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Laurence Armi and Georg J. Mayr

controlled flow: The top of the cloud layer in the WCR image ( Fig. 2b ) descends continuously from 6.0 km MSL upstream to 5.5 km MSL above the crest and 4.9 km MSL at the separation downstream. The height of the top of the cloud-filled layer measured relative to the crest at 3.85 km MSL is 2.15 km upstream and 1.65 km at the crest, giving the two-thirds ratio. Fig . 3. Vertical sections along tracks shown in Fig. 1a from the King Air (below 9 km; troposphere) and G-V (stratosphere) with reflectivity

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A. Bracci, P. Cristofanelli, M. Sprenger, U. Bonafè, F. Calzolari, R. Duchi, P. Laj, A. Marinoni, F. Roccato, E. Vuillermoz, and P. Bonasoni

1. Introduction Previous studies have suggested that stratosphere–troposphere exchange (STE) is an important aspect of climate change (e.g., Sudo et al. 2003 ), and long-term changes in stratospheric ozone (O 3 ) input can significantly affect the tropospheric O 3 budget (e.g., Ordóñez et al. 2005 ). Tropospheric O 3 strongly influences the radiative budget of the atmosphere ( Forster et al. 2007 ) and the oxidation capacity of the troposphere ( Gauss et al. 2003 ). Today, two main inputs

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