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Kevin R. Haghi and Dale R. Durran

1. Introduction Atmospheric bores are disturbances whose passage is accompanied by a pressure rise and a semipermanent upward displacement of the isentropic surfaces ( Knupp 2006 ; Haghi et al. 2017 ). A series of waves often trails behind the bore’s leading edge, and in contrast to density currents, the near-surface temperature remains relatively unchanged, or even warms, after the bore passes. One of the most spectacular and well-studied examples of an atmospheric bore is the “morning glory

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William C. Ladwig and David J. Stensrud

easterly wave variability and its relationship to Atlantic tropical cyclone activity. J. Climate , 14 , 1166 – 1179 . Wilks , D. S. , 1995 : Statistical Methods in the Atmospheric Sciences: An Introduction . Vol. 59, International Geophysics Series, Academic Press, 467 pp . Fig . 1. Geography of the North American monsoon region. The AZNM region used to define monsoon onset is outlined by the rectangular box. Vertical dashed line indicates 110°W. Fig . 2. Histogram of monsoon onset days

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Colin O. Hines

I APRIL 1988 COLIN O. HINES 1269Generation of Turbulence by Atmospheric Gravity Waves COLIN O. HINESArecibo Observatory, Arecibo, Puerto Rico(Manuscript received t3 April 1987, in final form 26 October 1987)ABSTRACT The standard current criterion for the generation of turbulence by atmospheric gravity waves and for theassociated limitation on wave growth is based upon the standard criterion for static

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Peter A. E. M. Janssen and Pedro Viterbo

Jt~E 1996 JANSSEN AND VITERBO 1269Ocean Waves and the Atmospheric Climate PETER A. E. M. JANSSEN* AND PEDRO VITERBOEuropean Centre For Medium-Range Weather Forecasts, Reading, Berkshire, United Kingdom(Manuscript received 3 April 1995, in final form 2 October 1995)ABSTRACT Ocean waves are generated by wind and, as a consequence, there is a considerable transfer of

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Joowan Kim, William J. Randel, Thomas Birner, and Marta Abalos

–2012 (34 yr). Monthly National Oceanic and Atmospheric Administration (NOAA) outgoing longwave radiation (OLR; Liebmann and Smith 1996 ) is also used to understand the relationship between wave forcing and convective activity in the tropics. b. Upwelling calculation Upwelling is computed in terms of the transformed Eulerian-mean (TEM) residual vertical velocity. The TEM vertical velocity in spherical log-pressure coordinates ( Andrews et al. 1987 ) is where an overbar represents zonal mean, a prime is

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Carly R. Tozer, James S. Risbey, Terence J. O’Kane, Didier P. Monselesan, and Michael J. Pook

highs (e.g., Catto and Pfahl 2013 ; Pfahl 2014 ), to the larger-scale atmospheric structures, like Rossby waves, which provide dynamic support to the synoptic processes ( Pezza et al. 2012 ) and which may act as longer-range precursors of these extreme events ( Wirth et al. 2018 ). Our interest lies in rainfall extremes in the Southern Hemisphere midlatitudes and, in particular, in Tasmania, Australia ( Figs. 1 , 2 ). Our motivation for focusing on Tasmania relates to its location in the storm

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J. Vanneste

centrifugally stable stratified Taylor–Couette flow. Phys. Rev. Lett. , 86 , 5270 – 5273 . Molemaker , M. J. , J. C. McWilliams , and I. Yavneh , 2005 : Baroclinic instability and loss of balance. J. Phys. Oceanogr. , 35 , 1505 – 1517 . Muraki , D. J. , 2003 : Revisiting Queney’s flow over a mesoscale ridge. Preprints. Ninth Conf. on Mountain Meteorology , Aspen, CO, Amer. Meteor. Soc., 5.3 . Ólafsdóttir , E. I. , 2006 : Atmospheric-wave generation: An exponential

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Kirsty E. Hanley and Stephen E. Belcher

1. Introduction Understanding the dynamical processes that occur in the lower atmosphere and upper ocean is important for a full understanding of air–sea interaction. Correct parameterization of the air–sea momentum fluxes in the atmospheric boundary layer is important for atmospheric, oceanic, and wave models. Currently, large-scale models only allow the momentum flux, τ tot , to be positive, from atmosphere to ocean. Recent observations have reported unusual behavior during conditions of

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Edward K. Vizy and Kerry H. Cook

, a temporal compositing technique is used in addition with synoptic analysis. For each wave, the location of the 700-hPa vortex center is used to determine when the vortex passes the 15° and 25°W meridians (i.e., into and out of the boxed area in Fig. 1 ), which we call the Cape Verde region. Atmospheric fields (i.e., geopotential height, temperature, winds, vertical velocity, relative humidity, precipitation) are averaged over this period to establish the environmental conditions in the Cape

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Christian Franzke, Andrew J. Majda, and Grant Branstator

planetary wave dynamics? In this linear view the atmospheric flow would consist of preferred flow patterns; any linear combination of these preferred patterns would again be a preferred flow pattern, and the probability density functions (PDFs) of these flow patterns would not have multiple extrema. If driven by additive white noise, these PDFs would be Gaussian. Another indication of linear dynamics is the form of mean tendencies in phase space. For a stable linear system these tendencies must be

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