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Ronald B. Smith, Alison D. Nugent, Christopher G. Kruse, David C. Fritts, James D. Doyle, Steven D. Eckermann, Michael J. Taylor, Andreas Dörnbrack, M. Uddstrom, William Cooper, Pavel Romashkin, Jorgen Jensen, and Stuart Beaton

statistical approach to this unique dataset. Our statistical results will build a foundation for later case studies, model–data comparisons, and merging flight-level and remote sensing data. Fig . 1. All DEEPWAVE flight legs during June and July 2014. Most legs were flown at z = 12.1 km. (top) Full DEEPWAVE region and (bottom) legs over New Zealand and upper-air stations. 2. Flux calculations a. Flux definitions In our statistical analysis of flight-level data, we focus on the standard momentum and

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Tanja C. Portele, Andreas Dörnbrack, Johannes S. Wagner, Sonja Gisinger, Benedikt Ehard, Pierre-Dominique Pautet, and Markus Rapp

. Dotted–dashed vertical lines are the separation into accelerating, maximum, and decelerating forcing phases. Dotted vertical lines further show the division into maximum forcing phase I and II and early, mid-, and late decelerating forcing phases. The analysis presented in this paper focuses on observations along the Mt. Aspiring 2b (hereinafter Mt-A-2b) transect ( Fig. 1 ), a mountain-wave flight track with a direction of 300° from northwest to southeast over Mt. Aspiring (44.38°S, 168.73°E). During

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Christopher G. Kruse, Ronald B. Smith, and Stephen D. Eckermann

Analysis for Research and Applications (MERRA) ( Rienecker et al. 2011 ) and MERRA2 ( Bosilovich et al. 2010 ). Throughout the DEEPWAVE period, there was a frequent ambient wind minimum in the lower stratosphere, resulting in significant mountain wave attenuation and GWD. GW dynamics within this layer are the focus of this paper. The outline of this paper is as follows. The WRF Model configuration and validation are presented in section 2 . In section 3 , mountain wave propagation and attenuation is

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