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Reinout Boers, S. H. Melfi, and Stephen P. Palm

variations in lapserate above the PBL and sea surface temperature leavingall other parameters fixed. Lapse rate changes with thesynoptic time scale, which is larger than 2 h, while a50-km change in initial position only produces littlechange in trajectory distance and sea surface temperature along the trajectory, so that the effect on themodel calculations is small.4. Observations and calculationsa. Introduction In this section the observations and calculations willbe presented. To simulate the lidar

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Shane D. Mayor

observations presented here are unique because 1) they include both in situ and scanning lidar data, 2) the lidar images reveal the microscale structure and motion of the fronts on horizontal and vertical cross sections, and 3) the dataset contains 7 fronts out of the nearly-continuous 77 days of data available. The Raman-shifted Eye-safe Aerosol lidar (REAL; Mayor et al. 2007 ) was deployed in Dixon, California, between 15 March and 11 June 2007 as an appendix to the Canopy Horizontal Array Turbulence

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James D. Spinhirne and William D. Hart

NOVEMBER 1990 JAMES D. SPINHIRNE AND WILLIAM D. HART 2329Cirrus Structure and Radiative Parameters from Airborne Lidar and Spectral Radiometer Observations: The 28 October 1986 FIRE Study JAMES D. $PINHIRNENASA Goddard Space Flight Center, Laboratory for Atmospheres, Greenbelt, Maryland WILLIAM D. HARTScience Systems Applications, Inc., Lanham, Maryland(Manuscript received

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C. M. R. Platt, David W. Reynolds, and N. L. Abshire

F-BRUAR-1980 C. M. R. PLATT, DAVID W. REYNOLDS AND N. L. ABSHIRE 195Satellite and Lidar Observations of the Albedo, Emittance and Optical Depth of Cirrus Compared to Model Calculations C. M. R. PLATTCS1RO Division of Atmospheric Physics, Aspendale, Victoria, Australia, 3195 DAVID W. REYNOLDSDepartment of Atmospheric Sciences, Colorado State University, Fort Collins 80,523 N. L

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Robert J. Conzemius and Evgeni Fedorovich

for comparing the observed evolution of the sheared atmospheric CBL with large-eddy simulation (LES; Moeng and Sullivan 1994 ; Pino et al. 2003 ; Conzemius and Fedorovich 2006a ). The primary goals of the study are twofold. First, we intend to evaluate LES predictions of the sheared CBL growth against lidar observations of CBL depth evolution and compare LES output with radiometer, radar, and radiosonde data to more fully understand the evolution of the mean wind and temperature in the CBL

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Lei Zhang and Zhaoxia Pu

of convective initiations and evolutions. Specifically, results from Wulfmeyer et al. (2006) indicated that the assimilation of water vapor differential absorption lidar data improves the simulation of the structures of the moisture field of a convective system. Although the importance of the high-resolution moisture information in the analysis and simulation of MCS has been well recognized and addressed, and the influence of wind observations, especially the winds in the boundary layers to

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Matt C. Wilbanks, Sandra E. Yuter, Simon P. de Szoeke, W. Alan Brewer, Matthew A. Miller, Andrew M. Hall, and Casey D. Burleyson

stratocumulus deck. The frontal zone slants backward with height up to the maximum depth of the flow (≈400 m). Behind the head, the height of the main flow levels off and gradually descends. Consistent with lidar observations, some of the clouds behind and along the frontal zone are very low lying (<400 m). The wind profile inside the density current is shown at B in Fig. 16 . Surface layer shear is present in the lowest ≈200 m of the main density current flow. The right-bound return flow ( Simpson 1997

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Lindsay J. Bennett, Tammy M. Weckwerth, Alan M. Blyth, Bart Geerts, Qun Miao, and Yvette P. Richardson

studies showing horizontal maps of the moisture in the CBL from an airborne water vapor lidar. The structure of the paper is as follows. The layout and description of instrumentation are described in section 2 and the general meteorological situation in section 3 . Observations of the evolution of the early morning boundary layer are presented in section 4 , the development of the convective boundary layer in section 5 , and the characteristics of the open cells in section 6 . A summary of the

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Paul J. Neiman, R. M. Hardesty, M. A. Shapiro, and R. E. Cupp

NOVEMBER 1988 NEIMAN ET AL. 2265Doppler Lidar Observations of a Downslope Windstorm PAUL J. NEIMANCooperative Institute for Research in the Environmental Sciences, University of Colorado/NOAA, Boulder, ColoradoR. M. HARDESTY, M. A. SHAPIRO AND R. E. CUPPNOAA/ERL / Wave Propagation Laboratory, Boulder, Colorado(Manuscript received 12 February 1988, in final form 5 May 1988

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Benjamin A. Toms, Jessica M. Tomaszewski, David D. Turner, and Steven E. Koch

the high spatiotemporal resolution of Oklahoma Mesonet surface observations in concert with vertical profiling observations from two Atmospheric Emitted Radiance Interferometers (AERI) and a Doppler wind lidar (DWL) to provide details on the four-dimensional evolution of a bore-soliton wave complex. Prior to discussing the wave complex, we provide details of the utilized instruments in section 2 . The prewave environment is discussed using both atmospheric profiles and synoptic weather analyses

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