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of the morning transition and the proper conditions for the onset and development of an upslope flow, we investigated the energetics of the flow evaluating the surface energy balance (SEB) as Q ˙ = R n − G − H − L E , where Q ˙ is the total heat storage in the surface layer, R n is the net all-wave surface irradiance, G is the ground heat flux, H is the sensible heat flux, and LE is the latent heat flux. A specific postprocessing treatment was applied to the tethered-balloon data. An
of the morning transition and the proper conditions for the onset and development of an upslope flow, we investigated the energetics of the flow evaluating the surface energy balance (SEB) as Q ˙ = R n − G − H − L E , where Q ˙ is the total heat storage in the surface layer, R n is the net all-wave surface irradiance, G is the ground heat flux, H is the sensible heat flux, and LE is the latent heat flux. A specific postprocessing treatment was applied to the tethered-balloon data. An
1. Introduction The low-level jet (LLJ) is a strong and narrow airstream typically observed within the planetary boundary layer (PBL) ( Stull 1988 ). The LLJ wind speed profile usually takes the shape of a nose, namely, a maximum with a fast decay of the wind speed with height both below and above it. Deviations from this “canonical” shape have been observed in the literature, consisting of wind speed profiles with two noses simultaneously observed along the vertical. These “atypical” LLJs will
1. Introduction The low-level jet (LLJ) is a strong and narrow airstream typically observed within the planetary boundary layer (PBL) ( Stull 1988 ). The LLJ wind speed profile usually takes the shape of a nose, namely, a maximum with a fast decay of the wind speed with height both below and above it. Deviations from this “canonical” shape have been observed in the literature, consisting of wind speed profiles with two noses simultaneously observed along the vertical. These “atypical” LLJs will
CAP strength and depth can occur because of synoptic and mesoscale influences ( Steinacker et al. 2007 ). Numerous mechanisms for CAP displacement have been advanced in the literature. The strong stratification observed in CAPs permits the development of wave motions such as internal gravity waves ( Lareau and Horel 2015b ) or solitary waves ( Cheung and Little 1990 ) that can produce temperature and wind variations at the surface. These wave motions can be induced by flow collisions ( Lin et al
CAP strength and depth can occur because of synoptic and mesoscale influences ( Steinacker et al. 2007 ). Numerous mechanisms for CAP displacement have been advanced in the literature. The strong stratification observed in CAPs permits the development of wave motions such as internal gravity waves ( Lareau and Horel 2015b ) or solitary waves ( Cheung and Little 1990 ) that can produce temperature and wind variations at the surface. These wave motions can be induced by flow collisions ( Lin et al
. Greco , 2012 : Airborne Doppler lidar of valley flows in complex coastal terrain . J. Appl. Meteor. Climatol. , 51 , 1558 – 1574 , doi: 10.1175/JAMC-D-10-05034.1 . Doran , J. C. , J. D. Fast , and J. Horel , 2002 : The VTMX 2000 campaign . Bull. Amer. Meteor. Soc. , 83 , 537 – 551 , doi: 10.1175/1520-0477(2002)083<0537:TVC>2.3.CO;2 . Eaton , F. D. , S. A. McLaughlin , and J. R. Hines , 1995 : A new frequency-modulated continuous wave radar for studying planetary boundary
. Greco , 2012 : Airborne Doppler lidar of valley flows in complex coastal terrain . J. Appl. Meteor. Climatol. , 51 , 1558 – 1574 , doi: 10.1175/JAMC-D-10-05034.1 . Doran , J. C. , J. D. Fast , and J. Horel , 2002 : The VTMX 2000 campaign . Bull. Amer. Meteor. Soc. , 83 , 537 – 551 , doi: 10.1175/1520-0477(2002)083<0537:TVC>2.3.CO;2 . Eaton , F. D. , S. A. McLaughlin , and J. R. Hines , 1995 : A new frequency-modulated continuous wave radar for studying planetary boundary
