Simple view of controls on CO 2 from last week!

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1 Simple view of controls on CO 2 from last week! Rate of CO 2 in/out of atmosphere! CO 2! Out from weathering! In from volcanoes! CO 2 and Phanerozoic" (550-0Ma) Climate!! Carbon reserviors, fluxes and isotopic composition!! Modelled CO 2 : GEOCARB III!! Measured paleo-co 2! 1!

2 Reservoirs! and fluxes! in gc and! gc/yr! Green: size of reservoir (10 18 gc)! Red: flux from one reservoir to another (10 18 gc/yr)! 2!

3 Isotopes of Carbon! 12 C 98.93%! 13 C 1.07%!! 13 C = (R sample /R std - 1)x1000! R std = 13 C/ 12 C PDB! Isotopic fractionation:!!physical transport!!chemical reactions! Imp: 12 C isotope preferred by plants, so organic carbon! is VERY depleted in carbon isotope composition (! 13 C)! relative to all other carbon reservoirs!! Organic matter 20 depleted relative to inorganic carbon reservoir!! Isotopic composition of carbon entering from volcanoes is the same as that of carbon being buried in rocks! 3!

4 GEOCARB (Berner, BLAG ) Model!! Aim: Reconstruct long term atmospheric CO 2 at 10 million year time resolution.!! Assumption: Flux of carbon into and out of the ocean/atmosphere reservoir are equal (steady state)!! Key component for stable output: weathering of silicate rocks increases with increasing temperature and CO 2! Berner and Kothavala (2001)! Why assume steady state?! 4!

5 GEOCARB Model!! CO 2 input to atmosphere!! Thermal breakdown of sedimentary carbonates and organic carbon (diagenesis, metamorphism and volcanism)!! Weathering of carbonates!! Oxidation of organic carbon!! CO 2 drawdown from atmosphere!! Silicate weathering (carbonate burial)!! Organic carbon burial! Urey reactions! Organic carbon cycling! 5!

6 Ocean/atm/biosphere reservoir is at steady state! mass balance of C! mass balance of isotopes! w = weathering! m = metamorphism and volcanism! b = burial! c = carbonate! g = organic matter! Organic carbon and Carbonate rock reservoirs can grow and shrink! 6!

7 What determines how fluxes (F) change with time?!! Weathering of carbonates (F wc ) and organic carbon (F wg ) depends on amount stored in rocks (model variable) plus climate (model variable) and geographic variables (specified as input)!! Return of rock carbon to the atmosphere from volcanism (F mg, F mc ) depends on spreading rate (specified) and whether they were buried on shelves or in deep sea (specified)!! Net burial of carbonate (by definition the silicate weathering flux) F bc - F wc depends on temperature, climate (model variables), geography, plants, etc. (input)!! F bg depends on the chemistry and circulation of the ocean among other things - cannot be specified or parameterized based on model variables! Weathering feedback term! 7!

8 Weathering uplift parameter! Plant weathering!! Deep rooted large vascular plants (trees) rose during Devonian ( Ma)!! Rise of Angiosperms ( Ma)!! Extent to which plants enhance weathering rate is not well constrained experimentally and in this model is tunable parameter! 8!

9 Simplification for easier understanding: G and C are big and relatively unchangeable! Fluxes on lhs depend on (1) spreading rate, (2) geography! and (3) climate! F bc depends on (1) geography and evolution and (2) climate! F bg depends on the chemistry and circulation of the ocean among other things! 2 equations, 2 unknowns (climate and burial of organic carbon)! Isotopes can be used to assess fraction of carbon buried as organic material! 9!

10 Model Results! What about the data?! 10!

11 Royer et al 2004! Paleosol (Cerling) Method!! Organic matter of land plants has lower! 13 C than the ratio in the atmosphere!! Plant organic matter (roots, fallen leaves) decays within the soil, releasing CO 2 that is low in! 13 C!! Atmospheric CO 2 (higher! 13 C ) also diffuses into the soil!! If atmospheric CO 2 concentrations are high, the! 13 C in soil CO 2 is close to the atmospheric ratio!! If atmospheric CO 2 concentrations are low, the! 13 C in soil CO 2 is close to the organic ratio!! CaCO 3 precipitating in desert soils records the! 13 C in soil CO 2.! 11!

12 no CO 2 low CO 2 high CO 2 atmosphere soil soil CO 2 (low 13 C/ 12 C) atmospheric CO 2 (high 13 C/ 12 C) Stomatal density method!! Stomatal density (stomates/unit area) and Stomatal index(percentage of epidermal cells that are stomates) correlate inversely with pco2!! Stomatal index less sensitve to changes in soil moisture humidity and temperature!! Calibration of extinct species?! 12!

13 Low CO 2, continental glaciation! Royer et al.,! 2004! Why do we care that BLAG" seems to work?! 13!

14 Why do we care that BLAG" seems to work?! 1)! understand causes of high CO2 in past; understand the!! timescales for CO2 removal from atmosphere! 2)!low CO2 and glaciations seem to be linked! 3)! can estimate climate sensitivity (definition: how much!! temperature change occurs with a doubling of CO2?)! Ex: estimate climate sensitivity! -!BLAG assumes feedbacks b/t CO2,! temperature, and weathering! -!if CO2 causes large T! changes, weathering rates! will skyrocket, and modeled! CO2 will fall below proxy data! -!if CO2 causes low T, weathering! rates will be low, and CO2 will! exceed proxy data! -climate models give C;! -BLAG model gives ~3 C! Royer et al., 2007! 14!

15 For further reading! Berner, RA and Z. Kothavala (2001). "GEOCARB III: A revised model of atmospheric CO2 over Phanerozoic time". American Journal of Science 304: " Royer, Dana L., Robert A. Berner, Isabel P. Montañez, Neil J. Tabor, and David J. Beerling (2004). "CO2 as a primary driver of Phanerozoic climate". GSA Today 14 (3): 4-10." 15!

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