Stratosphere-Troposphere Exchange in the Tropics. Masatomo Fujiwara Hokkaido University, Japan (14 March 2006)
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1 Stratosphere-Troposphere Exchange in the Tropics Masatomo Fujiwara Hokkaido University, Japan (14 March 2006)
2 Contents 1. Structure of Tropical Atmosphere 2. Water Vapor in the Stratosphere 3. General Circulation and Transport 4. Tropical Tropopause Layer 5. Cold Trap Hypothesis 6. Role of Large-scale Disturbances 7. Cirrus near the Tropopause 8. Summary
3 1. Structure of Tropical Atmosphere 1/4 Watukosek, Indonesia, 20 Jan Sapporo, Japan, 29 Mar Tropical Tropopause ( Cold-point tropopause defined by temp. minimum) : 16 km to 18 km, -75 deg. C to -90 deg. C (198 K to 183 K) (cf. 8 km to 12 km, -50 deg. C to -65 deg. C for mid-latitude tropopause) Stratospheric ozone layer peaks at 26 km in the tropics (22 km in mid latitudes) Dew-point/Frost-point temperatures correspond to water vapor concentrations
4 1. Structure of Tropical Atmosphere 2/4 [ Monthly Average 100 hpa (~16 km) Temperature ]
5 1. Structure of Tropical Atmosphere 3/4 [ Tropical & Global Ozone Distribution ] Mixing ratio = Poz / P Number density ~ Partial Pressure Poz (left: Thompson et al., 2003, right: Dessler, 2000)
6 1. Structure of Tropical Atmosphere 4/4 Stratospheric ozone layer : Solar ultraviolet (UV) shield for surface ecosystem Radiative balance of the Earth atmosphere Tropospheric ozone : Air quality Oxidation efficiency Global warming
7 2. Water Vapor in the Stratosphere 1/3 3~4 ppmv (parts per million by volume) (Galapagos) Saturation near the Tropical Tropopause Dehydration (Voemel et al., 2002) Entrance of the Stratosphere Determines the Lower Stratospheric Water Vapor Concentration
8 2. Water Vapor in the Stratosphere 2/3 (SPARC, No. 2, 2000) Global Stratospheric Water Vapor is Determined by: Dehydration at the Tropical Tropopause; Methane Oxidation; General (Brewer-Dobson) Circulation; Isentropic Transport
9 2. Water Vapor in the Stratosphere 3/3 Long-term Lower Strato. Water Vapor (at Boulder (40N), Colorado, USA) with NOAA Frost-Point Hygrometer (FPH) + UARS/HALOE satellite sensor Increasing Trend ~ 1% per year 50% Increase in Methane 50% Mechanism unknown (but probably related to the dehydration at the tropical tropopause) cf. Tropical Tropopause Temp. : -1.5K/20yr (Randel et al., 2004) Roles of water vapor in Strato.: Source of OH radical (Ozone Loss) Radiative Balance (Cooling of Strato.) Polar Stratospheric Clouds Increase in WV may delay the Ozone Recovery Dehydration Processes at the Tropical Tropopause?
10 3. General Circulation and Transport 1/2 Water Vapor and Ozone Meridional Mean Circulation (The Brewer-Dobson Circ.) Dynamical Mechanism: Wave-driven pump (angular momentum dissipation) Strato.-Tropo. Exchange: Tropo Strato in the Tropics Strato Tropo in high latitudes e.g., Water Vapor in Strato. Ozone in Tropo. (Holton et al., 1995)
11 3. General Circulation and Transport 2/2 Early Idea for Tropical STE process : Penetrating Cumulonimbus Clouds (Direct Observation/Explicit Modeling are very difficult) (Danielsen, 1982)
12 4. Tropical Tropopause Layer 1/4 Height of Most Tropical Clouds ( not highest cloud) : Cold-point Tropopause ~14km (P~150hPa,θ~350K) Existence of a Transition Layer at 14~18km, TTL Dehydration in TTL : Horizontal Transport ( Cold Trap ) Role of Large-scale Disturbances (Illustration by James Reed Holton)
13 4. Tropical Tropopause Layer 2/4 Folkins et al., 1999: A barrier to vertical mixing at 14 km in the tropics: Evidence from ozonesondes and aircraft measurements. (Samoa, 14.23S, W) If we want to think of the troposphere as a well mixed layer, then perhaps the most appropriate height for the tropical tropopause is 14 km. In the U.S. it seems that the km layer is being called the transition zone; in England people are calling it the tropical substratosphere. (Folkins, 19 July 1999)
14 4. Tropical Tropopause Layer 3/4 (For March Galapagos profile) Gettelman et al., 2004: The radiation balance of the tropical tropopause layer. Tropical Ozone & water vapor sonde data + Satellite data Clear-Sky Radiation Calc. with 5 different Radiation Codes Level of Q=0 at 15 km +/- 0.5 km (θ~360k) Bottom of TTL TTL may be the Radiative-Equilibrium Region; Slow Ascent dominant WV., CO2, Ozone all play a role in TTL radiative balance (Difference arises from Treatment of WV. Continuum and of Near IR)
15 4. Tropical Tropopause Layer 4/4 role of deep convection in TTL dominant or not? (Sherwood and Dessler, 2000)
16 5. Cold Trap Hypothesis 1/3 cf. Stratospheric Fountain Hypo. by Newell & Gould-stewart, 1981: Tropical Tropopause over Western Pacific in NH winter is cold enough for LS WV. Fountain to the Stratosphere However, in TTL, Vertical Motion is Slow Horizontal Motion is Dominant (Holton and Gettelman, 2001) Dehydration in the air parcels passing the regional-scale coldest tropopause may explain the LS WV.: Cold Trap Hypothesis
17 5. Cold Trap Hypothesis 2/3 Actual Flow Pattern? so-called Matsuno-Gill pattern : response to regional-scale convective heating (Hatsushika and Yamazaki, 2003)
18 5. Cold Trap Hypothesis 3/3 (Hatsushika and Yamazaki, 2003)
19 6. Role of Large-scale Disturbances 1/3 Q. Dominant disturbance in the tropics? A. MJO / Intra-Seasonal Osc. (organized convections) (Madden and Julian, 1972) (Nakazawa, 1988) Hierarchy of Tropical Conv.: - Cumulus Clouds - Cloud Clusters - Super Cloud Clusters (or Convectively Coupled Kelvin wave) - MJO / ISO Tropopause-level dist. associated with MJO
20 6. Role of Large-scale Disturbances 2/3 (Equator) (Equator) (Fujiwara and Takahashi, 2001)
21 6. Role of Large-scale Disturbances 3/3 Eastward-moving large-scale disturbances are dominant at the equatorial tropopause Most of them are equatorial Kelvin waves In the eastern hemisphere, these waves are associated with organized convective activity in the troposphere (MJO, convectively coupled Kelvin waves) Ozone & dry air transport Dehydration at the cold phase (Fujiwara and Takahashi, 2001)
22 7. Cirrus near the Tropopause Dehydration needs water vapor to condense and resulting cloud particles to fall out TTL should not be a clear sky Cirrus clouds influence the radiative balance and vertical motion (hence, the age of the TTL air) Supersaturation is needed for clouds to form; then, how much supersaturation is actually needed? Observations of cloud microphysical properties and water vapor in TTL are needed
23 7. Cirrus near the Tropopause Heymsfield, Ice particles observed in a cirriform cloud at -83C and implications for Polar Stratospheric Clouds, JAS, 1986 Marshall Is. (Kwajalein), 17 December 1973, WB57F (Only (?) in situ photos?) Radius of the ice particles :10~30μm
24 7. Cirrus near the Tropopause SAGE II (Wang et al., JGR, 1996) LITE Sep.9-20, 94 (Winker and Trepte, GRL, 1998) Aircraft and Lidar observations
25 8. Summary Stratosphere-Troposphere Exchange in the Tropics Structure of Tropical Atmosphere Water Vapor in the Stratosphere General Circulation and Transport Tropical Tropopause Layer Cold Trap Hypothesis Role of Large-scale Disturbances Cirrus near the Tropopause
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