Response of the North Atlantic atmospheric circulation to increasing LGM ice-sheet elevation
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1 Response of the North Atlantic atmospheric circulation to increasing LGM ice-sheet elevation Marcus Löfverström NCAR Rodrigo Caballero Johan Nilsson Gabriele Messori Stockholm University
2 The Northern Hemisphere LGM topography Two major ice sheets (+ Greenland) Larger ice sheet in North America than in Eurasia Laurentide Ice Sheet Greenland Eurasian Ice Sheet LGM Kleman et al. 2013, Löfverström et al. 2014
3 Laurentide extent known, elevation debated ~4500m ~3500m ~3300m Ullman et al. 2013
4 Circulation differences: high vs. low ice sheet Modern PMIP2 (high LIS) PMIP1 (low LIS) Li & Battisti 2008 Weak & tilted Atlantic jet Strong & zonal Atlantic jet Weak & tilted Atlantic jet
5 Experiments and simulations Slab-ocean CAM3 (T85 L26), ocean heat flux convergence calculated from Brandefelt & Otto-Bliesner (2009) Eight LGM simulations with increasing ice sheet elevation from 0 m to 5100 m Sensitivity simulations with prescribed sea-surface conditions (not discussed here): (i) the importance of the ice-sheet topography (very important) (ii) the importance of the SST/sea-ice field (important) Analysis based on 30 years of DJF data after the model climate has reached statistical equilibrium
6 300 hpa wind and 300 K potential vorticity PD: Weak and meridionally tilted jet, similar to ERA-Int
7 300 hpa wind and 300 K potential vorticity PD: Weak and meridionally tilted jet, similar to ERA-Int PD: Relaxed PV gradient in mid latitudes
8 300 hpa wind and 300 K potential vorticity PD: Weak and meridionally tilted jet, similar to ERA-Int High LIS: Strong, narrow and zonal jet PD: Relaxed PV gradient in mid latitudes
9 300 hpa wind and 300 K potential vorticity PD: Weak and meridionally tilted jet, similar to ERA-Int High LIS: Strong, narrow and zonal jet PD: Relaxed PV gradient in mid latitudes
10 300 hpa wind and 300 K potential vorticity PD: Weak and meridionally tilted jet, similar to ERA-Int High LIS: Strong, narrow and zonal jet PD: Relaxed PV gradient in mid latitudes High LIS: No PV gradient in low latitudes High LIS: Tight PV gradient in mid latitudes
11 Meridional tilt of 500 hpa jet (55 10 W) as function of ice sheet height Jet axis Jet axis lat lat
12 300 hpa Rossby wave breaking [(lat,lon) -1 season -1 ] (old interpretation) - AWB spread out - Almost no CWB - Tilted jet - Concentrated AWB on equatorward flank - Increased CWB on poleward flank - Overturning subtropical PV - Zonal jet
13 300 hpa Rossby wave breaking [(lat,lon) -1 season -1 ] (old interpretation) - AWB spread out - Almost no CWB - Tilted jet - Concentrated AWB on equatorward flank - Increased CWB on poleward flank - Overturning subtropical PV - Zonal jet
14 Stationary wave reflection (new interpretation) Atmospheric stationary waves: Zonally asymmetric component of climatological atmospheric state Can be seen in almost all dynamic fields, typically upper troposphere eddy streamfunction [m 2 s -1 ] Driven by flow-top. interactions, diabatic heating, stat. and trans. eddy fluxes Wave activity flux (Plumb flux): Indicates propagation direction of stationary waves Vector quantity almost parallel to the group velocity (energy propagation) in the WKB limit Orthogonal to phase lines of stationary waves
15 300 hpa eddy streamfunction and wave activity flux Wave activity flux (Plumb flux): Indicates propagation direction of stationary waves Vector quantity almost parallel to the group velocity (energy propagation) in the WKB limit Orthogonal to phase lines of stationary waves
16 300 hpa eddy streamfunction and wave activity flux Stationary wave absorption Momentum flux Phase line t=0 Wave activity Midlatitudes Strong PV gradient or low amplitude waves Subtropics
17 300 hpa eddy streamfunction and wave activity flux Stationary wave absorption Momentum flux Phase line t=0 Wave activity Midlatitudes Energy dissipation and absorption (possible wave breaking) t=later Strong PV gradient or low amplitude waves Subtropics
18 300 hpa eddy streamfunction and wave activity flux
19 300 hpa eddy streamfunction and wave activity flux Stationary wave absorption Stationary wave reflection
20 300 hpa eddy streamfunction and wave activity flux Stationary wave reflection Momentum flux Phase line t=0 Wave activity Midlatitudes Weak PV gradient or high amplitude waves Subtropics
21 300 hpa eddy streamfunction and wave activity flux Stationary wave reflection Momentum flux Phase line t=0 Wave activity Midlatitudes Interference Wave reflection t=later Weak PV gradient or high amplitude waves Subtropics
22 300 hpa eddy streamfunction and wave activity flux Stationary wave reflection Phase line Phase line Phase line Midlatitudes Momentum flux (Interference) Zonalisation of phase lines and thus the jet Wave activity Weak PV gradient or Subtropics high amplitude waves
23 Everything put together Climatologically non-reflective case Strong subtropical PV gradient Predominant absorption of stationary waves in the subtropics. Equatorward wave activity flux in Atl. basin Weak and meridionally tilted Atlantic jet
24 Everything put together Climatologically reflective case Homogenized subtropical PV & strong mid-lat. PV gradient Predominant reflection of stationary waves in the subtropics. Poleward wave activity flux in E. Atl. basin Strong and zonal Atlantic jet
25 Summary and conclusions Modern climate & low LIS LGM Weak stationary waves Strong subtropical PV gradient that resists stationary wave reflection Weak and meridionally tilted Atlantic jet High LIS LGM Strong mechanical stationary wave forcing in North America Organization of planetary waves (Rossby wave breaking) PV gradients expelled to mid-latitudes, weak subtropical PV Predominant stationary wave reflection that helps zonalise the Atlantic jet Reflected stationary waves tend to break cyclonically, which helps zonalise the jet even further
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