(a)(b)(c) Simulation of upper troposphere CO 2 from two-dimensional and three-dimensional models Xun Jiang 1, Runlie Shia 2, Qinbin Li 1, Moustafa T Chahine 1, Edward T Olsen 1, Luke L Chen 1, Yuk L Yung 2 National Aeronautics and Space Administration Abstract The Caltech/JPL two-dimensional (2-D) chemistry and transport model (CTM) and three- dimensional (3-D) GEOS-Chem model, driven respectively by NCEP and GEOS-4 reanalysis data, have been used to simulate the upper tropospheric CO 2 from 2000 to Model results of CO 2 mixing ratios agree well with aircraft observations between 9 km and 13 km [Matsueda et al., Tellus 2002] in the tropics. Some discrepancies are evident between the 2-D and 3-D model results in the mid-latitudes, where the 2-D model matches the observations better. Comparison of the simulated vertical profiles of CO 2 between the two models reveals that the stratosphere and troposphere exchange in the 3-D model is likely too strong in the winter and spring. Meridional circulations and vertical residual velocities were calculated from GEOS-4 Reanalysis data. There is more upwelling (downwelling) in the tropics (mid-latitudes) in GEOS- 4 than in the 2-D model. Zonal mean CO 2 simulated by 2-D and 3-D models are in good agreements with the AIRS CO 2 mixing ratio retrievals from Chahine et al. [GRL 2005] between 40ºS-40ºN. There is an anti-correlation between the AIRS CO 2 and O 3 mixing ratios in the upper troposphere over South Asia in the summer, reflecting the Asian Summer Monsoon circulation. Data and Model  Data: Aircraft measurements of CO 2 from Matsueda et al. [2002] and CMDL; AIRS retrieved upper troposphere CO 2 and O 3  Model: > 2-D Caltech/JPL Chemistry and Transport Model (CTM) 10º (latitude); 40 vertical levels Transport: NCEP Reanalysis Data Boundary condition: CMDL CO 2 > 3-D GEOS-CHEM Model 2º(latitude) × 2.5º (longitude), 30 vertical levels Transport: GEOS–4 Meteorological Data Boundary condition: CMDL CO 2 CO 2 sources and sinks This work was carried out at the Jet Propulsion Laboratory, California Institute of Technology under a contract with the National Aeronautics and Space Administration as well as at a number of other research organizations Jet Propulsion Laboratory California Institute of Technology Pasadena, California Comparison of CO 2 Between Model and Aircraft Data Figure 1: Aircraft observations between 9 km and 13 km (red dots) [Matsueda et al., 2002] and modeled CO2 mixing ratios from the GEOS-Chem model averaged at the layer between 9 km and 13 km (solid line) from 2000 to The panels are for 35  S, 25  S, 15  S, 5  S, 5  N, 15  N, 25  N, and 35  N, respectively. For comparison, the CO2 mixing ratios from the Caltech-JPL 2-D model [Shia et al. 2006] are shown by dotted lines. The lower boundary conditions for 2D Caltech/JPL CTM and 3D GEOS-Chem are set to ground-based measurements [Tans et al. 1998]. As shown in Fig. 1, simulated CO 2 mixing ratios from both models agree well with the aircraft data except at mid-latitudes, where GEOS-Chem results show a low bias [Shia et al. 2006]. CO 2 Vertical Profile Figure 2: Vertical profile of CO 2 computed by the GEOS-Chem (solid line) and the Caltech-JPL 2-D model (dotted line). Upper panel: Latitude = 5  N. Lower panel: Latitude = 35  N. Solid: GEOS-Chem; Dash: 2D Caltech/JPL CTM 35N 5N Meridional Circulation & Residual Vertical Velocity Figure 3: (a) Difference of stream function between GEOS-4 and 2D. Units are m 2 /s. (b) Difference of vertical residual velocity between GEOS-4 and 2D. (c) Vertical profile of vertical residual velocity at 35ºN. Units are m/s. Comparison of CO 2 Between AIRS Retrieval, Model and Aircraft Data Figure 4: AIRS retrieved upper tropospheric CO 2 in Jan, Apr, Jul, and Oct of 2003 [Chahine et al., 2005 GRL]. Please refer to Chahine et al. [2006 AGU] for more detail. Conclusions  The 2D Caltech/JPL CTM and 3-D GEOS-Chem simulations of CO 2 mixing ratio show good agreements with the Matsueda et al. [2002] aircraft CO 2 data from 35ºS to 35ºN. Both models capture the observed seasonal cycle and interannual variability of CO 2 in the tropical upper troposphere. Stratosphere and troposphere exchange is likely to be too strong in the GEOS-4 reanalysis data, which can explain in part the difference between GEOS- Chem simulated and aircraft observed CO 2 mixing ratio in the winter and spring.  The latitudinal distribution of AIRS tropospheric CO 2 agrees reasonably well with model CO 2 and aircraft CO 2 from 40ºS to 40ºN.  There is a clear anti-correlation between AIRS retrieved CO 2 and O 3 in the South Asia summer monsoon region.  Stream function derived from GEOS-4 Reanalysis data is much stronger than that from NCEP. Vertical residual velocities are derived from the stream functions. There is more upwelling (downwelling) in the tropics (mid-latitudes) in the winter, which contributes to the difference between GEOS-Chem and aircraft data. Anti-correlation Between AIRS CO 2 and O 3 In the South Asia Monsoon Region  AIRS retrieved CO 2 and O 3 over 26ºN- 30ºN, 60ºE-120ºE are investigated in July There is a clear anti-correlation between CO 2 and O 3. Correlation coefficient is Figure 7: Normalized AIRS CO2 and O3 from Jul 1, 2003 to Jul, 25, Please refer to Qinbin et al. [2006, AGU] for more detail. (a)(b) (c) (d) Fig. 2 shows vertical profiles of CO 2 simulated by the GEOS-Chem (solid line) and the Caltech- JPL CTM (dotted line) at 5  N (upper panel) and 35  N (lower panel). GEOS-Chem CO2 vertical profiles show a smaller vertical gradient than the Caltech/JPL model at mid-latitudes (35  N), likely due to excessive vertical transport in GEOS-4. Figure 5: Tropospheric CO2 from AIRS (black line) against 2D model (Green line), 3D model forced by CMDL boundary condition (Red line), 3D model forced by CO2 sources and sinks (Orange line), Matsueda aircraft data (Purple dots), and CMDL aircraft data (Blue cross) in Jan, Apr, Jul, and Oct of Figure 6: GEOS-Chem CO 2 at 300 hPa in Jan, Apr, Jul, and Oct of JanApr Oct Jul  The latitudinal distribution of AIRS tropospheric CO 2 agrees reasonably well with model and aircraft CO 2 from 40ºS to 40ºN. There are some longitudinal differences between GEOS-Chem and AIRS, which will be investigated in the future using inverse modeling. 1 Jet Propulsion Laboratory, California Institute of Technology, 4800 Oak Grove Drive, Pasadena, CA Division of Geological and Planetary Sciences, California Institute of Technology, Pasadena, CA 91125