Core Formation in the Lab
Sensitivity of a Coupled Earth System Model to Isopycnal Stirring
Climate interactions forced by continent assembly and breakup
The Young Inner Core
F-layer formation at the inner core boundary
How increasing mixing warms the polar regions
Modeling the Geodynamo
Global Paleobathymetry and Ocean Sediment Reconstruction
Magnetic Reversals and the Earth's Core
Geomagnetic Superchron Cycles Driven by Mantle Convection
Mantle convection, plates, and the Earth system
Geodynamic Carbon Cycling

Geodynamic Carbon Cycling

Crust Mantle

Because Earth’s mantle and crust are massive, open reservoirs of carbon, geodynamical processes affect the concentration of CO2 in the atmosphere and ocean, thereby playing key roles in Earth’s climate variability on geologic time scales. The mantle and crustal reservoirs of carbon have limited influence on short time scale CO2 variations such as those related to primary production and respiration, but they affect the long-term abundance of CO2 in the surface environment through the rock cycle, by altering the rates of weathering of silicate rocks, precipitation and burial of carbonate and organic carbon-rich sediments, volcanic degassing of CO2, and metamorphism of carbonate rocks.

Evidence for the long-term interaction between the mantle and crustal carbon reservoirs and the surface environment comes from the correlations between the oxygen isotope record from shallow marine carbonates, an indicator of sea- surface temperature, and various proxies for the concentration of atmospheric CO2 during the Phanerozoic. As shown in Figure 1, these imply very large changes in both atmospheric CO2 and the global climate system on hundred million year time scales.

Figure 1. Phanerozoic climate variations A: Atmospheric CO2 proxies vs. GEOCARB III model predictions; B: Record of glaciation events (blue shading); C: Latitude distribution of geological evidence for glaciation. Adapted from Royer et al. [2004].

A major geologic process that removes CO2 from the surface environment is the weathering of Ca- and Mg-bearing silicate rocks and the subsequent deposition of Ca- and Mg-bearing carbonate sediments. Another is the burial of organic carbon in sediments. Major geologic processes that add CO2 to the surface environment include volcanic emission, metamorphism of carbonate rocks, and thermal decomposition of marine carbonates and carbon-rich sediments.

These diverse geological processes are loosely coupled by global geodynamics, as schematically illustrated in Figure 2. Mantle convection and subduction produce plate boundaries with active continental margins where metamorphism and volcanism are concentrated. These represent sources of carbon for the surface environment. At the same time, mantle convection produces surface topography via continent collisions, which accelerates the erosion of silicate rocks, and also rifting, which produces passive continental margins and facilitates the deposition of carbonate sediments and the burial of organic carbon. Together these represent a sink of carbon for the surface environment.

Figure 2. A diagram illustrating geodynamic controls on the long-term inorganic carbon cycle. Silicate weathering and subsequent carbonate deposition at passive margins removes carbon from the atmosphere, while volcanic and metamorphic processes at active margins release carbon back to the atmosphere. From Kasting and Catling [2003].

The strength of the long-term carbon cycle is determined by how tightly the above-mentioned geologic processes are coupled by global geodynamics. If they were tightly coupled, that is, if the geologic sources and sinks were nearly in phase, then the long-term carbon cycle would be weak. However, the large variations in atmospheric CO2 implied by Figure 1 are evidence that the coupling between these processes is in fact rather weak, so that the geologic sources and sinks of environmental carbon are not only time variable, but they are also out of phase, by tens or hundreds of millions of years.

How does the Earth system produce such time variability and out of phase behavior? Super-continent formation and breakup controls the distribution, surface relief and sizes of continents, as well the distribution and length of subduction zones, ridges and passive margins, sea level, and the frequency of continent collisions. These in turn affect the circulation and transport of heat in the ocean and atmosphere that control the climate, which couples back to the rock cycle through precipitation, weathering, and erosion.

Some components of the long-term carbon cycle can be calibrated using the present-day Earth, and other components can be estimated from the geological record. However, several of the key parts of this cycle require modeling. For examples, the contributions from metamorphism and volcanism depend on the plate tectonic history. Likewise, the contributions from weathering and erosion depend on the climate history.

The Open Earth Systems project uses models of mantle convection and plate dynamics to calculate the volcanic and metamorphic contributions to the carbon cycle, and to reconstruct past ocean-continent configurations over Phanerozoic times. We then use ocean-atmosphere models to calculate the factors controlling erosion of silicates and carbonate precipitation during this time period, thereby closing the carbon cycle.


Kasting, J.F., and Catlin, D.F., 2003. Evolution of a habitable planet, Ann. Rev.
       Astron. Astrophysics
, 41:429–63.

Royer, D.L., Berner, R.A., Montañez, I.P., Tabor, N.J., and Beerling, D.A., 2004.
       CO2 as a primary driver of Phanerozoic climate, GSA Today, 14, 3.