An evaluation of upper troposphere NO sub(x) with two models

Upper tropospheric NO sub(x) controls, in part, the distribution of ozone in this greenhouse-sensitive region of the atmosphere. Many factors control NO sub(x) in this region. As a result it is difficult to assess uncertainties in anthropogenic perturbations to NO from aircraft, for example, without understanding the role of the other major NO sub(x) sources in the upper troposphere. These include in situ sources (lightning, aircraft), convection from the surface (biomass burning, fossil fuels, soils), stratospheric intrusions, and photochemical recycling from HNO sub(3) . This work examines the separate contribution to upper tropospheric ``primary'' NO sub(x) from each source category and uses two different chemical transport models (CTMs) to represent a range of possible atmospheric transport. Because aircraft emissions are tied to particular pressure altitudes, it is important to understand whether those emissions are placed in the model stratosphere or troposphere and to assess whether the models can adequately differentiate stratospheric air from tropospheric air. We examine these issues by defining a point-by-point ``tracer tropopause'' in order to differentiate stratosphere from troposphere in terms of NO sub(x) perturbations. Both models predict similar zonal average peak enhancements of primary NO sub(x) due to aircraft ( identical with 10-20 parts per trillion by volume (pptv) in both January and July); however, the placement of this peak is primarily in a region of large stratospheric influence in one model and centered near the level evaluated as the tracer tropopause in the second. Below the tracer tropopause, both models show negligible NO sub(x) derived directly from the stratospheric source. Also, they predict a typically low background of 1-20 pptv NO sub(x) when tropospheric HNO sub(3) is constrained to be 100 pptv of HNO sub(3) . The two models calculate large differences in the total background NO sub(x) (defined as the source of NO sub(x) from lightning+stratosphere+surface+HNO sub(3) ) when using identical loss frequencies for NO sub(x) . This difference is primarily due to differing treatments of vertical transport. An improved diagnosis of this transport that is relevant to NO sub(x) requires either measurements of a surface-based tracer with a substantially shorter lifetime than super(2) super(2) super(2) Rn or diagnosis and mapping of tracer correlations with different source signatures. Because of differences in transport by the