1. Examining a downslope warming wind event over the Antarctic Peninsula through modeling and aircraft observations: can mountain waves cause surface melting on the Larsen Ice Shelf? Daniel Grosvenor, Thomas Choularton, Martin Gallagher (University of Manchester, UK); Thomas Lachlan Cope and John King (British Antarctic Survey). ContentsContents The Antarctica Peninsula region – recent rapid regional warming and the collapse of Larsen BThe Antarctica Peninsula region – recent rapid regional warming and the collapse of Larsen B The Föhn (downslope windstorm) effectThe Föhn (downslope windstorm) effect Aircraft observations and modelling of such an event over Larsen C ice shelf:-Aircraft observations and modelling of such an event over Larsen C ice shelf:- What did the event look like and how well does the model capture it?What did the event look like and how well does the model capture it? What caused the event?What caused the event? How likely are such events and could they play a role in warming trends on the east side of the peninsula?How likely are such events and could they play a role in warming trends on the east side of the peninsula? What impact could such events have on the Larsen C ice shelf?What impact could such events have on the Larsen C ice shelf?

2. The Antarctic Peninsula region Larsen B Larsen C Wilkins 1540 km 1750 km Topography Scale comparison Warmer oceanic air is generally deflected along the mountain barrier Therefore, east side is usually under the influence of cold air from the continent Annual mean temperatures on east are 5- 10 o C cooler than on the west at comparable latitudes However, when westerlies impact on the peninsula in the right conditions the warmer air can cross the mountain barrier making east side warmer Extra warming is also possible from adiabatic descent of air down the mountain slope and/or latent heat release – Föhn effect WARMER OCEANIC AIR COLD CONTINENTAL AIR

3. The Antarctic Peninsula warming trend Warming trend o C per decade, 1965-2000, except where noted Marshall et al. (2006), Journal of Climate Possible causes of amplified warming:- -Southern Annular Mode (SAM) index has been increasing, especially in summer – leads to stronger westerlies -Linked to ozone loss (mainly) and greenhouse gases (less so) -May lead to more Föhn events. 1968-2000 1970-2000 B C Peninsula has shown a major warming – Faraday station showed 0.56 o C per decade (1951-2000) compared with mean global warming of 0.6 o C in whole of 20th century. The warming in summer on the east side has been greater than for the west side

4. Warming of westerly flow can be enhanced by latent heat release on the upslope side and/or adiabatic descent of air from above, on the downslope side:- Moist air rising in saturated adiabat – gains heat from latent heat of condensation Some of the moisture precipitates out Possible dry adiabatic descent leading to warm temperatures at the surface Dry adiabatic descent from aloft leads to warmer temperatures at the surface and gravitational acceleration produces strong winds. Wave breaking aloft allows air to descend on upslope of terrain and keep descending on downslope Type 1 Type 2 The Föhn/downslope flow Strengthening of westerly winds due to increasing trend in summer SAM index could be causing increased frequencies of Föhn events and thus might account for the enhanced warming trend observed on the east side.

5. Collapse of the Larsen B ice shelf Larsen C Wilkins MODIS satellite images 31 st Jan, 2002 Larsen B Scale comparison 175 km London

6. Collapse of the Larsen B ice shelf MODIS satellite images 17 th Feb, 2002 175 km Larsen C Wilkins Larsen B London

7. Collapse of the Larsen B ice shelf MODIS satellite images 23 rd Feb, 2002 175 km Larsen C Wilkins Larsen B London

8. Collapse of the Larsen B ice shelf MODIS satellite images 5 th Mar, 2002 Sediment data below the ice shelf suggests that it had been around for the last ~11,700 years. Evidence for glacier speed up – northern AP glaciers contribute ~0.16 mm/year to global sea levels 175 km Larsen C Wilkins 3200 km 2 lost Larsen B London

9. Collapse of the Larsen B ice shelf Larsen C Wilkins 175 km Larsen B London

10. Modelled using a special polar version of WRF (Weather Research and Forecasting) mesoscale model Initialised and boundaries driven by ECMWF 0.5 degree global model 3 nests - 30, 7.5 and 1.875 km resolution The 6 th January, 2006 Föhn flow case A British Antarctic Survey (BAS) flight over the Peninsula made observations in a Föhn flow

11. The synoptic situation Wind direction directed to the west where it rotates and impacts onto west side of the peninsula 6 UTC, 6th Jan Pressure (hPa) at 2.3 km from ECMWF analysis

12. Flight track and model results Colours are wind speed Arrows give wind speed and direction Wind speed (m/s) Rothera - BAS research station Aircraft observed jet windspeed maxima here 4 th vertical model level; ~293 m above surface 18 UTC, 5 th Jan

13. Wind speed (m/s) 4 th vertical model level; ~293 m above surface

14. Wind speed (m/s) 4 th vertical model level; ~293 m above surface

15. Wind speed (m/s) 4 th vertical model level; ~293 m above surface

16. Wind speed (m/s) 4 th vertical model level; ~293 m above surface 6 UTC, 6 th Jan

17. Wind speed (m/s) 4 th vertical model level; ~293 m above surface

18. Wind speed (m/s) 4 th vertical model level; ~293 m above surface

19. Wind speed (m/s) 4 th vertical model level; ~293 m above surface Aircraft observed jet windspeed maxima here 15 UTC, 6 th Jan

20. Wind speed (m/s) 4 th vertical model level; ~293 m above surface

21. Wind speed (m/s) 4 th vertical model level; ~293 m above surface 21 UTC, 6 th Jan

22. Wind speed (m/s) 4 th vertical model level; ~293 m above surface

23. Wind speed (m/s) 4 th vertical model level; ~293 m above surface

24. Wind speed (m/s) 4 th vertical model level; ~293 m above surface

25. Wind speed (m/s) 4 th vertical model level; ~293 m above surface 9 UTC, 7 th Jan

26. a)b)c) Descent (20:40) Ascent (22:01) Model Generally a good match for wind direction, temperature and the jet height. However, the timing is bad:- Aircraft descent and ascent were at 20:40 and 22:01 UTC respectively. After 15 UTC the model jets die down. Modelled wind jets are too weak at 15 UTC. Due to meteorology change – wind direction no longer perpendicular to mountain 15 UTC 6 th January (model) Wind speed (m/s) Wind direction (degrees) Temperature ( o C) Model profiles at location C 0 km 3 km 020 5 0 -15320

27. The changing synoptic situation that leads to the Föhn die down Wind direction directed more to the west where it rotates and impacts onto west side of the peninsula Föhn situation 6 UTC, 6th Jan

28. The changing synoptic situation that leads to the Föhn die down Non-Föhn situation Wind direction coming from continent directed more along and to the east of the peninsula Low pressure system has moved east 9 UTC, 7th Jan

29. Cross sections Well-mixed region caused by wave breaking Leads to strong downslope winds Approx. continuous stratification higher up Well mixed upstream region Blocked air below ~1 km Wind direction West East Potential temperature (K) Wind speed (m/s) Model predicts that a “type 2” Föhn event took place with severe blocking on the upwind side Blocking may be necessary for downslope flow – does sea-ice play a role in the degree of blocking? The past literature has often assumed that Föhn warming would not occur over the Antarctic Peninsula when the wind speed is low enough, or the stability high enough to produce upstream blocking. Indicates likely importance of upper level winds and direction rather than speed for these events. 6 UTC, 6th Jan

30. Melting of ice shelves over the 3 simulation days Production of melt water thought to have been the primary cause of the breakup of Larsen B through crevasse propagation. Clear reduction in melting moving south down the peninsula ice shelves Although northern sections of Larsen C experience similar melting to Larsen B Most important energy source for melting is from the Sun rather than the warm Föhn air – but melting would not begin without the warm air above the ice surface (on/off switch) Larsen B Larsen C Total melting (mm water equivalent)

31. Summary and conclusions Summer warming on the east side of the peninsula has been greater than that for the west and likely led to the collapse of the Larsen B ice shelf. Observations show that a Föhn event occurred on 6 th January. Model reproduces the observed jet structure and direction well except for the duration/timing and wind speed under-prediction. This looks to be the result of large scale analysis problems (meteorology) Modelling suggests that a “type 2” Föhn event occurred - driven by mountain wave breaking and characterised by upstream blocking Suggests Föhn events can occur at relatively low wind speeds in contrast to past literature for this region - may be more dependent on the stability and upper level wind direction – blocking looks to be a necessary condition – sea-ice, katabatic flow dependence? Warm air likely acts as an on/off switch for ice shelf surface melting rather than a significant energy source – most of the energy comes from the Sun

32. Acknowledgements I would like to thank Dave Bromwich and his team for supplying me with the polar WRF modifications. I also thank ECMWF for the use of their high resolution analysis data. And NCAS for the time provided on the HECTOR supercomputer.