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000892382 1001_ $$0P:(DE-HGF)0$$aThomas, Max$$b0
000892382 245__ $$aStratospheric carbon isotope fractionation and tropospheric histories of CFC-11, CFC-12 and CFC-113 isotopologues
000892382 260__ $$aKatlenburg-Lindau$$bEGU$$c2020
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000892382 520__ $$aWe present novel measurements of the carbon isotope composition of CFC-11 (CCl3F), CFC-12 (CCl2F2), and CFC-113 (CF2ClCFCl2), three atmospheric trace gases that are important for both stratospheric ozone depletion and global warming. These measurements were carried out on air samples collected in the stratosphere – the main sink region for these gases – and on air extracted from deep polar firn snow. We quantify, for the first time, the apparent isotopic fractionation, εapp(13C), for these gases as they are destroyed in the high- and mid-latitude stratosphere: εapp(CFC-12, high-lat) = (−20.2 ± 4.4) ‰ and εapp(CFC-113, high-lat) = (−9.4 ± 4.4) ‰, εapp(CFC-12, mid-lat) = (−30.3 ± 10.7) ‰, and εapp(CFC-113, mid-lat) = (−34.4 ± 9.8) ‰. Our CFC-11 measurements were not sufficient to calculate εapp(CFC-11) so we instead used previously reported photolytic fractionation for CFC-11 and CFC-12 to scale our εapp(CFC-12), resulting in εapp(CFC-11, high-lat) = (−7.8 ± 1.7) ‰ and εapp(CFC-11, mid-lat) = (−11.7 ± 4.2) ‰. Measurements of firn air were used to construct histories of the tropospheric isotopic composition, δT(13C), for CFC-11 (1950s to 2009), CFC-12 (1950s to 2009), and CFC-113 (1970s to 2009) – with δT(13C) increasing for each gas. We used εapp(high-lat), which were derived from more data, and a constant isotopic composition of emissions, δE(13C), to model δT(13C, CFC-11), δT(13C, CFC-12), and δT(13C, CFC-113). For CFC-11 and CFC-12, modelled δT(13C) was consistent with measured δT(13C) for the entire period covered by the measurements, suggesting no dramatic change in δE(13C, CFC-11) or δE(13C, CFC-12) has occurred since the 1950s. For CFC-113, our modelled δT(13C, CFC-113) did not agree with our measurements earlier than 1980. While this discrepancy may be indicative of a change in δE(13C, CFC-113), it is premature to assign one. Our modelling predicts increasing δT(13C, CFC-11), δT(13C, CFC-12), and δT(13C, CFC-113) into the future. We investigated the effect of recently reported new CFC-11 emissions on background δT(13C, CFC-11) by fixing model emissions after 2012, and comparing δT(13C, CFC-11) in this scenario to the model base case. The difference in δT(13C, CFC-11) between these scenarios was 1.4 ‰ in 2050. This difference is smaller than our model uncertainty envelope and would therefore require improved modelling and measurement precision, as well as better quantified isotopic source compositions, to detect.
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000892382 536__ $$0G:(EU-Grant)678904$$aEXC3ITE - EXploring Chemistry, Composition and Circulation in the stratosphere with InnovativeTEchnologies (678904)$$c678904$$fERC-2015-STG$$x1
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000892382 7001_ $$0P:(DE-Juel1)177681$$aLaube, Johannes C.$$b1$$eCorresponding author
000892382 7001_ $$00000-0002-1553-4043$$aKaiser, Jan$$b2
000892382 7001_ $$0P:(DE-HGF)0$$aAllin, Samuel$$b3
000892382 7001_ $$00000-0002-6820-2296$$aMartinerie, Patricia$$b4
000892382 7001_ $$00000-0002-5372-8148$$aMulvaney, Robert$$b5
000892382 7001_ $$0P:(DE-HGF)0$$aRidley, Anna$$b6
000892382 7001_ $$00000-0002-6688-8968$$aRöckmann, Thomas$$b7
000892382 7001_ $$0P:(DE-HGF)0$$aSturges, William T.$$b8
000892382 7001_ $$0P:(DE-HGF)0$$aWitrant, Emmanuel$$b9
000892382 773__ $$0PERI:(DE-600)2069857-4$$ahttps://doi.org/10.5194/acp-2020-843$$p843$$tAtmospheric chemistry and physics / Discussions$$v2020$$x1680-7367$$y2020
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