Global Carbon Cycle - I

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1 Global Carbon Cycle - I Reservoirs and Fluxes OCN Biogeochemical Systems 13 November 2012 Reading: Schlesinger, Chapter 11

2 Outline 1. Overview of global C cycle 2. Global C reservoirs 3. The contemporary global C cycle 4. Fluxes and residence times 5. Global seasonal variations in atmospheric CO 2 6. Linkages between the C and O Cycles 7. History of the global C cycle

3 The Global Carbon Cycle Major reservoirs: biomass on land biomass in the oceans and marine sediments atmosphere soil and rocks Processes atmospheric exchange with oceans and plants organic matter cycling weathering and the rock cycle the physical chemistry of the oceans Linked to the global cycles of oxygen, nitrogen and phosphorus

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6 Global Carbon Reservoirs Total 1 x g Sedimentary Rocks 8 x g Surficial Active Pools 4 x g Dissolved C in Ocean 3.8 x g* Extractable Fossil Fuels 4 x g Soil Organic Carbon 1.5 x g (Table 5.3) *Largest near-surface pool of C; ocean contains 56x more C than the atmosphere

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8 Listed in order of size (oceans): g C Carbonate sediments 6.5 x Organic matter in seds 1.2 x DIC in Ocean 3.7 x DOC in oceans 1.0 x Ocean biota 3.0 x Carbonate sediments are the largest reservoir larger than organic matter reservoir by ~ 5:1 Ocean water is next largest reservoir: Inorganic (DIC) is ~40x organic (DOC) ocean reservoir Listed in order of size (land + atmosphere)): CaCO 3 in soils 7.2 x Land biota 7.0 x Atmosphere CO 2 6 x Soil organic matter 2.5 x Soils are the next-largest reservoir Living biotic reservoir is ca. same as inorganic soil reservoir Dead organic matter is 1/3 of the inorganic soil reservoir Phytomass 100x bacteria and animal reservoirs Atmosphere is the smallest reservoir, similar to size of all living biomass

9 Organic Carbon vs. Atmospheric Carbon Buried reservoirs of organic carbon are large relative to atmosphere Transfers between organic reservoirs (on land and in the oceans) can occur on short time scales

10 The Contemporary Global Carbon Cycle Surficial active pools (10 15 g C) and fluxes between pools (10 15 g C yr -1 ) *Largest fluxes link atm CO 2 to land vegetation and the surface ocean * * * * *

11 Fluxes and Residence Times Global NPP = GPP - R p = 60 g/yr T R of Atm-CO 2 wrt terrestrial vegetation: 750 g / 60 g yr -1 = 12.5 yr Thus, each molecule of CO 2 in the atm has the potential to be taken up in terrestrial NPP every 12.5 years. T R of Atm-CO 2 wrt the ocean: 750 g / 92 g yr -1 = 8 yr (all units x g) Mean T R of Atm-CO 2 wrt the ocean + land: 750 g / ( ) g yr -1 = 5 yr Mean T R only slightly longer than the mixing time of the atmosphere, so only minor seasonal variations are evident about the mean global average concentration of ~380 ppm

12 Global Seasonal Variations in Atmospheric CO 2 Seasonal uptake of CO 2 results in oscillations in atm CO 2 content Effect is greater in Northern Hemisphere

13 Carbon dioxide is only a small fraction of the Earth s surficial C reservoir, but its role in photosynthesis, climate regulation and rock weathering make it a critical component of the system Globally, 2/3 of terrestrial vegetation occurs in regions with seasonal biomass growth Atm CO 2 fluctuations are greatest in the N. Hemisphere, where most of the continental landmass resides S. Hemisphere fluctuations believed due to exchange with surface ocean

14 large interannual changes in CO 2 growth rates can mostly be explained by natural climate variability (e.g., ENSO). (Patra et al. (2005))

15 Mauna Loa Observatory

16 Photosynthesis Links the C and O Cycles Photosynthetic uptake of C to synthesize organic matter releases O 2 : CO 2 + H 2 O CH 2 O + O 2 Oxidation of organic matter consumes O 2 : CH 2 O + O 2 CO 2 + H 2 O - Burial of organic matter (reduced C) equates to an increase in the atmospheric O 2 reservoir:

17 Organic C Burial Links CO 2 to Atmospheric O 2 Cycle A Simple Model

18 Carbonate and Silicate Rock Cycle A More Detailed Approach Weathering on land CaCO 3 + CO 2 + H 2 O = Ca HCO 3 - CaSiO 3 +2CO 2 +3H 2 O = Ca HCO H 4 SIO 4 --> Uptake of atmospheric CO 2 during weathering on land; delivery of dissolved form to oceans Deposition in the oceans Ca HCO 3 - = CaCO 3 + CO 2 + H 2 O H 4 SiO 4 = SiO 2 + 2H 2 O --> Release of CO 2 during carbonate precipitation Metamorphic reactions CaCO 3 + SiO 2 = CaSiO 3 + CO 2 --> Release of CO 2 via volcanic/hydrothermal activity Oxidation of uplifted organic matter CH 2 O + O 2 = CO 2 + H 2 O

19 The Global Cycle of Weathering Ions carried by Rivers to oceans Weathering of Silicate rocks The Rock Cycle: Primary minerals at Earth surface exposed to acidic forms of C, N, S from atmos Products of weathering reactions are carried to the ocean via rivers Weathering products accumulate as dissolved salts or sediments Subduction carries sediments back into the deep earth - CO 2 released - Primary minerals re-formed at high T and P

20 CaCO 3 weathering on land and re-precipitation in ocean has no net effect on atmospheric CO 2 Weathering of silicates on land and re-precipitation in ocean results in net uptake of atmospheric CO 2 Balance of weathering types affects atmospheric CO 2 Subduction of sediments and volcanic activity returns CO 2 to atmosphere In the absence of recycling, weathering would remove all CO 2 from atmosphere in ~ 1 million years Residence time of CO 2 in atmosphere relative to weathering and volcanic input is ~ 6,000 years, i.e. the rock cycle exerts long term control on atm CO 2 Rock cycle does not control decade- to century-scale changes seen in modern C cycle

21 History of the C Cycle Long-term changes in atmospheric CO 2 driven by rock cycle and biological evolution Initial high levels of atmospheric CO 2 and a weak sun Silicate weathering and carbonate precipitation in ocean reduced atmospheric CO 2 levels Evolution of life ~3.9 Ga sequestered organic C Oxygenic photosynthesis ~2.8 Ga accumulation of O 2

22 Initial production of O 2 consumed by oxidation of Fe in seawater Terrestrial weathering also consumed early O 2 production

23 Phanerozoic C Cycle (last 500 million years) Driven by evolution of land plants (and C storage) Ma 30 x moles C buried in sediments yr increases O 2 in atmosphere Atmospheric O 2 = 38 x moles; T r = 1 x 10 6 yrs (wrt sedimentary C) Uplift of rocks and weathering of kerogen balances process Atmospheric O 2 results from balance of organic C burial and its weathering

24 Evolution of angiosperms ~ 150 Ma Deeper roots increase Si weathering rates, leads to drop in atm CO 2

25 O 2 levels in atmosphere track maximum burial of organic C ~ 350 Ma Microbial processes then pull down O 2 levels as organic C is oxidized White rot fungi appear

26 The C Cycle Since the Industrial Revolution Since 1800, by burning fossil fuel and cutting forests, we have released more than 400 billion tons of carbon - half of it during the last 30 years only (upper part of the graph). This extra CO 2 accumulates in the atmosphere, vegetation and ocean (lower part of the graph). (Global Carbon Project, 2008)

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