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The composites of the local circulation were made from hourly wind profiles from thePiura BLTR (Scipión et al. [this issue]). The synoptic scale circulation composites were madefrom daily averaged NCEP/NCAR Reanalysis data (Kalnay et al. [1996]). The composition ofhourly data was justified as long as the assumption that rainfall in this period had a diurnalvariation locked to the insolation cycle through the sea-breeze circulation mechanism wasdominant. This assumption was supported by the fact that the SST anomalies were moderatein this period and by the observed timing in the river discharge data.3. Results and discussion.The results suggest that, given the favorable SST conditions, specific days are favoredwith rainfall over others through an enhancement of onshore flow near the top of theboundary layer (approximately 1.5 km above the surface) in the morning (Fig. 4, left). A waythe enhanced onshore could favor rainfall is through an associated forced lifting of air parcelsup the western slope of the Andes, which could trigger convection. This forcing would bemore efficient when superimposed on the action of the sea-breeze circulation, which has beeninvoked previously as an important mechanism for the genesis and timing of the rainfall. It isinteresting to note that the meridional wind seems to have little relevance to the occurrence ofrainfall. This sheds new light on the statement by Eguiguren [1894], who said "...it is aconstantly observed fact that it doesn't rain in Piura but when winds blow more or lessstrongly from the northwest". Eguiguren [1894] considered the northerly component of thewind to have the greater relevance to rainfall but in our study we found that the mean windwas essentially from the south and that the westerly component was the most relevant for therain. It would appear that what is important is that the mean wind blows from the highmoisture and heat source, as Woodman [1999] suggested, and that it is through enhancementof the westerly flow that rainfall can be triggered. After the convective systems have formed,they will tend to modify the regional circulation. Above 1.5 km the westerly flow wasprogressively replaced by easterly flow starting near 1.5 km at around noon and extendingfurther up to around 5 km in the evening. We speculate that the progressively higher verticalextension of the westerly wind is due to convective transport of westerly momentum from theboundary layer into the mid-levels.In the period of study, the rainfall events on Piura tended to be clustered in time andthese clusters had a recurrence time of about 10 days. The onshore low-level flowenhancement seems to be related to synoptic scale tropical systems which have similar spatialscales to the 10-day zonal wind oscillations reported in previous works (Wallace and Chang[1969]). Our results also show systematic differences in the circulation associated to thesubtropical high, with an enhanced equatorward flow off the Peruvian coast in rainy days. Thespatial scale of the disturbance allows us to associate it to a planetary wave number 5. Sincethese waves also have a period on 10 days (Figueroa [1999]), it is unclear if their phasingwith the circulation changes over Piura is fortuitous or not. Similar studies of other years areneeded to address this.4. ReferencesBendix, J. and Bendix, A. Climatological aspects of the 1991/1993 El Niño in Ecuador. Bull.Inst. fr. études andines 27, 3, 655-666, 1998Eguiguren, D.V., Las lluvias en Piura. Bol. de la Soc. Geogr. de Lima, 1894.Figueroa, S.N., Estudo dos sistemas de circulação de verão sobre a América do sul e suassimulações com modelos numéricos. Doctoral thesis, INPE, Brasil, 1999.Goldberg, R.A., Tisnado, G. and Scofield, R.A., Characteristics of extreme rainfall events innorth-western Peru during the 1982-1983 El Niño period. J. Geoph. Res. 92, C14, 14225-14241, 1987.288
Horel, J.D. and Cornejo-Garrido, A.G., Convection along the coast of northern Peru during1983: Spatial and temporal variation of clouds and rainfall. Mon. Wea. Rev. 114, 2091-2105,1986.Kalnay and co-authors, The NCEP/NCAR 40-year Reanalysis Project. Bull. Amer. Meteor.Soc. 77, 437-471, 1996.Scipión, D., Chau, J. and Flores, L., First results of the Boundary Layer and TroposphericRadar System for ENSO. This issue.Wallace, J.M. and Chang, C.P., Spectrum analysis of large-scale wave disturbances in thetropics. J. Atmos. Sci. 26, 5, 1010-1025, 1969.Woodman, R., Modelo estadístico de pronóstico de las precipitaciones en la costa norte delPerú. El Fenómeno El Niño. Investigación para una prognosis. 1er encuentro deUniversidades del Pacífico Sur: Memoria 93-108. Piura- Perú, 1999.Figure 4: Diurnal evolution of zonal (left) and meridional wind (right) (m/s) in a) rainy days (top) and b)dry days (middle) and c) the difference between the two (bottom). Only differences that pass a Student ttest at the 95% level are shown. Time is given in UTC (= Local + 5 hours) and height is given in km. Plusand minus signs indicate patches of positive and negative values.289
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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
Page 243 and 244: The main recently assumed mechanism
Page 245 and 246: Figure 2. Statistics of numbers of
Page 247 and 248: LIDAR OBSERVATIONS OF MIDDLE ATMOSP
Page 249 and 250: latitudinal dependence of the seaso
Page 251 and 252: APPLICATION OF THE DUAL-BEAMWIDTH M
Page 253 and 254: Figure 2: Mean zonal and meridional
Page 255 and 256: JLKLLK/ILIL6II/G/II/G/LEODFLK/LO/DD
Page 257 and 258: The monthly diurnal mean of horizon
Page 259 and 260: Session I.4: Meteorological Phenome
Page 261 and 262: Integration of the VHF wind profile
Page 263 and 264: Figure 1 : Map of the Lago Maggiore
Page 265 and 266: precipitating clouds, the cyclonic
Page 267 and 268: Eyewall(a)(b)(c)(d)Fig. 3: Radius-h
Page 269 and 270: as low as 0.55. The Piura 50-MHz ra
Page 271 and 272: place features in the profile with
Page 273 and 274: • Period 1 (June 1-10): SCCs exis
Page 275 and 276: Sumatera occurs by stratiform cloud
Page 277 and 278: very interesting to note the double
Page 279 and 280: 20(a) Convective Region(b) Transiti
Page 281 and 282: Typhoon LekimaFig. 2 Typhoon Lekima
Page 283 and 284: Fig. 5 Passage of typhoon Hayan on
Page 285 and 286: the 50 cm 2 sensor head, enabling t
Page 287 and 288: 22 June 2000 23:22:23 - 23:24:20 at
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: There are two main mechanisms which
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 and 334: Histogram of Zonal Velocityh=5.13 K
Page 335 and 336: 5. Summary of results and concludin
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
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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
Page 467 and 468:
THE STRUCTURE FUNCTION-BASED APPROA
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{ Ui( t), Vi( t), Wi( t)} = { Ui ,
Page 471 and 472:
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
Page 477 and 478:
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. .......................
Page 495:
TTabary, P. .......................
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