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GEOF236 CHEMICAL OCEANOGRAPHY (HØST 2012) Christoph Heinze

GEOF236 CHEMICAL OCEANOGRAPHY (HØST 2012) Christoph Heinze University of Bergen, Geophysical Institute and Bjerknes Centre for Climate Research Prof. in Global Carbon Cycle Modelling Allegaten 70, N-5007 Bergen, Norway Phone: +47 55 58 98 44 Fax: +47 55 58 98 83

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GEOF236 CHEMICAL OCEANOGRAPHY (HØST 2012) Christoph Heinze

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  1. GEOF236 CHEMICAL OCEANOGRAPHY (HØST 2012) ChristophHeinze University of Bergen, Geophysical Institute and Bjerknes Centre for Climate Research Prof. in Global Carbon Cycle Modelling Allegaten 70, N-5007 Bergen, Norway Phone: +47 55 58 98 44 Fax: +47 55 58 98 83 Mobile phone: +47 975 57 119 Email: christoph.heinze@gfi.uib.no DEAR STUDENT AND COLLEAGUE: ”This presentation is for teaching/learning purposes only. Do not useany material ofthispresentation for any purpose outsidecourse GEOF236, ”Chemical Oceanography”, autumn 2012, Universityof Bergen. Thankyou for yourattention.”

  2. Sarmiento&Gruber 2006 Chapter 9: Calcium carbonate cycle, part 2

  3. Carbon pumps SOLUBILITY Heinze, C., E. Maier-Reimer, and K. Winn, 1991, Glacial pCO2 reduction by the World Ocean - experiments with the Hamburg Carbon Cycle Model, Paleoceanography, 6, 395-430.

  4. Carbon in seawater: CO2 added, carbonate saturation The major factor for changing TA is precipitation/dissolutionof CaCO3: CaCO3solid↔ Ca2+ +CO32- calcium carbonate (calcite, aragonite) So in principle one can neutralise CO2gas by dissolving CaCO3: CaCO3solid + CO2gas + H2O ↔ Ca2++ 2HCO3- Over-/undersaturation with respect to CaCO3 is determined by the solubility product: Ksp = [Ca2+ ]sat x [CO32-]sat = const. x [CO32-]sat Therefore: By adding CO2 we decrease the carbonate saturation. Ω = saturation state = ([CO32-]actual ∙[Ca2+]actual)/Ksp ≈ [CO32-]actual/ [CO32-]sat

  5. Carbon pumps Source: Zeebe & Wolf-Gladrow, 2001

  6. Two different concepts to discriminate between over- and undersaturated areas: Lysocline: Depth interval , where CaCO3 shell material undergoes strong signs of corrosion. Calcium carbonate compensation depth, CCD: depth level, where rain and re-dissolution balance. Therefore: Below the CCD there is no CaCO3 available anymore. Tucker and Wright (1990)

  7. Atlantic Pacific Model Observation GEOSECS Black dots: approximate saturation depth level, using the critical CO32- concentration)

  8. CaCO3 top sediment coverage:

  9. Diagenesis model: • Model to predict: • solid concentrations in the bioturbated zone • porewater concentrations in the bioturbated zone • flux of dissolved constituents between water column and porewaters • Burial of solid material to “stone” • SEE ARCHER ET AL. 1993

  10. Diagenesis modelling: Heinze et al., 2009, Paleoceanography

  11. Diagenesis modelling: Heinze et al., 2009, Paleoceanography

  12. long-term variations (past)

  13. CaCO3 from Eq. Pac. Farrell&Prell 1989 last 130,000 years Atmosph. CO2 Siegenthaler et al., 2005

  14. Tracer signals – example Atlantic Balsam 1983 Pazific Farrell & Prell 1989

  15. Zachos et al., 2005 http://www.fossilmuseum.net/GeologicalTimeMachine.htm

  16. T anomaly across the Paleocene-Eocene boundary (Winguth et al., 2010)

  17. Van Andel, 1975

  18. Van Andel, 1975

  19. future evolution

  20. Caldeira and Wickett, 2003

  21. Direct measurements of Cant in the ocean: Sarmiento&Gruber, 2006

  22. Direct measurements of Cant in the ocean: Santana-Casiano et al., GBC, 2007

  23. Potential alterations in biological cycling of carbon with circulation and pCO2 change: 350 μatm (green)700 μatm (grey)1050 μatm (red) Mesocosm experiments at differing atmospheric pCO2: ”Captering natural ecosystem communities in plastic bags and watching their behavior for changes in forcing under controlled conditions” Apparent decrease of dissolved inorganic C with pCO2 Apparent increase of organically bound C with pCO2 Apparent increase of nutrient utilisiation efficiency with pCO2 Riebesell, Schulz, Bellerby, Botros, Fritsche, Meyerhöfer, Neill, Nondal, Oschlies, Wohlers & Zöllner, Nature, 2007 Mesocosm facilities at Espegrend, Bergen

  24. PTEROPODS (small snails) (aragonite producers) Antarctic pteropod, Fabry et al., Oceanography, 2009 CORALS (aragonite producers) Hoegh-Guldberg et al., Science, 2007

  25. Anthroogenic CO2emssion scenarios: Raupach et al., 2007, PNAS

  26. Aragonite saturation according to future climate projections:

  27. Aragonite saturation according to future climate projections: Steinacher et al., Biogeosciences, 2009

  28. CaCO3 sediment can start to dissolve close to deep-water production areas due to anthropogenic CO2: Gehlen et al., 2008

  29. CaCO3 sediment can start to dissolve close to deep-water production areas due to anthropogenic CO2: Gehlen et al., 2008

  30. CaCO3 sediment can start to dissolve close to deep-water production areas due to anthropogenic CO2: Gehlen et al., 2008

  31. Ocean is central for long-term uptake and storage of anthropogenic CO2: CaCO3 sediment neutralises without CaCO3 sediment with IPCC AR4, Ch. 7, following Archer, 2005 Core top CaCO3 Archer, 1996

  32. Warm water corals Guinotte&Fabry, 2008

  33. Deep water corals Guinotte&Fabry, 2008

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