The Global Carbon Cycle
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1 The Global Carbon Cycle Tom Bibby September 2003
2 The Carbon Cycle
3 - Look at past climatic change; as controlled by the carbon cycle. - Interpret the influence of human changes (Anthropogenic Perturbations) - Economic and Trade Policies
4 Venus Earth
5 States of water in the solar-system
6 The Faint Young Sun Paradox
7 The greenhouse effect
8 This false-color Terra satellite image of Earth shows infrared heat escaping to space. Greenhouse gases trap such heat and warm our planet.
9 Relative percentage composition of greenhouse gases in the Earth s atmosphere
10 Distribution of carbon reservoirs on Earth
11 Pools Quantity (gt) Atmosphere 720 Oceans 38,400 Total inorganic 37,400 Surface Layer 670 Deep layer 36,730 Total Organic 1,000 Lithosphere Sedimentary carbonates >60,000,000 Kerogens 15,000,000 Terrestrial biosphere (total) 2,000 Living Biomass 600-1,000 Dead Biomass 1,200 Aquatic biosphere 1-2 Fossil fuels 4,130 Coal 3,510 Oil 230 Gas 140 Other (peat) 250 Falkowski et al, 2002 Science, Vol 290,
12 Values of carbon exchange between reservoirs
13
14 Carbon Degassing MÖrner and Etiope, Global and Planetary Change 33 (2002)
15 Methane Hydrates
16 Cross-section through the Earth
17 The Ring of Fire
18 Chemical weathering Export of CO 2 From the atmosphere
19 The hydrological cycle
20 Chemical Weathering
21 Calcite (Carbonate) compensation depth (CCD) -- The depth in the ocean below which material composed of calcium carbonate is dissolved and does not accumulate on the sea floor
22 Factors effecting the rate of chemical weathering Temperature : Rate of chemical reactions Precipitation: Amount of H 2 O Vegetation: Efficiency of delivery of CO 2 to the soil
23 Falkowski and Raven 1997 Atmospheric CO 2 Levels Myrs ago
24 Faint Young Sun Paradox: Negative feedback controls.
25 Faint Young Sun paradox: Controlled by the Carbon cycle
26 Rate of Tectonic Movement
27 The Earth s Orbit
28 Long-term changes in tilt: Changes in the tilt of the Earth s axis have occurred on a regular 41,000-year-cycle
29 Long-term changes in eccentricity: The eccentricity of the Earth s orbit varies at periods of 100,000 and 413,000 years.
30 Long-term changes in precession: The precessional index changes mainly at a cycle of 23,000 years
31
32
33 Review of Lecture 1 Aim:Cover the long-term processes of the carbon cycle. -CO 2 release into the atmosphere. - Removal of CO 2 from the atmosphere via chemical weathering. These processes have existed in a dynamic equilibrium that has kept the Earth s climate relatively constant.
34 The Faint Young Sun Paradox
35 Falkowski and Raven 1997 Atmospheric CO 2 Levels Myrs ago
36
37 The Carbon Balance each year Gt from fossil emissions 1.6 Gt emitted from land-clearing Leaving a net 7.9 Gt in the atmosphere (estimated)
38 The Balance each year Gt from fossil emissions ca. 1.6 Gt emitted from land-clearing 1.7 Gt net uptake into ocean systems 3.0 Gt into terrestrial systems Leaving a net 3.2 Gt in the atmosphere
39 The evolution and global effect of photosynthetic organisms Myrs ago
40 The Organic Carbon Cycle
41 Z.Johanson; S.W., Chisholm Nature, V 40, p685 The Biological Pump
42 Diatom Coccolithophore
43 Fertilizing the oceans: IonEx - Experiments HNLC: High Nutrient Low Chlorophyll Iron is the limiting factor. Hypothesis to fertilize the ocean with iron, increase productivity of the phytoplankton, therefore increase amounts of carbon removed from the atmosphere.
44 Ocean Circulation
45 Ocean Sinks What are the ocean mechanisms? Solubility pump CO 2 taken up in high latitudes Transported to low latitudes Biological pump 45 Gt C /y uptake via a C pool of 1 Gt C of phytoplankton Mostly in low latitudes
46 The Carbonate System
47
48
49 Deffeyes Curve
50 Foraminifera Coccolithophore
51 Oxygen Fractionation δ 18 O = ( 18 O/ 16 O)sample ( 18 O/ 16 O)standard x1000 ( 18 O/ 16 O) standard 2 stable (nonradioactive) isotopes of Oxygen: 16 O 99.8%; 18 O the rest. Samples with large amounts of 18 O have more positive δ 18 O values and are 18 O-enriched Samples with small amounts of 18 O have more negative δ 18 O values and are 18 O-depleted
52 Oxygen fractionation (physical) - 16 O is more easily evaporated than 18 O - Leaving water vapor enriched in 16 O - If this vapor falls as precipitation and becomes locked up in ice-sheets (a cold climate) then surface waters become relatively 18 O enriched - δ 18 O values and are 18 O-enriched
53 Carbon Fractionation δ 13 C = ( 13 C/ 12 C)sample ( 13 C/ 12 C)standard x1000 ( 13 C/ 12 C) standard 2 stable (nonradioactive) isotopes of Carbon: 12 C 99%; 13 C the rest. Samples with large amounts of 13 C have more positive δ 13 C values and are 13 C-enriched Samples with small amounts of 13 C have more negative δ 13 C values and are 13 C-depleted
54 Carbon Fractionation during Oxygenic Photosynthesis Rubisco: Fixes CO 2 Preferentially fixes 12 C
55 Correlation of atmospheric Carbon and Ice Volume
56 Falkowski et. al. The Global Carbon Cycle: A Test of our knowledge of Earth as a System. Science; 2000 vol. 290 pp Hoffman et. al. A Neoproterozoic Snowball Earth. Science; 1998 vol pp Berner. Examination of hyphotheses for the Permo- Triassic boundary extinction by carbon modelling. PNAS; 2002 vol. 99 pp Norris and Rohl. Carbon cycling and chronology of climate warming during the Palaeocene/Eocene transition. Nature; 1999 vol. 401 pp
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