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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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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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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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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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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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Alice K. DuVivier, John J. Cassano, Steven Greco, and G. David Emmitt

the DAWN lidar, dropsonde, and satellite observations of the barrier wind observed on 21 May 2015 from approximately 1900 to 2200 UTC. Our focus is to use these observations to evaluate how well high-resolution regional simulations with the Weather Research and Forecasting (WRF) Model can reproduce the observed features with different horizontal and vertical resolutions and with two different boundary layer parameterizations. As such, we will not focus on diagnosing the dynamics that create the

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Andreas Schäfler, Ben Harvey, John Methven, James D. Doyle, Stephan Rahm, Oliver Reitebuch, Fabian Weiler, and Benjamin Witschas

their influence on high-impact weather downstream ( Schäfler et al. 2018 ). For the first time, an established Doppler wind lidar payload on board the research aircraft DLR Falcon performed dedicated observations of the jet stream winds providing both high vertical and horizontal resolution, which is not available from other observational sources. Additionally, the wind lidar dataset is supplemented by dropsonde and ground-based wind profiler observations to provide a wider coverage and to

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