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C. R. Dickson and J. K. Angell

993statistics. Hopefully, such an experiment can bemounted in the future. REFERENCESAngell, J. K., 1964: Use of tetroons to investigate the kinematics and dynamics of the planetary boundary layer. Mon. Wea. Rev., 92, 465-470.---~ D. H. Pack, G. C. Holzworth and C. R. Dickson, 1966: Tetroon trajectories in an urban atmosphere. J. Appl. Meteor., 5, 565-572. and C. R. Dickson, 1968: A Lagrangian study of helical circulations in the planetary boundary layer. J. Atmos. Sc

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Niels E. Busch, Simon W. Chang, and Richard A. Anthes

from the Great PlainsExperiment.1. Introduction The major sink of momentum and sources of heatand moisture are at the earth-atmosphere interface.The vertical fluxes of momentum, heat and moistureare therefore usually largest in the planetary boundarylayer (PBL), and considerable effort has been directedtoward the understanding of this relatively thin layernext to the earth's surface. Many PBL models of varying complexity have been developed with the purposeof studying the details of the physical

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C. H. Liu and D. Y. C. Leung

Introduction Dispersion of passive contaminants in the atmospheric boundary layer is a controversial issue in air pollution studies because of its complexity and the important consequences it may bring to our environment. The transport phenomenon of contaminants in the atmosphere, which is a function of the source conditions, meteorological parameters, geographical locations, etc., is difficult to predict accurately. Atmospheric boundary layer simulation models are essential tools to analyze

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Pamela E. Mlynczak, G. Louis Smith, Anne C. Wilber, and Paul W. Stackhouse

or LWD over most of the earth, implying that the LWU and LWD maps must resemble each other closely. The annual-average LWN is negative over the entire planet; that is, it represents cooling. During winter night of polar regions where the inversion forms, LWN becomes positive—that is, the atmosphere heats the surface radiatively, but the average over the year is still negative. The low LWN over ocean indicates that the surface and lower troposphere are closely coupled by planetary boundary layer

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A. Ghazi and J. J. Becker

network. Ann. Geophys., 25, 293-299.Chandrasekhar, S., 1950: Radiative Transfer. Clarendon Press, Oxford, 393 pp.Coulson, K. L., J. V. Dave and Z. Sekera, 1960: Tables Related to Radiation Emerging From a Planetary Atomospher- with Raylelgh Scattering. University of California Press, 548 pp.Dave, J. V., and P. M. Furukawa, 1966: Scattered radiation in the ozone absorption bands at selected levels of a terrestrial Rayleigh atmosphere. Meteor. Monogr., 7, No. 29, 233 pp.Dobson, G. M. B., 1957

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Alfredo Peña, Sven-Erik Gryning, Jakob Mann, and Charlotte B. Hasager

. , 2006 : Comments on “The neutral, barotropic planetary boundary layer, capped by a low-level jet inversion”. Bound.-Layer Meteor. , 119 , 171 – 179 . Blackadar , A. K. , 1962 : The vertical distribution of wind and turbulent exchange in a neutral atmosphere. J. Geophys. Res. , 67 , 3095 – 3102 . Blackadar , A. K. , 1965 : A single-layer theory of the vertical distribution of wind in a baroclinic neutral atmospheric boundary layer. Flux of Heat and Momentum in the Planetary Boundary

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Congbin Fu and Joseph O. Fletcher

During the northern summer the Tibetan Plateau is a heat source for the atmosphere, and the EquatorialPacific Ocean Cold Tongue is a heat sink, both contributing to the thermal forcing of large-scale quasi-zonalatmospheric circulation. For the period 1954-1979 interannual variability of Indian monsoon rainfall (IM) is found to correlatehighly with the thermal contrast between the Tibetan Plateau (TP) and the Equatorial Cold Tongue (ECT).An index of this thermal contrast (SLO for sea

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Charles R. Hosler and Thomas J. Lemmons

first 1.5-2.0 kmabove the surface, during fair weather conditions. Preliminary tests indicate that temperature profilesderived from the Thermasonde can provide usefu! information, particularly for air pollution meteorology, fordescribing dispersion characteristics within the planetary boundary layer. The evaluation of a preliminarydata reduction technique is described.1. Introduction A knowledge of the atmospheric thermal stabilityis useful to describe the dilution capacity of the atmosphere

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Toby N. Carlson and Peter Wendling

, 1975: Convective plumes in the planetary boundary layer, investigated with an acoustic echo sounder. ~r. AppL Meteor., 14, 513-523.Hooke, W. H., ]. M. Young and D. W. Beran, 1972: Atmospheric waves observed in the planetary boundary layer using an acoustic sounder and a microbarograph array. Boumt.-Lay~ Meteor., 2, 371-380.Little, C. G., 1969: Acoustic methods for the remote probing of the lower atmosphere. Proc. I--E, ~?, $71-578.McAliister, L. G., 1968: Acoustic sounding of the lower

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Joachim H. Joseph, Alexander Manes, and Dov Ashbel

aerosols on the average global albedo and surface temperature is also presented.1. Introduction Recently, the influence of aerosols on the thermalregime of a planetary atmosphere, both directly andby their effect on cloud properties, has become of muchinterest Ee.g., McCormick and Ludwig, 1967; Petersonand Bryson, 1968; Budyko, 1969; Bryson and Wendland, 1970; Galindo and Muhlia, 1970; Robinson, 1970;Man's Impact on the Global Environment (S.C.E.P.),1970; Study of Man's Impact on Climate (S

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