A Lagrangian perspective of the tropopause and the ventilation of the lowermost stratosphere

Abstract

Back trajectories driven by large‐scale analyzed wind fields are used to investigate troposphere to stratosphere transport (TST) in the Northern Hemisphere tropopause region, as well as the surface sources for such transport, defined in terms of the locations where each trajectory last left the atmospheric boundary layer (log pressure height z* < 1 km). The proportion χBL of those trajectories arriving in the tropopause region that have visited the boundary layer within the previous fixed time period (typically 30 days) is determined as a function of each trajectory's final equivalent latitude and potential temperature. For a range of potential temperature surfaces (∼300–380 K), χBL is shown to have a sharp gradient in the extratropics indicative of a partial permeable barrier to transport that can be identified as a “Lagrangian tropopause.” Variations in χBL with equivalent latitude and potential temperature and on seasonal timescales are shown to provide a novel measure for the relative location and permeability of the tropopause barrier. Details such as the presence of a “ventilated layer” in the northern summer extratropical lower stratosphere (∼370–410 K) are clearly apparent. Directly below this layer (340–370 K) the tropopause barrier to transport is shown to be relatively strong, whereas below 340 K it is again more permeable. A distinction can therefore be made between “extratropical” TST that primarily ventilates the lowermost stratosphere below 340 K and “tropical” TST that occurs into the 370–410 K ventilated layer. The boundary layer source regions for extratropical TST are shown to correspond to those regions previously identified as sources for deep frontal uplift in the warm conveyor belt circulations of extratropical cyclones, although elevated regions such as the Himalayan plateau are also seen to be important. Tropical TST has different source regions associated with regions of active deep convection such as the western tropical Pacific and, in the northern summer, the Indian subcontinent. The source regions are, in general, found to be geographically localized, leading to the conclusion that subject to the limitations of the methodology, trace gas emissions in specific regions are substantially more likely to be transported to the lowermost stratosphere than elsewhere. The implications for the assessment of ozone depletion by very short lived halogenated species are mentioned.

Residual circulation trajectories and transit times into the extratropical lowermost stratosphere

“…similar results from the trajectory studies by Berthet et al (2007); Hoor et al (2010) and the O 3 -N 2 O correlation analysis by Hegglin and Shepherd (2007)). Furthermore, they used simultaneous measurements of SF 6 and CO 2 to calculate tracer transit times (resulting from residual circulation transport and two-way mixing) from the tropical upper troposphere to the extratropical LMS.…”

Seasonal variations of CO2 near the tropopause observed by commercial aircraft

“…In addition, some studies have identified the longitudinal distribution of the STE activity [e.g., Postel and Hitchman, 1999;Sprenger et al, 2007]. It is possible that the spatial variation in the stratospheretroposphere exchange which our study and the others have identified is mainly related to Asian monsoon and cyclonic activity [e.g., Chen, 1995;Dethof et al, 1999;Sprenger and Wernli, 2003;Park et al, 2007;Levine et al, 2007;Berthet et al, 2007].…”

Seasonal and inter-annual variations in troposphere-to-stratosphere transport from the tropical tropopause layer

“…Hatsushika and Yamazaki, 2003;Bonazzola and Haynes, 2004;Fueglistaler et al, 2004 and, usually in an effort to explain the very low water vapour mixing ratios observed in the tropical lower stratosphere (see e.g., Mote et al, 1995 and. There have been relatively few model studies of transport from the TTL into the ELS (Chen, 1995;Berthet et al, 2007) despite recognition of its potential importance (e.g. Allam and Tuck, 1984;Holton et al, 1995) and observational evidence of its effects on the chemical composition of the mid-latitude lower stratosphere (e.g.…”