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Using multiple equilibria to interpret paleoclimate David Ferreira University of Reading Collaborators: John Marshall (MIT) Brian Rose (Albany) Taka Ito (Georgia Tech) David McGee (MIT) Outline Paleoclimate context Quick summary of


  1. Using multiple equilibria to interpret paleoclimate David Ferreira University of Reading Collaborators: John Marshall (MIT) Brian Rose (Albany) Taka Ito (Georgia Tech) David McGee (MIT)

  2. Outline • Paleoclimate context • Quick summary of multiple state dynamics • Dynamics of transitions, link with DO events • Glacial-interglacial states • Stochastic resonance and GI cycles • Bonus track

  3. Geology and paleoproxies indicate Earth climate went through very different states Neoproterozoic Snowball Earth Ice-free Cretaceous Eq = 20 − 23 o C Δ T Pole “ Moderate ” present-day Eq = 30 − 35 o C Δ T Pole T Deep = 10 − 13 o C

  4. Glacial-Interglacial cycles Antarctica: EPICA Dome C - Massive global climate shifts à large ice sheets over Canada/ US and Scandinavia (~120 m sea level drop) Δ T à a few deg. global cooling - Missing link between forcing (Milankovitch cycles?) and climate response Jouzel et al. (2007) Thousands of year ago Greenland: NGRIP Millenial timescale fluctuations 0 °C - @ Greenland: amplitude ~ δ 18 O -10 °C Glacial-Interglacial - Larger in North Atlantic -20 °C -30 °C Huber et al. (2006)

  5. Dansgaard-Oeschger events (DO events) Greenland ice core record kyr

  6. Multiple equilibrium states and abrupt changes A small forcing may trigger a large/abrupt change: Very Stable stable state state

  7. Can multiple equilibria play a role in Earth’s climate history? à There have been many studies in this direction: Benzi et al. (1982) and Paillard (1998), Saltzman et al., Gildor and Tzipermann et al., etc. Problem: multiple equilibria are commonly found in simple models, but not always/not easily found in complex coupled climate models. à simple/low order models: (semi-)analytical models à GCMs: from intermediate complexity (e.g. zonally averaged models to state-of-the-art IPCC class models)

  8. Multiple equilibrium states in low-order models Multiple states of the Meridional Overturning Circulation 1 Atlantic Overturning Depth (m) in Sv =10 6 m 3 /s Latitude See Ferreira et al. (2018) for why OCCA Ocean state estimate (Forget, 2009) there isn’t a Pacific equivalent

  9. Multiple equilibrium states in low-order models, II Multiple states of the Meridional Overturning Circulation Stommel (1961) 1 Density-driven q = k ( ρ h − ρ l ) flow ρ l ρ h q (1 − q ) − H = 0 à q “On” branch: thermal mode “Off” branch: haline mode Freshwater forcing H (Sv) Rahmstorf (2002)

  10. Multiple equilibrium states in low-order models Multiple states of the Meridional Overturning Circulation 1 à Widely used to interpret past abrupt changes Rahmstorf et al. (2005) (Broecker et al. 1985, Knutti et al, 2004) à Easy to find in coupled GCMs of intermediate complexity (Water-hosing experiment, ) à Less obvious in IPCC-class GCMs (but, see Mecking et al. 2016) à Freshwater forcing difficult to reconcile with estimates from paleoproxies (~ 0.1 Sv)

  11. Multiple equilibrium states in low-order models Multiple equilibrium states in low-order models 2 Sea ice-albedo feedback: Budyko-Sellers Energy Balanced Model (EBM) Hoffman et al. (2017) Solar f lux (wrt present) 0.9 1.0 1.1 1.2 1.3 < 10 Myr e d 90 o Ice line latitude present 60 o f a ~ 2 kyr 30 o ~ 150 yr Eq c b Rose and Marshall (2009) > 10 Myr 0.1 1 10 100 1000 p CO 2 (wrt present) Few examples in GCMs: • Langen and Alexev (2004): atmosphere only GMC • Marotzke and Bozet (2006): a warm state and a Snowball state

  12. Modeling approach MIT GCM: Ocean- Atmosphere-Sea ic e: Aqua Geometrical constraints Ridge Drake How much can we explain with dynamics and simple geometries ? Double Drake

  13. MIT GCM: Coupled Ocean-Atmosphere-Sea ice: Fully coupled: • Primitive equation models, Same grid for no adjustments ocean and • Cube-sphere grid: ~3.75º, atmosphere • Synoptic scale eddies in the atmosphere, • Gent and McWilliams eddy parameterization in the ocean, Poles well represented • Simplified atmospheric physics (SPEEDY, Molteni 2003), • Conservation to numerical precision (Campin et al. 2008) Temperature Model complexity: Big step snap-shot at 500 mb. compare to EBM models

  14. Idealized geometries but complex dynamics à Not a low order model

  15. Starting with highly idealized configurations Warm Snowball Cold state state state RidgeWorld Stable states for thousands of year AquaPlanet Eq = 28 o C Eq = 55 o C Ferreira et al. 2011 Δ T Pole Δ T Pole

  16. How are the multiple It’s the shape states maintained ? of the OHT ! Cold State: OHT Observed OHT convergence arrests sea-ice expansion MOC Warm State: OHT heats the poles remotely through Cold state enhanced mid-latitudes convection and green- Warm state house effect Ferreira et al. (2011), Rose and Ferreira (2012)

  17. Ocean-Atmosphere EBM Key differences with the “ classical ” EBM (Rose and Marshall, 2009): # & • A coupled ocean-atmosphere EBM, ∂ T a ∂ T C a ∂ t = D y C a K a ( + F up − F out % • OHT has a meridional structure, ∂ y $ ' • sea ice insulates the ocean. ∂ T o ( ) − F up + Λ × S C o ∂ t = D y H o OHT not diffusive but linked to (effective) MOC: ψ res & ) T s − T deep H o ∞ ψ res ( + Δ z ' * Snowball Cold state Warm state

  18. Rose et al. 2012 Transition between states RidgeWorld NGRIP Solar warmer δ 18 O constant Warm state Ice Edge latitude Cold state Slow cooling Abrupt warming ~1000 y ~ 200 y

  19. SST and Sea ice Rose et al. 2012

  20. Ice grows Evolution of Salt Brine rejection Start from Warm State 40 y 600 y 1000 y deep convection 1400 y 1800 y 2240 y Peak of glaciation 2800 y 3000 y 4800 y Rose et al. 2012

  21. Scenario from paleoproxies à Suggest an ocean/sea ice instability à Does rely on AMOC on/off behavior Dokken et al. (2013)

  22. Self-sustained oscillations of ocean/sea ice system Vettoreti and Peltier (2016)

  23. Boomerang Continents • Δ SST = 8.2 °C • Δ SAT = 13.5 °C • SH sea ice: +14° in Winter • NH sea ice cap grows to ~45°N • Atm. pCO 2 : -108 ppm (from 265 to 157 ppm).

  24. OHT/sea ice edge relationship in “Boomerang” Global OHT à Ice edges rest poleward of the large mid-latitudes OHT “Warm” convergences à Multiple states emerge from Northern Hemisphere “Cold” 50S Eq 50N Latitude

  25. Global MOC and Temperature Ventilation of deep ocean shifts to the southern ocean: Depth [km] “Cold” state bottom waters: • colder: -1.5°C, ~freezing point • saltier (+0.5 psu) • See Adkins et al. (2002) “Warm” • Brine rejection drives AABW- like cell Depth [km] • Net SO upwelling rate unchanged • NH cell shoals and weakens (see Watson et al. 2015, Ferrari “Cold” et al. 2014) Latitude

  26. In steady state, Water coming to the surface: - Moves south for a buoyancy loss - Moves to the North for a buoyancy gain Watson et al. (2015)

  27. Surface Winds τ x “Interglacial” “Glacial” N/m 2 In glacial climate: • Trade winds strengthen (as do the Hadley circulation) • SH westerly winds shift equatorward ~1.5 deg • and weaken ~10% à Driven by equatorward expansion of sea ice Paleoproxie: no consensus (Shulmeister et al. 2004, Kohfeld et al. 2016) PMIP simulation: no consensus (Sime et al. 2016)

  28. Ocean Heat transports “AMOC” decreases à Decreased OHT in Small basins à Over compensated by PW increase in Large basin Atlantic-like Basin Pacific-like Basin Global PW

  29. 0 Depth [m] 1000 2000 “Interglacial” 3000 δ 13 C 0 Sea ice Depth [m] 1000 In “Cold” state: Curry and Oppo 2005 • Shallower, weaker “NADW”, 2000 • Deep convection shifted by 15° southward • Nutrient-rich AABW-like water “Glacial” • Depleted upper ocean, 3000 See also Lynch-Stieglitz etal. 2007

  30. How is carbon stored in the “Glacial” ocean? • ocean carbon-cycle model coupled to atmospheric CO 2 , • inventories of carbon, alkalinity, and phosphate are identical in the 2 solutions. • the atmospheric CO 2 is not radiatively active . Change (“Warm” à “Cold”) in 3 carbon reservoirs: Δ C tot = Δ C sat + Δ C bio + Δ C des Solubility Air-sea pump: disequilibrium Biological -58 ppm pump: pump: -85 ppm Bias-corrected: +36 ppm -27 ppm • Solubility pump: Temperature dominated (but include salt) • Net Biological pump: organic + carbonate (CaCO 3 + Alkalinity)

  31. Disequilibrium pump How is carbon stored in the “Glacial” ocean? “Warm” pCO 2 =268 ppm à Increased sea-ice cover reduces the ventilation of upwelled deep waters: DIC accumulates in the deep ocean (Stephens and Keeling, 2000). Caveats: • Solubility is overestimated “Cold” pCO 2 =160 ppm • Biological pump decreases everywhere in Cold state; Oxygen content also increase in deep ocean (Jaccard and Galbraith 2011, Kohfel et al. 2005) à lack of iron cycle? More complex ecosystem

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