Water and Methane in the Upper Troposphere and Stratosphere based on ACE-FTS Measurements Acknowledgements: The Canadian Space Agency (CSA) is the primary source of funding for this work. Other sources of funding include the Meteorological Service of Canada (MSC), Natural Sciences and Engineering Research Council of Canada (NSERC), Canadian Foundation for Innovation (CFI) and the University of Waterloo. Ray Nassar, Chris Boone, Kaley A. Walker and Peter F. Bernath Department of Chemistry, University of Waterloo, Waterloo, Ontario, Canada N2L 3G1 The SCISAT-1 mission, also known as the Atmospheric Chemistry Experiment (ACE), is a Canadian satellite mission to investigate chemical and dynamical processes that control the distribution of ozone in the stratosphere and upper troposphere. The primary instrument on SCISAT-1 is the ACE-FTS, a high resolution Fourier transform spectrometer operating in the cm -1 range. ACE-FTS solar occultation spectra dating back to January 2004 have been processed to produce Version 1 temperature and pressure profiles from. the mid-troposphere to the mesopause and VMR profiles of H 2 O, N 2 O, CO, NO, HCl, HF, HNO 3, CH 4, O 3, NO 2, HDO, SF 6, COF 2, N 2 O 5, ClONO 2, CCl 3 F, CCl 2 F 2 and CHF 2 Cl. VMR profiles of many other molecules will be included in our Version 2 data, which will soon be available. Here we present ACE-FTS H 2 O, HDO and CH 4 data and discuss their relationship to trends and measurements by other instruments as well as the implications of these results for understanding processes relating to stratospheric water. Figure 2: [H 2 O] vs. [CH 4 ] correlations from 4 ATMOS missions ( ) and ACE (2004). (ATMOS plots were reproduced from H.A. Michelsen et al. JGR 105, D18, 22713, 2000.) Tangent heights from km (open circles) were fit, with the slope giving –  and the intercept giving potential water as [H 2 O] +  [CH 4 ]. Our results indicate that increases in potential water and water entering the stratosphere [H 2 O] e have not continued. Figure 1: 83 extratropical extravortex profiles of [CH 4 ] and [H 2 O]. Individual profiles are shown as thin colored lines, averaged profiles are shown as black dotted lines and potential water as PW = [H 2 O]+2[CH 4 ] is shown in black with 1  error bars. Notice that [H 2 O] and [CH 4 ] variability from ~30-48 km is anti- correlated thus does not contribute to uncertainty in the PW profile. Figure 3: (A) ATMOS ATLAS-3 [HDO]/[H 2 O]  D profiles taken from Z. Kuang et al. GRL, 30, 7, 1372, (B) ACE-FTS [HDO]/[H 2 O]  D profiles from 25°N-25°S, which show a similar  D value at the TTL and exhibit evidence of seasonal variation. 1. Background and introduction The amount of water vapor in the stratosphere plays an important role in the climate and the chemistry of our atmosphere. Elevated levels of water are known to enhance tropospheric warming and stratospheric cooling. Elevated levels of stratospheric water accompanied by enhanced cooling, increase the formation of polar stratospheric clouds (PSCs) during the polar winter enabling heterogeneous reactions that form species which can catalytically destroy stratospheric ozone during the polar spring. Water primarily enters the stratosphere through vertical transport across the tropical tropopause layer (TTL), then circulates to midlatitudes and descends at the poles. The major photochemical source of water in the stratosphere is oxidation of CH 4 by the reaction CH 4 + 2O 2 → 2H 2 O + CO 2, in which one CH 4 molecule creates two H 2 O molecules. A high level of variability is often observed if one treats H 2 O and CH 4 independently but [H 2 O]+2[CH 4 ], often referred to as potential water (PW) is conserved with CH 4 oxidation. Numerous studies indicate an increases in stratospheric water vapor occurring in the time frame of a few years up to the past half century. This increase can partially be attributed to an increase in CH 4 emissions but the remainder is attributed to an increase in water entering the stratosphere across the TTL, known as [H 2 O] e. More recent evidence from instruments such as HALOE indicate a halt or possible plateau in the increase in stratospheric [H 2 O] in the last few years. 4. HDO and H 2 O near the tropical tropopause layer The relative importance of processes that control the quantity of water entering the stratosphere are still not well understood. In gradual dehydration, assumed to be the major process, condensation occurs gradually and the humidity of the stratosphere is controlled by the coldest temperature (or lowest saturation water VMR) that the air has experienced. In convective dehydration, air entering the TTL by deep convection is already dehydrated below stratospheric abundances. Since HDO has a lower vapor pressure than H 2 O, the isotopic composition of water vapor in the TTL region can act as a useful tracer for determining the type of dehydration processes involved. When vapor is in equilibrium with the condensed phases, HDO is preferentially removed relative to H 2 O, a process called fractionation. The convention is to express the result relative to VSMOW (Vienna Standard Mean Ocean Water) using the following relationship: Kuang et al. determined a near-vertical  D profile with  D ~ -670‰ based on 11 tropical ATMOS occultations, cited as evidence for convective dehydration. Our preliminary work with ACE-FTS data gives  D ~ -673‰ from 45 winter/spring occultations and  D ~ -648‰ based on 25 summer occultations above the TTL (14-18 km). Furthermore, we observe an increase in [HDO]/[H 2 O] ratios with altitude in the stratosphere and some seasonal variability above the TTL. We plan to do a more in depth analysis of  D profiles based on [HDO]/[H 2 O] in the future. 2. H 2 O and CH 4 measured by the ACE-FTS We have determined [H 2 O], [CH 4 ] and PW based on 83 extratropical extravortex ACE-FTS occultations. Figure 1 shows the individual and averaged profiles of the occultations used in the determination. Based on these measurements, we obtain PW = 7.14±0.05 ppm and [H 2 O] e = 3.65±0.15 ppm. Due to high variability in measured values of water crossing the TTL, [H 2 O] e is often calculated as: [H 2 O] e = [H 2 O] -  ([CH 4 ] e - [CH 4 ]) or [H 2 O] e = PW -  [CH 4 ] e where  is the magnitude of the slope of the [H 2 O] vs. [CH 4 ] correlation plot (shown in Figure 2e) and [CH 4 ] e is the methane entering the stratosphere across the TTL which can be measured more accurately than [H 2 O] e. 3. Trends and comparison with other measurements The ATMOS and ACE-FTS instruments, measurement techniques and retrievals are similar enough to justify a direct comparison of results. The occultations used above were selected to minimize seasonal affects during comparison with ATMOS measurements recorded from Figure 2 shows the [H 2 O] vs. [CH 4 ] correlation plots and indicates that the increases in PW and [H 2 O] e observed by ATMOS have clearly not continued to present. We observe only a negligible change from , however we make no prediction regarding how stratospheric water levels will unfold in the future. B e g f