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Satellite (TIROS-N) Operational Vertical Sounder (TOVS) spaceborne instruments, and from a couple of ground lidars in France. Also, high-cloud optical thicknesses from GLAS are compared similarly from a number of worldwide multiyear ground-based lidar datasets. The second motivation comes from the fact that high clouds strongly affect the performances of any airborne electro-optical sensor for limb-viewing observations. Chervet and Roblin (2006) have developed a model to determine the performance
Satellite (TIROS-N) Operational Vertical Sounder (TOVS) spaceborne instruments, and from a couple of ground lidars in France. Also, high-cloud optical thicknesses from GLAS are compared similarly from a number of worldwide multiyear ground-based lidar datasets. The second motivation comes from the fact that high clouds strongly affect the performances of any airborne electro-optical sensor for limb-viewing observations. Chervet and Roblin (2006) have developed a model to determine the performance
uncertainty and contributes up to 70% of the total error. In addition, those errors can be horizontally correlated over several hundred kilometers ( Bormann et al. 2003 ). As a consequence, AMVs are usually thinned rigorously for the assimilation in NWP models. Spaceborne lidars such as the one on the Cloud–Aerosol Lidar and Infrared Pathfinder Satellite Observations ( CALIPSO ) satellite can accurately determine the height of cloud tops. Therefore, the combination of AMVs with cloud-top information
uncertainty and contributes up to 70% of the total error. In addition, those errors can be horizontally correlated over several hundred kilometers ( Bormann et al. 2003 ). As a consequence, AMVs are usually thinned rigorously for the assimilation in NWP models. Spaceborne lidars such as the one on the Cloud–Aerosol Lidar and Infrared Pathfinder Satellite Observations ( CALIPSO ) satellite can accurately determine the height of cloud tops. Therefore, the combination of AMVs with cloud-top information
assimilation in NWP models and only a small fraction of the available observations is used. Preceding studies ( Velden and Bedka 2009 ; Weissmann et al. 2013 ) demonstrated that AMVs actually represent the wind in a vertically extended layer, although they are traditionally assimilated at discrete levels. In addition, Weissmann et al. (2013) showed that the height of AMVs can be corrected using airborne lidar cloud-top observations. The study presented here further investigates these two approaches that
assimilation in NWP models and only a small fraction of the available observations is used. Preceding studies ( Velden and Bedka 2009 ; Weissmann et al. 2013 ) demonstrated that AMVs actually represent the wind in a vertically extended layer, although they are traditionally assimilated at discrete levels. In addition, Weissmann et al. (2013) showed that the height of AMVs can be corrected using airborne lidar cloud-top observations. The study presented here further investigates these two approaches that
observations at Cabauw in the Netherlands. Sodar data have also been used to determine the occurrence and characteristics of LLJs—for example, in Florida ( Karipot et al. 2009 ) and in Moscow ( Kallistratova and Kouznetsov 2012 ). High-resolution Doppler lidar has proven to be an ideal instrument to measure vertical wind profiles ( Banta et al. 2002 , 2013 ), and Doppler lidar systems have even been deployed on ships ( Tucker et al. 2010 ; Pichugina et al. 2012 ), enabling the investigation of LLJs in
observations at Cabauw in the Netherlands. Sodar data have also been used to determine the occurrence and characteristics of LLJs—for example, in Florida ( Karipot et al. 2009 ) and in Moscow ( Kallistratova and Kouznetsov 2012 ). High-resolution Doppler lidar has proven to be an ideal instrument to measure vertical wind profiles ( Banta et al. 2002 , 2013 ), and Doppler lidar systems have even been deployed on ships ( Tucker et al. 2010 ; Pichugina et al. 2012 ), enabling the investigation of LLJs in
data relies on the subjective observation of the researchers, which can be a remarkably time-consuming process for a large dataset and furthermore it is substantially difficult to ensure consistency throughout the classification. We have developed an automated method with the aim to achieve consistent medium-to-large fluctuations and coherent structures (mlf-cs) classifications for single Doppler wind lidar observations ( Cheliotis et al. 2020 ). We focus on the streaks and rolls as presented by
data relies on the subjective observation of the researchers, which can be a remarkably time-consuming process for a large dataset and furthermore it is substantially difficult to ensure consistency throughout the classification. We have developed an automated method with the aim to achieve consistent medium-to-large fluctuations and coherent structures (mlf-cs) classifications for single Doppler wind lidar observations ( Cheliotis et al. 2020 ). We focus on the streaks and rolls as presented by
proven very useful in the understanding of atmospheric dynamics and structure. Shortly after the development of the first pulsed lasers, the applicability of lidar to the study of mountain-wave-related phenomena was recognized. Collis et al. (1968) were the first to document aerosol lidar observations in the Sierra Nevada in February and March 1967, followed by more comprehensive observations by Viezee et al. (1973) in March and April 1969 and 1970. These studies provided evidence that pulsed
proven very useful in the understanding of atmospheric dynamics and structure. Shortly after the development of the first pulsed lasers, the applicability of lidar to the study of mountain-wave-related phenomena was recognized. Collis et al. (1968) were the first to document aerosol lidar observations in the Sierra Nevada in February and March 1967, followed by more comprehensive observations by Viezee et al. (1973) in March and April 1969 and 1970. These studies provided evidence that pulsed
268 JOURNAL OF APPLIED METEOROLOGY VOLUM-29NOTES AND CORRESPONDENCEAirborne Lidar Observations during AGASP-2B. M. MORLEY, E. E. UTHE AND W. VlEZEESRI International, Menlo Park, California23 May 1989 and 23 September 1989 ABSTRACT Sample observations of the lower troposphere made by airborne lidar during the Arctic Gas and AerosolSampling Program-2 (AGASP-2) are shown for the area of
268 JOURNAL OF APPLIED METEOROLOGY VOLUM-29NOTES AND CORRESPONDENCEAirborne Lidar Observations during AGASP-2B. M. MORLEY, E. E. UTHE AND W. VlEZEESRI International, Menlo Park, California23 May 1989 and 23 September 1989 ABSTRACT Sample observations of the lower troposphere made by airborne lidar during the Arctic Gas and AerosolSampling Program-2 (AGASP-2) are shown for the area of
://www.arl.noaa.gov/HYSPLIT.php ; Draxler and Hess 2004 ). 2. Observations and data analysis methods The lidar was installed on the top of the Guangdong Environmental Protection Bureau building (23.134°N, 113.264°E, 50 m above sea level). The lidar instrument is similar to that reported in our previous papers ( Sugimoto et al. 2002 , 2006 ). It has three channels and measures the backscattering at 1064 and 532 nm and the depolarization at 532 nm. The depolarization ratio, which is a parameter sensitive to nonsphericity of the
://www.arl.noaa.gov/HYSPLIT.php ; Draxler and Hess 2004 ). 2. Observations and data analysis methods The lidar was installed on the top of the Guangdong Environmental Protection Bureau building (23.134°N, 113.264°E, 50 m above sea level). The lidar instrument is similar to that reported in our previous papers ( Sugimoto et al. 2002 , 2006 ). It has three channels and measures the backscattering at 1064 and 532 nm and the depolarization at 532 nm. The depolarization ratio, which is a parameter sensitive to nonsphericity of the
stability of the basin air mass have in the MHs derived from the lidar ceilometer. 1) Conceptual model and indices As the most simple framework in which we can analyze our observations of ML over the Santiago Basin, we consider the encroachment or thermodynamic model of convective boundary layer growth ( Stull 1988 , p. 454). In this case the growth of a CBL is estimated by a simple energy balance in which the only heat source of the CBL is the sensible heat flux at the surface. The integral of this
stability of the basin air mass have in the MHs derived from the lidar ceilometer. 1) Conceptual model and indices As the most simple framework in which we can analyze our observations of ML over the Santiago Basin, we consider the encroachment or thermodynamic model of convective boundary layer growth ( Stull 1988 , p. 454). In this case the growth of a CBL is estimated by a simple energy balance in which the only heat source of the CBL is the sensible heat flux at the surface. The integral of this
1306 JOURNAL OF APPLIED METEOROLOGY Vot, uMgl6Lidar Observations of the Convective Boundary LayerK. E. KUNKEL, E. W. ELORANTA AND S. T. SmVLE-Dep~rtnten~ of Meteorology, University of Wisconsin, Madison 53706(Manuscript received 16 May 1977, in revised form 20 September 1977) ABSTRACT A scanning lldar system has been used to observe convection in the atmospheric boundary layer
1306 JOURNAL OF APPLIED METEOROLOGY Vot, uMgl6Lidar Observations of the Convective Boundary LayerK. E. KUNKEL, E. W. ELORANTA AND S. T. SmVLE-Dep~rtnten~ of Meteorology, University of Wisconsin, Madison 53706(Manuscript received 16 May 1977, in revised form 20 September 1977) ABSTRACT A scanning lldar system has been used to observe convection in the atmospheric boundary layer
