Vorticity, deformation and divergence signals associated with stratosphere–troposphere exchange

Jaeger, Eric B.; Sprenger, Michael

doi:10.1002/qj.482

Cited by 3 publications

(2 citation statements)

References 37 publications

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“…Following the idea of the gradient Richardson number Ri , which is an indicator for hydrostatic instabilities [ Turner , 1973], mixing is expected to be triggered not only by deformations in the flow such as stirring or stretching, but also by convective instabilities. The conditions of low static stability, i.e., dθ / dz ∼ 0, is a significant contributor to mixing in the troposphere [ Jeager and Sprenger , 2009].…”

Section: Introductionmentioning

confidence: 99%

On the mixing‐driven formation of the Extratropical Transition Layer (ExTL)

Konopka

Pan

2012

J. Geophys. Res.

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[1] We present a case study on the formation and structure of the Extratropical Transition Layer (ExTL) using in situ observations and a Lagrangian chemical transport model. The results show that the model with mixing parameterized from the large-scale flow deformations well reconstructs the observed asymmetric structure of the ExTL with a deeper transition layer on the cyclonic side of the jet stream. Information from the model and observations are integrated using tracer-tracer correlations between ozone (O 3 ) and carbon monoxide (CO). Transport of chemical tracers from the stratospheric or tropospheric background to the ExTL through mixing is identified by the change of the CO-O 3 correlation in the CO-O 3 space. The ExTL formation process simulated by the model, therefore, provides a scenario to connect the mixed air parcels to the history of mixing. An estimate of timescales of ExTL formation is made using model experiments. The results show that the fastest formation of the ExTL occurs on the isentropic levels below the subtropical jet core, e.g. around 3 weeks for 310 K, whereas at 360 K level (jet core) the formation of the ExTL needs around 3 months. Overall, this result demonstrates the important role of mixing in transport of trace gases across the tropopause.

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Section: Introductionmentioning

confidence: 99%

On the mixing‐driven formation of the Extratropical Transition Layer (ExTL)

Konopka

Pan

2012

J. Geophys. Res.

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“…Many studies have aimed at quantifying the STE flux (e.g., Danielsen, 1968;Holton et al, 1995;Appenzeller et al, 1996;Olsen et al, 2003;Sprenger et al, 2003;Stohl et al, 2003;Jaeger and Sprenger, 2009). This is a global problem that requires global observation and modelling.…”

Section: Introductionmentioning

confidence: 99%

Correlating tropospheric column ozone with tropopause folds: the Aura-OMI satellite data

Tang

Prather

2010

Atmos. Chem. Phys.

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Abstract. The geographic and temporal variations in tropospheric and stratospheric ozone columns from individual swath measurements of the Ozone Monitoring Instrument (OMI), on the NASA Aura spacecraft, are reasonably well simulated by the University of California, Irvine (UCI) chemistry transport model (CTM) using 1 • ×1 • ×40-layer meteorological fields for the year 2005. From the CTM we find that high-frequency spatial variations in tropospheric column ozone (TCO), including around the jet streams, are not generally correlated with variations in stratospheric ozone column, but instead are collocated with folding events involving stratospheric-origin, high-ozone layers below the tropopause. The CTM fold events are verified in many cases with available ozone sondes. Using the OMI Level 2 profiles, and defining tropopause height from our CTM using the European Centre for Medium-Range Weather Forecasts (ECMWF) fields, we find that most of the variations in TCO near CTM folding events are also not correlated with those in stratospheric ozone column. A large fraction of the OMI TCO variance is accurately simulated by the CTM where the variance is significant, especially along the subtropical jets. The absolute tropospheric columns from OMI and CTM agree swath-by-swath, pixel-by-pixel within ±5 Dobson Units (DU) for most cases. Notable exceptions are in the tropics where neither the high ozone from biomass burning nor the low ozone in the convergence zones over the Pacific is found in the OMI observations, because of OMI's insensitivity to the lower troposphere. Another difference is identified with the OMI profiles near the southern subtropical jet. The CTM has a high bias in stratospheric column outside the tropics, due to problems previously identified with Correspondence to: Q. Tang (tangq@uci.edu) the stratospheric circulation in the 40-layer meteorological fields. Overall, we identify ozone folds with short-lived features in TCO that have scales of a few hundred kilometres as observed by OMI.

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Correlating tropospheric column ozone with tropopause folds: the Aura-OMI satellite data

Tang¹,

Prather²

2010

Preprint

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The geographic and temporal variations in tropospheric and stratospheric ozone columns from individual swath measurements of the Ozone Monitoring Instrument (OMI) on the NASA Aura spacecraft are reasonably well simulated by the University of California, Irvine (UCI) chemistry transport model (CTM) using 1°×1°×40-layer meteorological fields for year 2005. From the CTM we find that high-frequency spatial variations in tropospheric column ozone (TCO), including around the jet streams, are not generally correlated with variations in stratospheric ozone column, but instead are collocated with folding events involving stratospheric-origin, high-ozone layers below the tropopause. The CTM fold events are verified in many cases with available ozone sondes. Using the OMI Level 2 profiles, and defining tropopause height from our CTM using the European Centre for Medium-Range Weather Forecasts (ECMWF) fields, we find that most of the variations in TCO near CTM folding events are also not correlated with those in stratospheric ozone column. The absolute tropospheric columns from OMI and CTM agree swath-by-swath, pixel-by-pixel within ±5 Dobson Units (DU) for most cases. Notable exceptions are in the tropics where neither the high ozone from biomass burning nor the low ozone in the convergence zones over the Pacific is found in the OMI observations, likely because of OMI's insensitivity to the lower troposphere. A separate bias is identified with the OMI profiles near the southern sub-tropical jet. The CTM has a high bias in stratospheric column outside the tropics, due to problems previously identified with the stratospheric circulation in the 40-layer meteorological fields. Overall, we identify ozone folds with short-lived features in TCO that have scales of a few hundred kilometers as observed by OMI

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Vorticity, deformation and divergence signals associated with stratosphere–troposphere exchange

Cited by 3 publications

References 37 publications

On the mixing‐driven formation of the Extratropical Transition Layer (ExTL)

On the mixing‐driven formation of the Extratropical Transition Layer (ExTL)

Correlating tropospheric column ozone with tropopause folds: the Aura-OMI satellite data

Correlating tropospheric column ozone with tropopause folds: the Aura-OMI satellite data

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