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J. M. Austin

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J. M. Austin
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J. M. Austin

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J. M. Austin and Collaborators

The results of an empirical study of 500-mb patterns are presented. It is shown that the prediction of the 24-hr and 48-hr intensification or weakening of troughs and ridges can be aided by a consideration of upstream changes. Qualitative rules for the prediction of a 24-hr change in the speed of troughs and ridges are included. Finally a climatological summary is presented of intensification, weakening and speed of troughs and ridges.

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J. M. Austin and R. Shapiro

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The hypothesis is investigated that there is a physical difference between the development and motion components of a surface pressure change. Temperature changes indicate that deepening and filling are accompanied by high-level heating and cooling, respectively, while the motion part of pressure changes is associated with low-level temperature variations.

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H. G. Houghton and J. M. Austin

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H. G. Houghton and J. M. Austin

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Surface pressure changes can occur only when an accelerational field exists. The regularity of occurrence, the distribution, and the magnitudes of the accelerational fields found in the atmosphere have been determined from the available data. The most direct method used was to plot maps of the deviation of the observed wind from the geostrophic wind. Charts of the horizontal divergence, as determined from the observed winds, were prepared for several levels. Charts were also drawn of the non-geostrophic temperature changes, which are defined as the difference between the actual 12-hour temperature changes and the temperature changes which would result from geostrophic advection of the temperature field. It is shown that the magnitudes of the divergence and the non-geostrophic temperature changes are consistent with the observed deviations from the geostrophic wind. The errors of each method are investigated and it is concluded that they are not sufficient to affect the order of magnitude of the results. All of the charts exhibit definite patterns which show a considerable degree of correspondence with the weather conditions. It is concluded that accelerational fields regularly occur in the atmosphere which are one order of magnitude greater than cyclostrophic accelerations and accelerations due to the variation of the Coriolis parameter.

The equation for the pressure tendency is discussed with reference to the observational data. Since the total divergence in a vertical column is the relatively small difference between large divergences of opposite sign, the divergence integral in the tendency equation apparently cannot be evaluated from the data. Furthermore the sum of the divergence and advective integrals yield only the surface pressure tendency, which is already available. It does not appear that the divergence can be prognosticated as accurately as the pressure field. It is pointed out that the vertical velocities associated with a field of divergence may cause large pressure and temperature changes aloft with no surface pressure change. This shows that it is not possible to determine the regions responsible for surface pressure changes by considering the changes in the several layers. The influence of vertical stability on surface pressure changes was investigated statistically with indeterminate results.

A model of a cyclonic development based on the latent heat of condensation is discussed. It appears that this mechanism is incapable of explaining pressure changes of the magnitude commonly observed. A mechanism by which additional accelerations and pressure changes might result from the deformation of the field of mass by an initial accelerational field is presented. Sufficient evidence has not been accumulated to determine whether this mechanism operates in the atmosphere.

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J. B. Jensen, P. H. Austin, M. B. Baker, and A. M. Blyth

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The analysis of Paluch suggests that some cumuli contain cloudy air from only two sources: cloud base and cloud top. A framework is presented for the investigation of droplet spectral evolution in clouds composed of air from only these two sources. The key is the investigation of the dependence of droplet concentration N on the fraction of cloud base air F in a sample of cloudy air. This N-vs-F analysis is coupled with an investigation of droplet spectral parameters to infer the types and scales of entrainment and mixing events.

The technique is used in a case study of a small, nonprecipitating continental cumulus cloud which was sampled during the 1981 CCOPE project in eastern Montana. The mixing between cloudy and entrained air in this cloud often appears to occur without total removal of droplets, although there is evidence that total evaporation occurs in some regions with low liquid water content. The observed droplet spectra are compared with those calculated from an adiabatic parcel model. The spectral comparison and the results of the N-vs-F analysis support the hypothesis that cloudy and environmental air interact on fairly large scales with subsequent homogenization of the large-scale regions. This description is consistent with recent models of mixing in turbulent flows.

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P. H. Austin, M. B. Baker, A. M. Blyth, and J. B. Jensen

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We have analyzed small-scale fluctuations in microphysical, dynamical and thermodynamical parameters measured in two warm cumulus clouds during the Cooperative Convective Precipitation Experiment (CCOPE) project (1981) in light of predictions of several recent models. The measurements show the existence at all levels throughout the sampling period of two statistically distinct kinds of cloudy regions, termed “variable” and “steady,” often separated by transition zones of less than ten meters. There is some evidence for microphysical variability induced by local fluctuations in thermodynamic and dynamic parameters; however, the predominant variations are of a nature consistent with laboratory evidence suggesting that mixing is dominated by large structures. Entrainment appears to occur largely near cloud top but the data presented here do not permit identification of a mechanism for transport of the entrained air throughout the cloud.

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Gary R. Austin, Robert M. Rauber, Harry T. Ochs III, and L. J. Miller

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Two case studies of rainband evolution off the windward coast of the Big Island of Hawaii are presented along with an overview of the complete radar and satellite dataset from the Hawaiian Rainband Project conducted in the summer of 1990. These studies reveal that radar-observed rainbands and cells offshore of the windward coastline are nearly always embedded within larger-scale stratocumulus cloud patches and/or cloud lines moving in from the northeastern Pacific Ocean in the easterly trade winds. These cloud patches develop in the trade-wind flow downstream of the large shallow stratocumulus cloud mass that covers much of the northeastern Pacific Ocean between Hawaii and California. Tropical cyclones originating in the intertropical convergence zone sometimes move north through this stratocumulus cloud mass, producing, in their wake, cloud-free regions that then advect toward the Hawaiian Islands. These regions contribute to the variability of the organization of cloud patterns and rainband occurrence offshore of Hawaii.

Previous studies have employed data analysis and modeling to explain dynamical and thermodynamical processes that lead to the development of a flow separation line upwind of Hawaii and cloud formation along the line. This study shows that most rainbands occurring near the flow separation line first form upstream within cloud patches and/or cloud lines approaching the island and stretch within the deformation flow as the trade winds deflect around the island. Analyses of thermodynamic soundings suggest that lifting associated with convergence at the flow separation line is frequently sufficient to produce clouds but insufficient to trigger free convection and rainbands.

A diurnal oscillation in rainband frequency upwind of the island is documented. This diurnal behavior in rainband frequency may be related to the strong diurnal radiational forcing that occurs at the top of the trade-wind marine layer.

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