1. Southern Ocean Surface Measurements and the Upper Ocean Heat Balance Janet Sprintall Sarah Gille Shenfu Dong Scripps Institution of Oceanography, UCSD

2. Challenges in the Southern Ocean Western Boundary Currents Southern Ocean data richdata poor sampling possible all year roundvery few winter observations heat transport from low to high latitudes circumpolar SST probably means little net heat transport ocean heat transport primarily geostrophic strong westerlies drive strong meridional Ekman transport fairly reliable, validated surface heat flux products heat flux products with very large uncertainties Talk Outline: 1.Status of shipboard observations in the Southern Ocean 2.Science Applications:- a. Variability in the Antarctic Polar Front b. The upper ocean heat budget in the Southern Ocean 3. Conclusions: Implications for data sampling requirements in the Southern Ocean

3. Southern Ocean HR-XBT Measurements USA-SIO; Aust-CSIRO; NZ-NIWA; France www-hrx.ucsd.edu U.S-Chinese moon.ldgo.columbia.edu/~xiaojun/xbt/ Italian CLIMA PX08 IX15 IX21 PX50 PX81 AX22 IX28 AX25 AX18 PX14 NOAA-AOML www.aoml.noaa.gov/phod/hdenxbt/high_density_home.html

4. Drake Passage Measurements wind speed (m/s) pCO2 (  atm) salinity (psu) XBT temperature Depth averaged ADCP velocity PIs: Sprintall (XBT); Takahashi, Sweeney (pCO2); Chereskin, Firing (ADCP)

5. Science Application: 1. Variability in the Antarctic Polar Front* AMSR-E (Microwave) AMSR-E: cloud penetration MODIS (Infrared) Lots of cloudy or bad data *Dong, Sprintall & Gille, Location of the Antarctic Polar Front from AMSR-E Satellite Sea Surface Temperature measurements, J. Phys. Oceanogr., in press, 2006.

6. Comparison of the PF Location from XBT and AMSR-E SST  Subsurface Polar Front from XBT (northern extent of the 2°C isotherm at 100- 300m depth) Surface Polar Front from AMSR-E (southernmost location of an SST gradient above 1.5x10 -2 °C km -1 )

7. Mean Polar Front Location AMSR-E (2002-05) Dong et al. (2006) AVHRR SST (1987 – 1993) Moore et al. (1999) Deep ocean basin with weak bottom slope: large PF variability

8. What controls the Polar Front Variability? 1. Response of PF location to meridional shifts in the wind field (∂  PF /∂t ~ ∂  (  x )/∂t) negative phase: shift in latitude of maximum zonal wind stress leads meridional shift in PF histogram of phase coherence 60% > 95%CI phase wind PF wind phase

9. Science Application: 2. Southern Ocean Upper Ocean Heat Budget* Domain Averaged Surface Layer Heat Balance (weekly resolution on 1°x1° grid) * Dong, Gille and Sprintall, Heat budget of the Southern Ocean, in prep, 2006

10. Horizontal Advection geostrophic advection (AVISO SSHa plus GRACE) Ekman advection (COAPS wind stress) T m mixed layer temperature AMSR-E SST

11. Imbalance of the Heat Budget Analysis Largest imbalance in winter (~100 W m -2 ) “Best Case” rms of the imbalance is 146 Wm -2 (0.031°C/day) (NCEP1 air-sea heat fluxes; ARGO density MLD; diffusion  =500 m 2 s -2 ; spatially-variable ∆T from ARGO)

12. Spatial rms of Q net (Wm -2 ) (1 Jan 2000 - 31 August 2002) Sensitivity: 1. Surface heat flux products NCEP1-NCEP2 NCEP1-ECMWF NCEP1-SOC (monthly clim) RMS of heat balance: NCEP1: 146 Wm -2 NCEP2: 148 Wm -2 (June 02 - Dec 05)

13. Sensitivity: 2. Mixed Layer Depth (h m ) h m from ARGO float data (∆  =0.03kg/m 3 ) Variable h m Time-Mean h m

14. Sensitivity: 2. Mixed Layer Depth (h m ) RMS of Heat Balance for Various MLD: 1.Argo Floats climatology (Jun 02 - Dec 05): -density diff 0.03kgm -3 : 0.031°C/day (146 Wm -2 ) “best” case -temp diff 0.2°C:0.033°C/day (157 Wm -2 ) 2.de Boyer Montegut et al. (2004) climatology: -density diff 0.03kgm -3 :insufficient data -temp diff 0.2°C:0.037°C/day (151 Wm -2 ) 3.WOA 2001 climatology: -density diff 0.125kgm -3 :0.038°C/day (235 Wm -2 ) NB: Density MLD criteria uses variable ∆T in entrainment term; temperature MLD criteria uses ∆T=0.02°C.

15. Sensitivity: 3. ∆T across the base of the MLD many studies use ∆T =0.2°C (eg. Qiu and Kelly, 1993) for ∆T =0.2, rms of imbalance is 159 Wm -2 cf “best” case of 146 Wm -2. largest improvement in Indian Ocean where ∆T can be negative: salinity matters! differences in ∆T are largest in fall and winter when entrainment is strongest Annual Average ∆T from Argo floats

16. Spatial Variability in the Imbalance of the Heat Budget Largest imbalance north of ACC: h m is large & temperature gradient is strong complex upper ocean processes not well resolved by existing measurements

17. Regional Heat Budget: The Agulhas Retroflection March Average strong SST gradient and large meanders in Agulhas region reanalysis Q net has long length scales, while w e & advection have smaller scales: net effect on imbalance is small scale structure. large imbalances related to small-scale coupling of the wind field and SST? (e.g O’Neill et al. (2003) find wind stress curl (divergence) related to cross (down) wind components of SST gradient) (x10 -6 °Cs -1 ) cooling warming

18. Conclusions: Implications for data sampling requirements 1.Shipboard Measurements - met & pCO2 sampling opportunity: need identified PIs. 2. Science Application: Polar Front Variability - weekly and daily SST fields resolve similar PF locations - winds are important! Global forcing fields from satellite. - winds more energetic at higher frequencies 3. Science Application: Upper Ocean Heat Balance - large uncertainties in all terms! - Q net varies enormously. Need validation with in situ data and winter time measurements - salinity matters! Need Argo floats for MLD and ∆T - need spatial resolution ~0.25° for small-scale coupling - weekly and daily SST fields give similar heat balance

20. What controls the Polar Front Variability? 2. Response of PF Transport to changes in zonal wind stress du/dt (~ u==dT/dy) and  x negative phase: change in zonal wind stress leads to changes in PF transport coherence 70% > 95%CI phase histogram of phase ACC wind ACC wind

21. Southern Ocean Heat Balance by Basin