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Stephan Rasp, Tobias Selz, and George C. Craig

Mediterranean Sea. Two phenomena were associated with this system: a WCB extending from the Mediterranean Sea to Scandinavia and intense, deep convection over the Adriatic Sea. Therefore, a combination of convective and slantwise ascent processes can be expected. This case was already investigated as part of the THORPEX North Atlantic Waveguide and Downstream Impact Experiment (T-NAWDEX-Falcon) observation campaign ( Schäfler et al. 2014 ). On 14 October a cyclone formed ahead of an upper-level trough

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Andreas Schäfler, George Craig, Heini Wernli, Philippe Arbogast, James D. Doyle, Ron McTaggart-Cowan, John Methven, Gwendal Rivière, Felix Ament, Maxi Boettcher, Martina Bramberger, Quitterie Cazenave, Richard Cotton, Susanne Crewell, Julien Delanoë, Andreas Dörnbrack, André Ehrlich, Florian Ewald, Andreas Fix, Christian M. Grams, Suzanne L. Gray, Hans Grob, Silke Groß, Martin Hagen, Ben Harvey, Lutz Hirsch, Marek Jacob, Tobias Kölling, Heike Konow, Christian Lemmerz, Oliver Lux, Linus Magnusson, Bernhard Mayer, Mario Mech, Richard Moore, Jacques Pelon, Julian Quinting, Stephan Rahm, Markus Rapp, Marc Rautenhaus, Oliver Reitebuch, Carolyn A. Reynolds, Harald Sodemann, Thomas Spengler, Geraint Vaughan, Manfred Wendisch, Martin Wirth, Benjamin Witschas, Kevin Wolf, and Tobias Zinner

) on 13 October when it triggered heavy precipitation and strong winds over France and Italy. The 24-h accumulated precipitation in the Herault region reached ∼250 mm ( Fig. 10b ), and wind gusts exceeding 100 km h −1 were observed along the French Mediterranean coast ( Fig. 10c ). As in typical Cévenol episodes, strong southerlies brought warm and moist air from the Mediterranean Sea toward the Massif Central and caused heavy orographic precipitation over the mountain ranges of the Cevennes

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Hilke S. Lentink, Christian M. Grams, Michael Riemer, and Sarah C. Jones

influence of Sardinia on Corsican rainfall in the western Mediterranean Sea: A numerical sensitivity study . Atmos. Res. , 153 , 451 – 464 , . 10.1016/j.atmosres.2014.10.004 Evans , C. , and Coauthors , 2017 : The extratropical transition of tropical cyclones. Part I: Cyclone evolution and direct impacts . Mon. Wea. Rev. , 145 , 4317 – 4344 , . 10.1175/MWR-D-17-0027.1 Foerster , A. M. , M. M. Bell , P

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Andreas Schlueter, Andreas H. Fink, Peter Knippertz, and Peter Vogel

clear picture of the propagation of the ER wave. As a largely independent dataset, rain gauge measurements confirm the significant influence over the entire continent. The wave exhibits significant modulation patterns that reach up to the Mediterranean Sea and to East Africa. The approximate wavelength is 8000 km; thus, it is dry over central and East Africa when wet anomalies persist over West Africa and vice versa. The modulation patterns as measured by TRMM are very similar to CHIRPS but more

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Georgios Fragkoulidis and Volkmar Wirth

.g., the jet exit and cyclolysis region over Europe and the Norwegian Sea). Furthermore, by comparing the c gx maps ( Figs. 4i–l ) to the respective ones of c gy ( Figs. 4m–p ), it is apparent that RWP propagation is almost everywhere predominantly zonal ( c gx > | c gy |). In most regions, the spatial pattern and seasonal variability of c gx follows closely the ones of zonal wind velocity ( Fig. S9 ). Focusing on the winter season, a distinct band of high c gx values appears in the

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Kevin Bachmann, Christian Keil, George C. Craig, Martin Weissmann, and Christian A. Welzbacher

potential biases in temperature and surface pressure ( Hanley et al. 2015 ; Necker et al. 2018 ; Hirt et al. 2019 ). Fig . 2. Map of the investigated COSMO-KENDA and the DE-EPS domain centered over Germany and covering parts of central Europe: the altitude above sea level is shown in grayscale and the blue (red) box indicates the subdomain north (south); political borders are displayed in dotted lines for orientation. The model setup chosen is configured as similar to the idealized COSMO

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Andreas Schlueter, Andreas H. Fink, and Peter Knippertz

-lagged analysis The MJO and ER waves trigger rainfall anomalies up to the Mediterranean Sea ( Part I ). To test, whether and how the waves couple with the extratropical circulation, geopotential and wind at 300 hPa were analyzed. The influence on lower-tropospheric thickness was analyzed between 600 and 925 hPa. The origin and development of the wave signal were traced using a time-lag analysis. The tropical plumes were observed in the local phase 4 (see section 2d of Part I for more detail on the phase

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Julia H. Keller, Christian M. Grams, Michael Riemer, Heather M. Archambault, Lance Bosart, James D. Doyle, Jenni L. Evans, Thomas J. Galarneau Jr., Kyle Griffin, Patrick A. Harr, Naoko Kitabatake, Ron McTaggart-Cowan, Florian Pantillon, Julian F. Quinting, Carolyn A. Reynolds, Elizabeth A. Ritchie, Ryan D. Torn, and Fuqing Zhang

-hPa waveguide as red contour separating high PV air (>3 PVU; orange shading) from lower PV air (<3 PVU; unshaded). Midlevel baroclinic zone as blue tilted surface. Trajectories of rapidly ascending air parcels as blue–red–blue lines, reflecting the diabatic PV modification of the parcels from low to high to low PVU, respectively. Mean sea level pressure (gray contours; every 8 hPa) and equivalent potential temperature (violet contours; 320 and 330 K) are indicated in the lower panel. [Figure 11a

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Thomas Engel, Andreas H. Fink, Peter Knippertz, Gregor Pante, and Jan Bliefernicht

TRMM radar data (e.g., Gosset et al. 2013 ; Pfeifroth et al. 2016 ). The period used in the present study is 1983–2014. 3. Methods a. Analysis of atmospheric dynamics Both Ouagadougou and Dakar are located in the Sahel, a region stretching between about 12° and 18°N from the Atlantic coast to the Red Sea (see Fig. 1a ). This area is characterized by the transition from the arid conditions of the Sahara with less than 200 mm rainfall per year to a more humid climate equatorward. The West African

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Gabriel Wolf and Volkmar Wirth

propagation. On the other hand, the diagnostic in Fig. 4a completely misses the generation of the wave packet over the Beaufort Sea. Instead, it connects the North American RWP with an anomaly over the mid-Pacific. This is consistent with the path of the RWP (see the trajectory on the latitude–longitude map atop the Hovmöller diagram in Fig. 4a ), which starts at about 45°N and 170°W. The poor representation of meridionally propagating RWPs is a known deficiency of the method of Zimin et al. (2003

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