.jsp?options=full360
MOVEABLE UHF/S-BAND PROFILER/DISDROMETERSYSTEMS AS A CALIBRATION STANDARD IN RAINY PLACESWallace L. Clark 1,2 , Kenneth S. Gage 2 , Christopher R. Williams 1,2 , Paul Johnston 1,2 ,and David Carter 21. CIRES/University of Colorado, Boulder, CO, 80309-0216, USA2. NOAA Aeronomy Laboratory R/AL3, Boulder, Colorado, 80305-3328, USAIntroductionA critically important task for many types of radar work is reflectivity calibration. Theobvious, and probably most thorough, method of calibrating is to find the radar constant bybringing the reflectivity observed from a standard calibration target into agreement with thevalue expected. However, the fixed and more or less vertical orientation of profiler/MSTradar beams makes the use of such artificial targets quite difficult. Fortunately, in locationswhere it rains, raindrops can serve as the calibration target. The relation between drop-sizedistribution (DSD) and reflectivity is well developed and may be measured for any givenperiod of time by a collocated surface disdrometer. The near vertical orientation of profilersand MST radars is nearly optimum for such a comparison, although it is required that a fullyrecovered range gate in the far field of the antenna be less than a few hundred meters abovethe surface. Commercial disdrometers are readily available that are rugged, stable overperiods of years, and thus suitable as a field reference standard. This technique has beenused many times over the years for scanning radar calibration (Joss, J. and Pittini, A., 1991),even though the geometry between scanning radars and a surface disdrometer is generally notso ideal.Since small profilers (Gage, K. S., Williams, C. R. et al., 2000) such as the AL (NOAAAeronomy Lab) UHF/disdrometer systems are quite moveable, they can serve as travelingreference standards for larger systems for which the low range gate requirement is notfulfilled. When collocated with such systems, the calibrated profiler becomes a transferstandard to the larger system provided echoes (clear air or rain) can be simultaneouslyobserved in nearly coincident range gates. Differing sizes of range gates, of course, wouldrequire some more sophisticated analysis.Over the last few years the AL has, along with studies of obtaining profiler basedDSDs ( Williams, C. R., Kruger, A. et al., 2000), been field-testing this disdrometer methodof calibrating profilers during the ground validation campaigns of the NASA/NASDATropical Rainfall Measuring Mission (TRMM). The results of these campaigns suggest thatcalibration accuracies within a dBZ or so are obtainable, and the technique has been used forverification, and in at least one case, correction of scanning radar observations. It has alsobeen found easy and beneficial to use this calibration procedure to monitor the health of radarsystems, thus allowing timely correction of occasional system component failures.Calibration SetupThe inset in Figure 1 shows a sketch, more or less to scale, of the geometricalrelationship of the disdrometer/profiler combination. The rest of the Figure shows an actualfield implementation for calibration of wind-profilers with disdrometers during the TRMM-LBA campaign. In this case there are two profilers of different wavelengths (10.6 and 32.8361
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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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Page 333 and 334: Histogram of Zonal Velocityh=5.13 K
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Page 339 and 340: Boundary layer height, km32.521.5(a
Page 341 and 342: Figure 1:Data from the MST radar at
Page 343 and 344: spectral processing. In this partic
Page 345 and 346: 3. Results and discussionIn the pre
Page 347 and 348: 4. SummaryAn attempt has been made
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Page 351 and 352: Figure1. Three-day average of momen
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Page 359 and 360: The profilers of WINDAS weredesigne
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Page 363 and 364: FIRST RESULTS OF THE BOUNDARY LAYER
Page 365: Figure 3. Pulse Design Diagram to s
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Page 373 and 374: 3. Cloud Evolution Case StudyOn the
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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
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Page 387 and 388: ON THE RADIATION EFFICIENCY OF COCO
Page 389 and 390: Table 2: Experiment #1 results, Tra
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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
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Page 413 and 414: THE EQUATORIAL ATMOSPHERE RADAR:SYS
Page 415 and 416: Table 1: Specifications of the EAR
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VHF ATMOSPHERIC AND METEOR RADAR IN
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ased upon a geotechnical engineerin
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VORTICAL MOTIONS OBSERVED WITH THE
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interpolation from the original gri
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A NEW MINIRADAR TO INVESTIGATE URBA
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e eliminated to analyze correctly t
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Session PWG 1: System Calibrations
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Session PWG 2: Data Analysis, Valid
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• the time series vectors x(k) of
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Fig. 4: reflectivity of the hydrome
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Session PWG 3: Accuracies and Requi
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Session PWG 4: International Collab
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Session II.E: NOVEL PERSPECTIVES AN
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2 Proposed AlgorithmReceived signal
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N#4E-1-16E1A1#1#2A-1-1C1#3C-1-19Fig
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of conventional DCMP, with which th
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applying the directional constraint
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while for a beam of finite width, t
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In order to make the process more q
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WHAT IS TURBULENCE SEEN BY VHF RADA
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Enhanced resolution applyingpulse s
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Beckmann, Spizichino, 1964Fig. 8 Po
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Fig. 11 Plots of temporal variation
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Fig. 14 Distributions of phase cent
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Hocking, W.K., Radar studies of sma
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THE STRUCTURE FUNCTION-BASED APPROA
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{ Ui( t), Vi( t), Wi( t)} = { Ui ,
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161). Assumption 2H: the instantane
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Only the second order SF are consid
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fluctuations umk( t ) along the bas
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VHF PARASITIC RADAR INTERFEROMETRYF
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• All the costs of transmitter pr
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Figure 2: Example of range-azimuth
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Target Altitude, km1009080706050403
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ReferencesGriffiths, H. D., A. J. G
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Participants ListAvery, James P.Uni
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Hysell, David L.EAS/Cornell Univers
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Silva, Robert R.ATRADAustraliarsilv
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AAdachi, A. .......................
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TTabary, P. .......................
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