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RAIN DROP SIZE DISTRIBUTION OVER GADANKI, INDIA DURINGSOUTHWEST AND NORTHEAST MONSOONK.Krishna Reddy 1 , Toshiaki Kozu 2 , T.Narayana Rao 3 , Kenji Nakamura 3 and D.Narayana Rao 41Frontier Observational Research System for Global Change, 3173-25 Showa-machiKanazawa-ku, Yokohama, Kanagawa 236-0001, Japan2Interdisciplinary Faculty of Science and Engineering, Shimane University, 1060 Nishi-kawatsu, Matsue,Shimane 690-8504, Japan3Hydrospheric-Atmospheric Research Center, Nagoya University, Furocho, Chikusaku, Nagoya 464-8601,Japan4 National MST Radar Facility, P.O.Box. 123, Tirupati – 517502, India1. IntroductionMonsoons are the most complicated yet interesting phenomena as it is associated withrain in large areas and can affect 60% of population leaving under its influence. Further, itplays a significant role in modulating global climate. Among these, Indian summer monsoon(or south-west (SW) monsoon) is the most significant one. Numerous reports are available inliterature on the dynamics of the monsoon system (monsoons, 1987 and references therein).Though, the principal rainy season for Indian subcontinent as a whole is the summermonsoon, some parts of India, particularly east coast of south peninsula, gets about 50% ormore of the annual rainfall in post monoon season (so called north-east (NE) monsoon). Thegeneral features of these monsoon systems, mainly large-scale features, are well known andare well documented (please visit IMD website, www.imd.ernet.in). For instance, the onsetof monsoon (1 May for SW monsoon and 20 October for NE monsoon with a deviation of aweak on either side), the seasonal rainfall and the diurnal variation of rainfall. However,much is not known about the differences in the microphysics of cloud systems [for ex, thedrop size distribution (DSD)] in these seasons. It is due mainly to lack of suitablemeasurements at these locations. Recently a UHF wind profiler and disdrometer has beeninstalled at Gadanki (13.5 N, 79.2 E), India under Indo-Japanese colloboration program. Itenabled us to study the differences in the microphysics of the cloud systems in SW and NEmonsoon seasons. It forms the crux of the present paper.3182. Data and InstrumentationThe Lower Atmospheric Wind Profiler (LAWP) operates at a frequency of 1.3 GHz islocated at Gadanki, about 120 km from Chennai and about 80 km from the coast, in southernIndia. It has been installed in August 1997 and since then operating continuously byproviding wind and reflectivity information with a good height and time resolution. The datacollected between October 1997 and September 2000 has been used for the present study.Complete description of LAWP and initial results can be found in Reddy et al. (2001). Thedisdrometer used in the present study is of impact type, originally developed by Joss andWaldvogel (1969). It is located close to LAWP and provides the DSD at 1 min. intervals.Important rain parameters are derived from the available DSD using standard momentsmethod. The present disdrometer data has been successfully evaluated by comparing with thenearby Optical Rain Gauge products (Reddy et al., 2003). Disdrometer has been operatingcontinuously since September 1997, except for few months in 1998 due to malfunctioning ofthe instrument. For the present study, the data collected between September 1997 andDecember 2001 are used. Further, seasons are divided as follows with the months May toSeptember comes under southwest monsoon season, while the northeast monsoon comprisingOctober, November and December months.
3. Results and discussionUHF profiler is an excellent instrumentation system for providing continuousmeasurements of wind as shown in Figure 1. It shows time series of wind velocity anddirection for over one year of observations starting from March 1999 to September 2000. Itclearly shows a shift in wind direction from northeasterly to southwesterly in May and againback to northeasterly in late September coinciding with the onset of southwest and northeastmonsoon systems. Another noted difference in the wind pattern between these seasons is themagnitude of wind. A strong Low Level Jet (LLJ) apparent at about 2 km with peakmagnitude reaching 20 m/s in southwest monsoon season is not seen in northeast monsoonseason.Figure 1. 5 day mean horizontal winds observed from March 1999 to September 2000.Figure 2. Monthly variation of (a) median volume diameter and (b) N 0 .319
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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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Page 281 and 282: Typhoon LekimaFig. 2 Typhoon Lekima
Page 283 and 284: Fig. 5 Passage of typhoon Hayan on
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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 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
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Page 307 and 308: Figure 8 shows the profile of virtu
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Page 313 and 314: In Fig. 2 a sketch of a mountain le
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Page 317 and 318: Figure 1: composite day (13 days) o
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Page 321 and 322: 3. Characteristics of precipitation
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Page 333 and 334: Histogram of Zonal Velocityh=5.13 K
Page 335 and 336: 5. Summary of results and concludin
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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
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
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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 and 366: Figure 3. Pulse Design Diagram to s
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Page 371 and 372: TOWARD A MULTISENSOR GROUND BASED R
Page 373 and 374: 3. Cloud Evolution Case StudyOn the
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DEVELOPMENT OF A DIGITAL RECEIVER F
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Experiment 1 Experiment 2IPP 999Km
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ELECTRONIC DIGITAL BEAMFORMING IMPL
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The main element of the unit (figur
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.ON-LINE ADAPTIVE DC-GROUND-CLUTTER
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esulting in a widening of the bandw
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ON THE RADIATION EFFICIENCY OF COCO
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Table 2: Experiment #1 results, Tra
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A NEW NARROW BEAM MF RADAR AT 3 MHZ
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Off-zenith beams towards N, S, E, W
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95ALWIN VHF radar: signal powerdB80
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ANTENNA BEAM VERIFICATION USING COS
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Figure 2: A 45 MHz reference sky te
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AN ATTEMPT TO CALIBRATE THE UHF STR
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is at 4.7 km, but in the first 4-ga
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QUALITY CONTROL FOR DOPPLER WIND PR
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The resulting moments are subjected
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SOUSY RADAR AT JICAMARCA: SYSTEM DE
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NEControl andcomputer roomCompCoute
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THE EQUATORIAL ATMOSPHERE RADAR:SYS
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Table 1: Specifications of the EAR
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VHF ATMOSPHERIC AND METEOR RADAR IN
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ased upon a geotechnical engineerin
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VORTICAL MOTIONS OBSERVED WITH THE
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interpolation from the original gri
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A NEW MINIRADAR TO INVESTIGATE URBA
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e eliminated to analyze correctly t
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Session PWG 1: System Calibrations
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Session PWG 2: Data Analysis, Valid
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• the time series vectors x(k) of
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Fig. 4: reflectivity of the hydrome
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Session PWG 3: Accuracies and Requi
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Session PWG 4: International Collab
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Session II.E: NOVEL PERSPECTIVES AN
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2 Proposed AlgorithmReceived signal
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N#4E-1-16E1A1#1#2A-1-1C1#3C-1-19Fig
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of conventional DCMP, with which th
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applying the directional constraint
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while for a beam of finite width, t
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In order to make the process more q
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WHAT IS TURBULENCE SEEN BY VHF RADA
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Enhanced resolution applyingpulse s
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Beckmann, Spizichino, 1964Fig. 8 Po
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Fig. 11 Plots of temporal variation
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Fig. 14 Distributions of phase cent
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Hocking, W.K., Radar studies of sma
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THE STRUCTURE FUNCTION-BASED APPROA
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{ Ui( t), Vi( t), Wi( t)} = { Ui ,
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161). Assumption 2H: the instantane
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Only the second order SF are consid
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fluctuations umk( t ) along the bas
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VHF PARASITIC RADAR INTERFEROMETRYF
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• All the costs of transmitter pr
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Figure 2: Example of range-azimuth
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Target Altitude, km1009080706050403
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ReferencesGriffiths, H. D., A. J. G
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Participants ListAvery, James P.Uni
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Hysell, David L.EAS/Cornell Univers
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Silva, Robert R.ATRADAustraliarsilv
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AAdachi, A. .......................
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TTabary, P. .......................
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