Climate and Carbon Cycle Coupling Carbon Cycle - Modern
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1 Early Cenozoic Carbon Cycle and Climate Coupling: Evidence from δ 13 C & δ 18 O Zachos et al. (2008) Climate and Carbon Cycle Coupling Carbon Cycle - Modern Fluxes and Feedbacks Carbon Isotope Tracers Mass balance 1
2 Biosynthesis & C-isotopes 12 C = 98.89%, 13 C = 1.11% R = absolute isotope ratios (heavy/light)! 13 C/ 12 C For example, two substances (100,000 isotopes) 13 C/ 12 C = R CO / = CH 2 O 1080 / = For consistency, need to measure & report ratios (R samp ) relative to standards (reference) R ] g = c samp Rstd - 1m # 1000 d 0 00 Fractionation Factor (α) 13 C 12 C A R a A-B = A RB = 13 C 12 C B For example, two substances R CO2 = 13 C/ 12 C CO2 = R CH2O = 13 C/ 12 C CH2O = α CH2O-CO2 = R CH2O / R CO2 =
3 Modern C-Isotope Distributions Organic carbon (Corg) Inorganic carbon (Carb) Rise in Atmospheric CO 2 ( ) Projections (11 Carbon Cycle models) Observation 3
4 Anthropogenic Carbon Emissions Gigaton (Gt)= 1 billion metric tons 8 GtC/y Since 1850, Total emissions >400 Gt C Fossil Fuel 5000 Gt C 8 Gt C/y Anthropogenic Carbon Emissions Perspective: Earths Primary Carbon Reservoirs Atmosphere (2010) (1850) Gt C Surface Ocean 1500 Gt C Deep Ocean 38,000 Gt C 4
5 Seasonal Cycles/Interhemispheric Gradients ( ) CO 2 + H 2 O CH 2 O + O 2 CH 2 O + O 2 CO 2 + H 2 O Ocean & Atmosphere in Equilibrium Two Sinks CaCO 3 (C carb ) 2HCO Ca 2+ CaCO 3 + CO 2 + H 2 O Organic (C org ) CO 2 + H 2 O CH 2 O + O 2 5
6 What regulates the amount of CO 2 that the ocean absorbs? ph - carbonate equilibria play an important role in determining ocean ph HCO 3- is the 3rd most concentrated anion in the ocean CO 3 controls the saturation state for calcite (Ω) and aragonite, and hence the production, preservation, and dissolution of these mineral phases The marine carbon cycle (+distribution of carbonate sediment) is a key factor in determining the fate of anthropogenic CO 2 Dissolved Inorganic Carbon (DIC or ΣCO 2 ) Species in Seawater Bjerrum Plot!CO2 CO2 = [CO2] + [H CO3 - ] + [CO3 = ] 2.10E-03 [HCO 3- ] [H 2 CO 3 ]* [CO 3 2- ] [H2CO3*] [HCO3-] [CO3-2] 1.10E E-04 Seawater Range ph Note: [H 2 CO 3 ]* = [CO 2aq ] + [H 2 CO 3 ] 6
7 Atmosphere/Ocean Carbon Trends ( ) Surface Ocean (DIC) Atmos Gruber, keeling, Bates, 2002 Short-term Global Carbon Cycle (Gt C) Fossil Fuels Gt Gt/yr Atmosphere 110 Gt/yr 760 Gt δ 13 C = Gt/yr Terrestrial Biomass 610 Soils ~1000 Ocean 38, CH 4 Hydrates ,000? Gt/yr 0.5 Gt/yr Marine Sediments Carbonates ; Organic C <1 Gt/yr Rocks Carbonates 40x10 6 Gt; 0.0 ; Organic C 1x10 7 Gt -20 Table (fluxes/13c) 7
8 Atmosphere pco2/surface Ocean δ13c A.D. Archives 273 ppm Industrial Revolution (Fossil fuel CO2) δ13c = -25 Corals 373 ppm Surface ocean (Corals) Atmosphere (Ice-cores) Böhm et al. (2002) Change in Ocean ph (last 100 y) 8
9 Rise in Atmospheric CO 2 ( ) Projections (11 Carbon Cycle models) Observation Ocean Uptake of Anthropogenic CO 2 Since 1850, Total C emissions ~380 GtC Ocean uptake ~120 GtC 2009? 9
10 C isotopes & input of Fossil Fuel CO 2 The DIC of the surface ocean has decreased by 1.3 in the last century (δ 13 C p = δ13 C i )! Why? Addition of CO 2 from Fossil Fuel (M ff ) Combustion! If so can we use this to estimate the mass of carbon absorbed? δ 13 C P = 1.0, M P =1000 Gt C, δ 13 C i = 2.3, M i =?? δ 13 C ff = -20.0, M ff =?? M P =M i + M ff Add a tracer δ 13 C p M p = δ 13 C i M i + δ 13 C ff M ff M ff = M p -M i δ 13 C p M p = δ 13 C i M i + δ 13 C ff (M p -M i ) M i = M p (δ 13 C p - δ 13 C ff )/(δ 13 C i - δ 13 C ff ) M i = 940 Gt M ff = 60 Gt, or roughly 0.6 Gt/yr for the last 100 yr Natural Long-term Carbon Sinks & Sources Feedbacks on carbon levels: Weathering & Burial 1. Temperature - reaction rates 2. Net precipitation - chemical reactions 3. Corg production & burial 10
11 Long-term carbon cycle fluxes long-term sources of CO 2 : Volcanism (ridges, plumes) CO 2 carbonate metamorphism CaCO 3 + SiO 2 CaSiO 3 + CO 2 carbonate sedimentation 2HCO Ca 2+ CaCO 3 + CO 2 + H 2 O weathering of organic-rich seds. ("respiration"; CH 2 O + O 2 CO 2 + H 2 O) long-term sinks of CO 2 : carbonate rock weathering CaCO 3 + CO 2 + H 2 O 2HCO Ca 2+ silicate rock weathering CaSiO 3 + 2CO 2 + H 2 O 2HCO Ca 2+ + SiO 2 silicate weathering + carb sedimentation CaSiO 3 + CO 2 CaCO 3 + SiO 2 burial of organic matter ("photosynthesis"; CO 2 + H 2 O CH 2 O + O 2 Long-term Global Carbon Cycle (Gt C) Atmosphere 760 Gt 60 Gt/yr δ 13 C = Gt/yr Terrestrial Biomass 610 Soils CH 4 Hydrates ,000? Gt/yr Ocean 38, Gt/yr 0.17 Gt/yr 0.05 Gt/yr 0.5 Gt/yr Marine Sediments Carbonates ; Organic C Gt/yr 0.05 Gt/yr Volcanoes Gt/yr Rocks (~Continental) Carbonates 40x10 6 Gt; 2.0 ; Organic C 1x10 7 Gt
12 C isotopes & the burial of organic vs. inorganic carbon Flux in (Gt/yr) = Flux out (Gt/yr) Flux out = Flux org + Flux carb Flux in = volcanoes and weathering Fluxes difficult to quantify!!! Volcanic Assume steady state flux 1 = f carb + f CO 2 org δ 13 C = -5 Add a tracer δ 13 C in = f carb δ13 C carb + f org δ 13 C org δ 13 C in = -5, f carb = 1 - f org δ 13 C in = (1 f org ) δ13 C carb + f org δ 13 C org f org = (δ 13 C carb + δ 13 C in )/( δ 13 C carb - δ13 C corg ) f org = (δ 13 C carb + 5)/Δ 13 C carb-corg Exogenic Carbon Reservoir Dissolved Inorganic Carbon (DIC) δ 13 C = 0 Organic Matter (CH 2 O) δ 13 C = -25 Calcite (CaCO 3 ) δ 13 C = 0 13 C carb/corg = 25 1 : 4 f org = (0 + 5 )/25 f org = 0.2 C isotopes & the burial history of organic and inorganic carbon f org = (δ 13 C carb + 5)/Δ 13 C carb/corg Fraction of Corg/Carb Burial f org Δ 13 C Carb/corg = DIC (δ 13 C carb ) forg δ 13 C carb = δ 13 C input + f org (δ 13 C carb - δ 13 C org ) 12
13 Cenozoic Carbon and Climate: δ 13 C & δ 18 O Zachos et al. (2008) Paleocene-Eocene Thermal Maximum Carbon Anomaly Carbon Isotope Excursion of -3.0 Global Warming 5-6 C 100 k.y. Cause? Massive Carbon Input Ocean Acidification Zachos et al.,
14 3 Possible Sources of Carbon 1. Dissociation of Methane Hydrate - (Dickens et al., 1996) (feedback) Bacterial, δ 13 C = -60 to -80. ~ PgC (Archer & Buffet, 2004) 2. Mantle Plume/Mid-ocean Ridge Volcanism - CH 4 /CO 2 (Svensen et al., 2004) Thermal Corg decomposition, δ 13 C = -7 to -25 Emission rate to?? PgC/y Carbon Source for the PETM? N. Atlantic Plume/Rift volcanism Main phase of production (<0.5 m.y.) Intrusive volcanism & thermal decomposition of Corg/Ccarb Storey et al.,
15 Carbon Source for the PETM? Hydrothermal Vent Complex? Intrusive Volcanism & Combustion of Corg/Carb Mass/Rate of CO2/CH4 venting? Svensen et al., 2004 Source of Carbon? ³ Decomposition of Methane Hydrates - (Dickens et al., 1996) (feedback?) ³ Bacterial, δ13c = -60. ³ ~ PgC (Archer & Buffet, 2004) ³ Mantle Plume/Mid-ocean Ridge Volcanism - CH4/ CO2 (Svensen et al., 2004) ³ Thermal Corg decomposition, δ13c = -7 to -25 ³ Emission rate? ~0.1 PgC/y ³ Oxidation of Terrestrial Corg (feedback?) ³ Forest peat/bogs/permafrost - δ13c = -25 ³ PgC ³ (Kurtz et al., 2003; Higgins & Schrag, 2006; DeConto et al., in press) 15
16 Carbon Mass / δ 13 C 4 Carbon Isotope Excursion (CIE) Dunkley-Jones et al., 2009 Constraints on the Source of Carbon? Mass of carbon ü Carbon isotope excursion (CIE) ü Ocean carbonate saturation Rate of release - fast vs. slow? ü High-fidelity records ü Orbital Background Variability ü Was the PETM unique? 16
17 Simulations of Massive Carbon Release Models 1. Carbon Cycle Box Model Zeebe et al., Earth System Model Panchuk et al., 2008; Ridgwell et al., 2009 Observational Constraints 1. CCD shoaling 2. Carbon Isotope Excursion (-3.5 to -4.0 ) Walvis Ridge (ODP Leg 208) Spiess et al.,
18 Leg 208, Walvis Ridge P-E Boundary Dissolution Horizon Rapid Shoaling, and gradual recovery of the CCD Leg 208, Walvis Ridge CCD Shoaling and Recovery 18
19 Best Fit PETM Simulation M S = 4500 Pg C δ 13 C S = -50 Zeebe et al. (2009) CCD sensitivity to RATE of initial carbon pulse Carbon Input MI=3000 Pg C δ 13 CI=-50 t=1 to 80 k.y <5 k.y. Observation? 19
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