TTL & H 2 O Brewer-Dobson Circulation (~years) Waves. Waves T T TEMPERATURE. Tropical Tropopause Layer (TTL) Equator. Stratosphere Ozone Layer QBO
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1 H 2 O in Strato. - Radiative Balance (IR cooling) - Source of HOx Ozone Layer H 2 O Distribution in Strato. - Dehydration/cold trap in TTL (microphysics of cirrus clouds matter!) - Brewer-Dobson Circ. - Methane Oxidation ~3.5 ppmv (tropical LS) to ~6 ppmv (higher) TTL & H 2 O Brewer-Dobson Circulation (~years) QBO Waves Waves T T TEMPERATURE Stratosphere Ozone Layer 18 km -80C (Colder in NH Winter) H 2 O & Cirrus clouds Tropical Tropopause Layer (TTL) Tropopause 10 km -55C Convection (on various scales) Troposphere Southern Hemisphere Equator 1~2 km Planetary Boundary Layer Northern Hemisphere
2 Tropical Tropopause Layer (TTL) Upper Troposphere and Lower Stratospehre (UTLS) Masatomo Fujiwara (Hokkaido U), Yoichi Inai, Takatoshi Sakazaki (Kyoto U),Suginori Iwasaki (NDA), Junko Suzuki, Shin-ya Ogino, Tomoe Nasuno (JAMSTEC), & the SOWER team 1. Roles of tropical organized convection and waves in the TTL 2. Investigation of dehydration processes in the TTL using the match technique 3. Roles of overshooting cumulonimbus clouds for hydration and dehydration of the tropical stratosphere 4. Diurnal variations in the TTL 5. Cross-tropopause transport by Asian monsoon circulation 6. TTL modeling using the Nonhydrostatic ICosahedral Atmospheric Model (NICAM)
3 Roles of tropical organized convection and waves in the TTL Dehydration in the stratosphere suppresses the increase of the surface temperature and the rate of global warming(e.g., Solomon et al., 2010, Science) Approach: Observations using the Equatorial Atmosphere Radar (EAR), Ozonesondes, Water vapor sondes, cloud particle sensors, etc.
4 Investigation of dehydration processes in the TTL using the match technique Match Technique Measuring water vapor amount before/after the dehydration in the TTL by multi-point balloon soundings w.v. mixing ratio 2nd ー ) w.v. mixing ratio 1st ーーーーーーーーーーーー dehydration amount quantify the dehydration in the lower TTL (Inai et al., ACP, 2013)
5 Roles of overshoot for hydration/dehydration of the tropical stratosphere <Satellites obs.> Two cloud layers above CPH Jumping cirrus? Hydration? <Simulation> Some cloud layers Tb < 200 K (MODIS) No rainfall (CloudSat) Less wind (radiosonde) No rainfall Latitude CALIOP signals Numerical simulation of overshoot under no wind condition. Courtesy of Pao Wang.
6 Diurnal variations in the TTL Diurnal variations in cirrus clouds (Fujiwara et al., 2009) atmospheric tides? diurnal variations in convection? Clouds (backscatter coefficient: β) measured by a lidar (7.5 o N, o E) [December 2004 to January 2005] Diurnally descending cirrus December 2004 January 2005 Fujiwara et al. (2009) Diurnal variability (convections, tides) and its role in the transport and dehydration in the TTL.
7 Cross-tropopause transport by Asian monsoon circulation Based on ozonesonde data taken at Hanoi, Vietnam, Ogino et al. (2013) showed that ozone transport over the subtropical region is strongly controlled by the monsoon circulation. We will investigate detailed processes of the ozone and water vapor transport by the Asian monsoon circulation in both winter and summer seasons to evaluate their budget in the TTL. <Satellite ozone obs. & trajectories in UT> Winter Summer Poleward transport due to Rossby wave response to convective heating over MC. Equatorward transport due to anti-cyclonic circulation associated with Tibetan High Ogino et al. (2013, JGR)
8 TTL in NICAM Simulation Explicit representation of cloud processes in TTL Dynamical Structure Bottom height of TTL (km) 2006 MJO case - T anomaly Z=16.9 km (5S-5N) Tropopause height (km) MJO and Kelvin wave signal in TTL Deep Convection Freq. (%) Z=18.4 km (5S-5N) Kubokawa et al. (2012)
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