WHY CARBON? The Carbon Cycle 1/17/2011. All living organisms utilize the same molecular building blocks. Carbon is the currency of life
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1 The Carbon Cycle WHY CARBON? Inventories: black text Fluxes: purple arrows Carbon dioxide (+4) AN = 6 (6P/6N) AW = Oxidation: -4 to +4 Isotopes: 11 C, 12 C, 1 C, 14 C Methane (-4) Carbon is the currency of life Time Scales of Carbon Exchange in the Biosphere Carbohydrates Protein Nucleic acids All living organisms utilize the same molecular building blocks. 4 places carbon is stored: 1) Lithosphere, 2) Atmosphere, ) Ocean, 4) Terrestrial biosphere 1
2 The oceans carbon cycle The main components: DIC, DOC, PC (includes POC and PIC) Primary processes driving the ocean carbon cycle: abiotic: solubility, ventilation, transport; biotic: photosynthesis, respiration, calcification 0.01 g C in a sugar cube The ocean holds 50 grams of CO 2 for every 1 gram of CO 2 in the atmosphere CO 2 in the atmosphere ~750,000,000,000,000,000 g C CO 2 in oceans ~9,120,000,000,000,000,000 g C Dissolved organic carbon ~700,000,000,000,000,000 g C Living and dead particles ~,000,000,000,000,000 g C Pools of Carbon in the Sea DIC in the oceans ~7500 x g C H 2 CO -carbonic acid HCO - -bicarbonate CO 2 carbonate DOC ~700 x gc POC (living i and detrital organic particles)-22 x g C PIC (CaCO )- <1 x g C Because of its solubility and chemical reactivity, CO 2 is taken up by the oceans more readily than other atmospheric gases. Over the long term (1000s of years) the oceans will consume ~90% of anthropogenic CO 2 emissions. Vertical profiles of carbon in the North Pacific Depth (m) Particulate Carbon ( mol L -1 ) Dissolved Organic Carbon ( mol L -1 ) DIC DOC POC Dissolved Inorganic Carbon ( mol L -1 ) 2
3 Dissolved inorganic carbon H 2 O + CO 2(g) H 2 CO H 2 CO H + + HCO - HCO - H + + CO Solubility of CO 2 in seawater and its equilibrium among these different species depends on temperature, pressure, salinity, ph, and alkalinity. The residence time of CO 2 in the atmosphere is ~10 years; it exchanges rapidly with the ocean and terrestrial biome. Vertical profiles of DIC and ph at Station ALOHA Depth (m) ph Surface seawater (ph~8.2): [H 2 CO ] : [HCO - ] : [CO ] 0.5% : 88.6% : 10.9% Ocean acidification due to increasing atmospheric carbon dioxide The Royal Society Dissolved inorganic carbon ( mol C L -1 ) What processes control DIC gradients in the sea? Abiotic and biotic processes control carbon distributions in the sea. Need to understand controls on the variability of these processes DIC (mol m - ) Solubility pump: Cooler water gains CO 2 -high latitude regions are sinks for CO 2 Cooler, CO 2 rich waters sink Maintains vertical gradient in CO 2 Air-sea heat fluxes drive air-sea CO 2 fluxes Temperature dependent relationship of DIC at atmospheric pco ppm (preindustrial levels) Equator Poles
4 Physics plays a key role in controlling ocean carbon distributions The oceanic laboratory: World Ocean Circulation Experiment hydrography transects Upwelling Mixing pco 2 = pco 2(W) pco 2(A) Long-term changes in the ocean carbon system in waters off Hawaii. Oceanic uptake of CO 2 also influences seawater ph. pco 2 (µatm) 80 Sea Air ph (total scale, in situ) Surface ocean pco 2 Regions of negative pco 2 flux are regions where the ocean is a net sink for atmospheric CO
5 The biological carbon pump Ocean acidification due to increasing atmospheric carbon dioxide The Royal Society Organic Carbon Pump Calcium carbonate pump CO 2 CO 2 CO 2 Ca 2+ 2HCO - CaCO + H 2 O + CO 2 CO 2 + 2H 2 O CH 2 O + O 2 Increasing oceanic DIC has two important implications H 2 O + CO 2(g) H 2 CO H 2 CO H + + HCO - HCO - H + + CO Increased H 2 CO (lowers ph) Decreased CO (increases solubility of CaCO ) CO 2 5
6 Line 5 Saturation state: Ω = ([Ca 2+ ] seawater X [CO ] seawater ) / ([Ca 2+ ] saturated X [CO ] saturated ) When Ω > 1, CaCO supersaturated, shell formation favored. When Ω < 1, CaCO undersaturated, dissolution occurs. Aragonite: Pteropods and corals Calcite: Coccolithophores and foraminifera Dissolution and formation of shells changes [Ca 2+ ] <1%; thus changes in [CO ] largely control Ω Feely et al. (2008); Science 20: Distribution of the depths of the undersaturated water (aragonite saturation < 1.0; ph < 7.75) on the continental shelf of western North America. On transect line 5, the corrosive water reaches all the way to the surface in the inshore waters near the coast. The black dots represent station locations. Primary biologically mediated carbon transformations in the sea Plankton and carbon Photosynthesis : Photosynthesis: 6CO H 2 O Respiration: C 6 H 12 O 6 + 6O 2 Photosynthesis and respiration Sunlight C 6 H 12 O 6 + O 2 + 6H 2 O + heat 6CO 2 + 6H 2 O + heat Note that these reactions are VERY generalized: does not include other bioelements (N, P, S, Fe, etc.) that also are involved in these biological transformations. + CO 2 +H 2 O = + O 2 Decomposition : = CO 2 +H 2 O + O 2 6
7 CO 2 The biological carbon pump 0 Export and vertical attenuation of particle flux 1000 Mixed layer CO 2 Depth (m m) Biology <5 to 10% Total inorganic carbon ( mol C kg -1 ) ~1-5% ~0.1% Pick up line and float Glass buoyancy SEDIMENT TRAPS VERTEX program late 70 s mid 80 s Extensive upper ocean trap studies Knauer et al., 1979 ~ Sediment trap Current meter + transm issom eter ~ Martin curve Acoustic Release Anchor (scrap chain) Deep ocean sediment traps. Anchored to the seafloor. Collection interval is determined by the investigator. Provide estimates of sinking particle flux to the deep sea. F = F 100 (z/100) b F 100 = 1.5 (mol m 2 y 1 ) b =
8 Food web structure is a key determinant on carbon fluxes: Horizontal flow Sinking particles do not sink vertically sinking velocity = 10 s >500 m/day horizontal velocity = 1 10 s cm/sec 1) Cell size and geometry influence sinking rate 2) Zooplankton repackage material and vertically migrate ) Small cells support longer food webs = more carbon recycled to CO 2 Avg. sinking particle: 4 m vertical drop & 520 m horizontal trajectory during 50 min talk Zooplankton repackage plankton into rapidly sinking fecal material Direct aggregation and pulsed export is also important Sedimentation i of diatom rich ih salp fecal pellets > 1 mm long, 50 µm wide, 10 µg C per pellet these things sink FAST... Flux of labile phytodetritus to the deep North Atlantic 8
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