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iii. That the Superficial Sea Temperature Anomaly (SSTA) in front of Paita (in the north coastof Peru) is bigger than 2º C. According to the data of “Instituto del Mar Peruano”(IMARPE).All of these conditions had to be met at least for three consecutives months.On the basis of the above criteria, we have considered El Niño events:* The summer of 1992 (El Niño 1992).* The period between Winter 1997 and Autumn 1998 (El Niño 1997-98).* Winter and Spring of 2002 (El Niño 2002)The present analysis only shows the results for the event 1997-98 because they were moresignificant. The rest of seasons in the period 1991-2002 were considered as part of the normalconditions.With regard to the summer and autumn of 1997, in spite of being included in normal periods,they have also been analysed separately in search of possible indicators as precursors of “ElNiño” in the high altitude horizontal wind. We have called this period conditions pre-El Niño1997-98.4. Validity of the measurementsThe dependence of the measurements of vertical and horizontal winds as a function of heightwith this type of wind profiler has been proven by means of comparisons made by Christmasisland (2° N, 157° E) wind profiler, with the analysis of the NMC and the ECMWFinterpolated for Christmas island (Gage et al., 1988).Comparison data from Piura radar ST vs. data of NCEP-NCAR ReanalysisMaps of zonal, meridional and vertical wind have been made with velocities calculated forPiura according to data of Reanalysis (NCEP_NCAR) and those has been compared to thewinds measured by the Piura wind profiler. Both winds are in good agreement, particularlyfor the high altitudes. The best agreement is observed in the zonal component (results notshown here). However details and figures can be found in Flores et al. [2002](a) ZONAL WIND PIURA - WINTERNORMAL CONDITIONS (NC) - EL NIÑO 1992 - EL NIÑO 1997-98108(b) ZONAL WIND PIURA - SUMMERNORMAL CONDITIONS (NC) - EL NIÑO 1992 - EL NIÑO 1997-98108Height (Km)642Height (Km)6420-10.5 -8.5 -6.5 -4.5 -2.5 -0.5 1.5 3.50-10.5 -8.5 -6.5 -4.5 -2.5 -0.5 1.5 3.5u (m/s)u (m/s)1992 1997 1998 NC1992 1997 1998 NCFigure 2. Zonal wind for (a) Winter normal conditions (NC) and “El Niño” conditions, and (b)Summer normal conditions (NC) and “El Niño” conditions. NC are indicated by line with error bars.Values for normal conditions are obtained from the 1991-2000 base period seasonal means.328
5. Summary of results and concluding remarksBased on the diurnal analysis under normal conditions we have found that easterlywind prevails during the whole day at all altitudes. The biggest intensities of wind are givenbetween the 0600 and the 1800 hours. The meridional component, on the other hand, there issoutherly wind prevalence between 2 and 5 km during the day, reversing at night. At higheraltitudes (5-10 km) we have observed predominant southerly winds as well as a dailyvariability in the intensity of the wind. This variability can be due to the temperature gradientfrom north to south and the unequal heating between mountains and the Sechura desert. Thespecific causes of this effect will be left for future work.About seasonal analysis in lower troposphere, the meridional wind does not maintain apredominant direction throughout the year. During the winter and the spring the southerlywind dominates all day long. The northerly wind appears only few hours in the afternoon. Onthe other hand, in the summer and autumn, the northerly wind prevails. In the middletroposphere the northerly winds dominates during all seasons and it is maximum at noon. It isnecessary to point out that both the zonal and meridional winds reached their maximumvalues in the winterDuring El Niño 1997-98, in their initial stage we have observed a significant decreaseof easterly wind above 4 km compared to normal periods (see Figure 2a). However, in theirmature and final phase at the same heights we observe a notable increase of the easterly windas height increases. On the other hand, there is an increase in the northerly wind above 4 kmDuring the event 1997-98 in the middle levels the larger differences were observed inintensities of wind along the day, however at lower heights there were significant dailychanges: Reinforcement of the east wind around 0200 and 1000 hours during the mature stageof the event and increasing the variability of meridional wind (approximately 1.5 times more)during the initial stage.We have detected possible precursors of El Niño in the behaviour of the troposphericwind. In the zonal wind there is a strong decrease of the east wind above 4 km., six monthsbefore and during initial stage of "El Niño 1997-98" (Fig. 2b). In addition, there is asignificant decrease of the northerly wind in the meridional wind between 2 and 10 km, butonly during the previous six months to the event 1997-98.More details and figures can be found in Flores et al. [2002]ReferencesFlores L. A., La Madrid J., Chau J. L., Vientos troposféricos observados con el radar VHF enPiura-Perú: condiciones normales versus “El Niño 1997-1998”, Rev. Geof. IPGH, 57, 81-110, 2002.Gage K. S., Balsley B. B., Ecklund W.L., Woodman R. F. and Avery S. K. , Wind-Profilrelatedresearch in the tropical Pacific, J.Geophys. Res., 96(Suplement), 13209-3220, 1991.Gage K. S., McAfee J. R., Colins W. G., Soderman D., Bottger H., Radford A. and Balsley B.B., A comparison of winds observed at Christmas Island using a wind-profiler Dopplerradars with NMC and ECMWF analyses, Bull. Am. Meteorol. Soc., 69, 1041-1046, 1988.Judas T. J., Ecklund W. L. And Balsley B. B., The coaxial collinear antenna. Currentdistribution from the cylindrical antenna equation, IEEE Trans. Antennas Propag., 35,327-331, 1987.Nastrom G. D., Clarck W. L., Vanzandt T. E. And Warnock J. M., Seasonal and diurnalchanges in wind variability from Flatland VHF profiler observations, Beitr. Phys.Atmosph., 69(1), 5-12, 1996.Ragaini E., Rodriguez R., Migioramento del progetto di ricerca sull’ indagine troposfericanella regione di Piura, L’ELETTROTENICA, 79(9), 863-869, 1992.Reynolds R. W. and Smith T. S., A high resolution global sea surface temperatureclimatology, J. Climate, 8, 1571-1538, 1995329
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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
Page 283 and 284: Fig. 5 Passage of typhoon Hayan on
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Page 289 and 290: the time-height section of a convec
Page 291 and 292: Thurai, M., T.Iguchi,T. Kozu, J.D.E
Page 293 and 294: There are two main mechanisms which
Page 295 and 296: Horel, J.D. and Cornejo-Garrido, A.
Page 297 and 298: estimating two independent and redu
Page 299 and 300: RASS THETA (K) RASS v-component (m/
Page 301 and 302: Surface winds usually range from 10
Page 303 and 304: weak (maximum of 5 m s -1 ) and the
Page 305 and 306: The vertical component from the VTB
Page 307 and 308: Figure 8 shows the profile of virtu
Page 309 and 310: 2 3D ( , ) ( ) ( ) ˆ ( ) ˆp∆ xm
Page 311 and 312: presented in Praskovsky et al. (200
Page 313 and 314: In Fig. 2 a sketch of a mountain le
Page 315 and 316: In Fig. 8 the lamina is aligned on
Page 317 and 318: Figure 1: composite day (13 days) o
Page 319 and 320: virtual sensible heat fluxes ( Wm-2
Page 321 and 322: 3. Characteristics of precipitation
Page 323 and 324: Fig. 3: Horizontal distribution of
Page 325 and 326: 3. Results and discussionUHF profil
Page 327 and 328: Figure 4. Monthly variation of slop
Page 329 and 330: system with two receiving antennae,
Page 331 and 332: cycle of precipitation. Figure 3(a)
Page 333: Histogram of Zonal Velocityh=5.13 K
Page 337 and 338: the two nearby major cities, Chenna
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
Page 349 and 350: The purpose of this study is to exa
Page 351 and 352: Figure1. Three-day average of momen
Page 353 and 354: 3. The improved method to estimate
Page 355 and 356: But in case of period until 1800 UT
Page 357 and 358: Session I.5: Operational Aspects an
Page 359 and 360: The profilers of WINDAS weredesigne
Page 361 and 362: 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
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esulting in a widening of the bandw
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ON THE RADIATION EFFICIENCY OF COCO
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Table 2: Experiment #1 results, Tra
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A NEW NARROW BEAM MF RADAR AT 3 MHZ
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Off-zenith beams towards N, S, E, W
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95ALWIN VHF radar: signal powerdB80
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ANTENNA BEAM VERIFICATION USING COS
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Figure 2: A 45 MHz reference sky te
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AN ATTEMPT TO CALIBRATE THE UHF STR
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is at 4.7 km, but in the first 4-ga
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QUALITY CONTROL FOR DOPPLER WIND PR
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The resulting moments are subjected
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SOUSY RADAR AT JICAMARCA: SYSTEM DE
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NEControl andcomputer roomCompCoute
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THE EQUATORIAL ATMOSPHERE RADAR:SYS
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Table 1: Specifications of the EAR
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VHF ATMOSPHERIC AND METEOR RADAR IN
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ased upon a geotechnical engineerin
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VORTICAL MOTIONS OBSERVED WITH THE
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interpolation from the original gri
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A NEW MINIRADAR TO INVESTIGATE URBA
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e eliminated to analyze correctly t
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Session PWG 1: System Calibrations
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Session PWG 2: Data Analysis, Valid
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• the time series vectors x(k) of
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Fig. 4: reflectivity of the hydrome
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Session PWG 3: Accuracies and Requi
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Session PWG 4: International Collab
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Session II.E: NOVEL PERSPECTIVES AN
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2 Proposed AlgorithmReceived signal
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N#4E-1-16E1A1#1#2A-1-1C1#3C-1-19Fig
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of conventional DCMP, with which th
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applying the directional constraint
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while for a beam of finite width, t
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In order to make the process more q
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WHAT IS TURBULENCE SEEN BY VHF RADA
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Enhanced resolution applyingpulse s
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Beckmann, Spizichino, 1964Fig. 8 Po
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Fig. 11 Plots of temporal variation
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Fig. 14 Distributions of phase cent
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Hocking, W.K., Radar studies of sma
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THE STRUCTURE FUNCTION-BASED APPROA
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{ Ui( t), Vi( t), Wi( t)} = { Ui ,
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161). Assumption 2H: the instantane
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Only the second order SF are consid
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fluctuations umk( t ) along the bas
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VHF PARASITIC RADAR INTERFEROMETRYF
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• All the costs of transmitter pr
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Figure 2: Example of range-azimuth
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Target Altitude, km1009080706050403
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ReferencesGriffiths, H. D., A. J. G
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Participants ListAvery, James P.Uni
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Hysell, David L.EAS/Cornell Univers
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Silva, Robert R.ATRADAustraliarsilv
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AAdachi, A. .......................
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TTabary, P. .......................
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