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E. Kassianov, M. Pekour, C. Flynn, L. K. Berg, J. Beranek, A. Zelenyuk, C. Zhao, L. R. Leung, P. L. Ma, L. Riihimaki, J. D. Fast, J. Barnard, A. G. Hallar, I. B. McCubbin, E. W. Eloranta, A. McComiskey, and P. J. Rasch

al. 1998 ) and the Interagency Monitoring of Protected Visual Environments (IMPROVE; ; Malm et al. 1994 ) networks, while the combined satellite observations featured AOD from the Moderate Resolution Imaging Spectroradiometer (MODIS) aboard the NASA’s Terra satellite ( Levy et al. 2013 ) and aerosol extinction profiles from the Cloud–Aerosol Lidar with Orthogonal Polarization (CALIOP) lidar on board the Cloud–Aerosol Lidar and Infrared Pathfinder

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D. I. Cooper, W. E. Eichinger, S. Barr, W. Cottingame, M. V. Hynes, C. F. Keller, C. F. Lebeda, and D. A. Poling

was placed in front ofthe APD to block out visible solar background radiationfor day and night operation. APD analog signals weredigitized at 100 MHz, resulting in an inherent minimumrange resolution of 1.5 m. No attempt was made tostabilize the system for ship movement, making detailed observations problematic within the boundarylayer except in the calmest seas.3. Observational procedure The Raman and elastic backscatter lidars col!ectedwater vapor mixing ratio and relative aerosol

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Q. S. He, C. C. Li, J. Z. Ma, H. Q. Wang, G. M. Shi, Z. R. Liang, Q. Luan, F. H. Geng, and X. W. Zhou

; Comstock et al. 2002 ; Pace et al. 2003 ; Sunilkumar and Parameswaran 2005 ). Over the Tibetan Plateau, however, vertically and temporally resolved measurements of cirrus cloud properties are still scarce, whereas the cloud-top and tropopause relationships by Cloud–Aerosol Lidar and Infrared Pathfinder Satellite Observations ( CALIPSO ; ) ( Pan and Munchak 2011 ) and case study of cirrus cloud properties by balloon ( Tobo et al. 2007 ) has been reported recently

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G. S. Kent and M. T. Philip

1358 JOURNAL OF THE ATMOSPHERIC SCIENCES VOLUME 37Lidar Observations of Dust from the Soufri&e Volcanic Eruptions of April 1979 G. S. KENT' AND M. T. PHILIPDepartment of Physics, University of the West Indies, Kingston, Jamaica(Manuscript received 12 October 1979, in final form 29 January 1980)ABSTRACTLidar observations of the stratosphere were made at Kingston, Jamaica (18.O"N, 76.8%') followingthe eruptions of the Soufritre volcano of St. Vincent (13.2"N, 61.2"W) between 13

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Chester S. Gardner, Marcus S. Miller, and C. H. Liu

1838 JOURNAL OF THE ATMOSPHERIC SCIENCES VOL. 46, NO. 12 Rayleigh Lidar Observations of Gravity Wave Activity in the Upper Stratosphere at Urbana, Illinois CHESTER S. GARDNER, MARCUS S. MILLER AND C. H. LIUDepartment of Electrical d Computer Engineering, University of Illinois at Urbana-Champaign, Urbana, Illinois(Manuscript received 2 March 1988, in final form 25 January 1989) During 13 nights

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Volker Wulfmeyer, Shravan Kumar Muppa, Andreas Behrendt, Eva Hammann, Florian Späth, Zbigniew Sorbjan, David D. Turner, and R. Michael Hardesty

different meteorological conditions, both at the surface and throughout the mixed layer (ML) and the EL. The observations should provide not only measurements of profiles and gradients of atmospheric variables but also their turbulent fluctuations. Reaching the CBL top is possible with aircraft in situ or remote sensing instrumentation as well as ground-based, vertically steering, or scanning lidar or clear-air radar systems. Unfortunately, dedicated observations for studying LES and TPs are relatively

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Tobias Selz, Lucas Fischer, and George C. Craig

, however, the values differ significantly, showing a much smaller intermittency and higher H and exponents in the observational data. Partly these differences can be explained by observational limitations and will be discussed in the following section. b. Sensitivity to observational limitations In this section, we use the numerical simulation as a surrogate data source to address the impact of three intrinsic limitations of lidar observations on the structure function analysis: the domain size

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Lukas Strauss, Stefano Serafin, and Vanda Grubišić

at elevation angles ranging from 3° to 60° (PPI-03–PPI-60). Lidar-measured fields included the aerosol backscatter intensity, radial Doppler velocity, and Doppler spectral width. In addition to the observational datasets, 700-hPa analyses from the European Centre for Medium-Range Weather Forecasts (ECMWF) Integrated Forecast System (IFS) are used here to provide the context of the large-scale synoptic flow. 3. Observations The main objective of this work is to reexamine the conceptual model of a

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J. M. Intrieri, A. J. Bedard Jr., and R. M. Hardesty

nondimensional ratio ofinertial to gravitational forces.a. Meteorological observations for case 1 On 4 August 1986 a small thunderstorm line, 15 kmwest of the lidar, produced an outflow boundary thatpropagated at 7 m s-j toward the Mesogamma 86 site.This outflow collided with another boundary that originated in a thunderstorm cell 25 km to the east. Thecollision occurred at 2310 UTC just west of the towerand was scanned by the lidar in Range Height Indicator(RHI) mode along the line labeled AB in Fig. l a

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William L. Smith, Xia Lin Ma, Steven A. Ackerman, H. E. Revercomb, and R. O. Knuteson

in the range of 500-1667 cm-I (20-6um) with a resolution of 1 cm-~ apodized. A more detailed discussion of the ground-based HIS M 120 instrument is given by Knuteson et al. ( 1991 ). In this study, cloud-base and cloud-top altitudes wereassigned from lidar observations made simultaneouslywith the HIS spectra. In the case of the NASA ER~2based observations, the lidar measurements of Spinhirne et al. (1988) were used. A description of the cloudaerosol lidar and its applications can be found in

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