coupled biogeochemical cycles william h. schlesinger millbrook, new york
TRANSCRIPT
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Coupled Biogeochemical Cycles
William H. Schlesinger
Millbrook, New York
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1. Some basic stoichiometry for life―in biomass
First articulated by Liebig (1840)and later advanced by Redfield (1958), Reiners (1986), Sterner and Elser (2002), and Cleveland and Liptzin (2007)
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Complementary Models for Ecosystems
Reiners, W.A. 1986
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145
100 + ?Δ
121
40
The Global Nitrogen Cycle - Modern
48-59
18
<5
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IF NPP = 60 x 1015 g C/yr
60 X 1015 g C x 1 N = 1.2 x 1015 g N 50 C
= 1200 x 1012 g N/yr
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From: Magnani et al. 2007
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Townsend et al. 1996. Ecological Applications 6(3):806-814.
Spatial Distribution of the 1990 Carbon Sink Resulting from Fossil-fuel N Deposition between 1845 and 1990
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Coupling of biogeochemical cycles, due to:
2. The flow of electrons in the oxidation/reduction reactions―
First articulated by Kluyver (1926),and later advanced by Morowitz, Nealson, Falkowski, and many others
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Schlesinger, W.H. 1997
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H2O/O2 C N S FeH
2O/O
2
X
PhotosynthesisCO2 CH2O O2
C
RespirationC CO2
O2 H2O X
DenitrificationC CO2
NO3 N2
Sulfate reductionC CO2
SO4 H2S
Iron reduction- organic C oxidation4a or
AOM4b
C CO2
FeIII FeII
N
Heterotrophic nitrification
NH4 NO3
O2 H2O
Chemoautotrophy(nitrification)
NH4 NO3
CO2 C
AnammoxNH4 + NO2
N2+H2O
Sulfate reduction7
NH4 N2/ NO3
SO4 H2S
Feammox 5a,b,c
NH4 NO2/N2/NO3
FeIII FeII
S
Sulfur oxidationS SO4
O2 H2O
Chemoautotrophy(sulfur-based
photosynthesis)S SO4
CO2 C
Autotrophic DenitrificationS SO4
NO3 N2/NH4
X
Iron reducing and sulfur oxidizing
bacterial consortium 6
S SO4
FeIII FeII
Fe
Chemolithotrophic(Iron oxidizing
bacteria) 1
FeII FeIIIO2 H2O
Autotrophic or mixotrophic (iron
oxidizing bacteria) 2
FeII FeIIICO2 C
iron oxidizing archaeum3a or nitrate-
reducing, Fe(II)-oxidizing bacteriums3b
FeII FeIIINO3 N2/NH4
X X
Oxidized ReducedO
xidi
zed
R
educ
ed
Table 1. Matrix of redox reactions via microbial metabolisms as updated and modified from Schlesinger et al (2011).
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Mikucki et al. 2009
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Coupled Metabolism & The Sulfur Wars
Howarth and Teal 1979report 75 moles/m2of sulfate reduction annually
2H+ + SO4= + 2CH2O 2CO2 + H2S + 2H2O
implies 150 moles of C is oxidized
150 mols C = 1800 g C/m2/yr
Howes et al. 1984
NPP nowhere near that high!
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145
100 + ?Δ
121
40
The Global Nitrogen Cycle - Modern
48-59
18
<5
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Denitrification
5CH2O + 4H+ + 4NO3- →
2N2 + 5CO2 + 7H20
Intermediates include NO and N2O
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Hirsch et al. 2006Hirsch et al. 2006
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∆ N20= TOTAL
N20 __________________
N2 + N20
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Schlesinger 2009
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Calculation of change in denitrification from N2O
124 Tg (0.37) + 110 Tg (0.082) = 234 Tg (0.246)
4 TgN2O/yr / 0.25 = 17 TgN/yr
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145
116-124
121
40
The Global Nitrogen Cycle - Modern
48-59
18
150+9
<5
Land-sea Transport48
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3. Coupling of biogeochemical cycles to carbon through chelation
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Fig. 2. The fractional amount of Pb loss calculated over the study period is significantly correlated with the thickness (cm) of the forest floor at each site. A logarithmic fit to these data give r2 = 0.65.
Kaste et al. 2006.
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Principles of coupled biogeochemical cycles apply to geo-engineering
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For example, if we wanted to sequester a billion metric tons of C in the oceans by enhancing NPP with Fe fertilization
Current marine NPP = 50 x 1015 g C/yr
F-ratio of 0.15 means that 7.5 x 1015 g C/yr sinks through the thermocline
An additional 1 x 1015 g C/yr sinking would require ~7 x 1015 g C/yr additional NPP, so
7 x 1015 g C x 23 x 10-6 Fe/C = 1.6 x 1011 g Fe (Lab uptake), or x 6 x 10-4 = 4.2 x 1012 (Field observation) Buesseler & Boyd (2003)
Versus, the global production of Fe annually (1900 x 1012 g Fe/yr)
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For example, to provide a sink for 1 x 1015 gC/yr in the world’s soils by
fertilizing them:
Current terrestrial NPP = 50 x 1015 g C/yr
Preservation ratio of 0.008; i.e., global NEP – 0.4 g C/yr (Schlesinger 1990)
To store an additional 1.0 x 1015 g C in soils would require adding125 x 1015 g C/yr to terrestrial NPP
125 x 1015 g C/yr x 1 N/50 C = 2.5 x 1015 g N as fertilizer each year
2.5 x 1015 g C @ 0.857 g C released as CO2 per g N = 2.14 x 1015 g C/yr released in fertilizer production
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The Global Phosphorus Cycle
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Natural Biogeochemical Cycle in Surface Biosphere (terrestrial & oceanic)Element Flux (1012 g/yr) Biospheric Flux/Sedimentary Flux
C 107000 446N 9200 368P 1000 500S 450 5.6Cl 120 0.46Ca 2300 3.7Fe 40 5.3Cu 2.5 23.6Hg 0.003 4.3
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Comparison of Biogeochemical Cycle to Anthropogenic Cycle (Flux in 1012 g/yr)
Element Biospheric Flux Anthropogenic Flux Anthro/Sedimentary Anthro/Biospheric
C 107000 8700 36.3 0.081
N 9200 221 8.8 0.024
P 1000 25 12.5 0.025
S 450 130 1.6 0.29
Cl 120 170 0.65 1.42
Ca 2300 65 0.10 0.028
Fe 40 1.1 0.14 0.028
Cu 2.5 1.5 14.3 0.60
Hg 0.003 0.0023 3.3 0.77
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My final message today:
There is an increasing role for biogeochemists
to contribute to the understanding and fruitful
solutions to global environmental problems.
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