Abstract
On a planetary scale, the carbon cycle describes the movement of carbon between the atmosphere and the deep Earth. Carbon species are involved in diverse Earth processes, ranging from sedimentary, metamorphic and igneous petrology to the long-term viability of life at the Earth's surface. Volcanoes, and their associated magmatic systems, represent the interface through which carbon is transferred from the deep Earth to the surface. Thus, quantifying the CO 2 budget of volcanic systems is necessary for understanding the deep carbon cycle and, concomitantly, the CO 2 budget of the near surface, including the atmosphere. In this review, Kilauea volcano (Hawaii) is used as a case study to illustrate simple calculations that can account for processes that affect the amount and distribution of CO 2 in this relatively well-studied volcanic system. These processes include methods to estimate the concentration of CO 2 in a melt derived by partial melting of a source material, enrichment of CO 2 in the melt during fractional crystallization, exsolution of CO 2 from a fluid-saturated melt, trapping and post-entrapment modification of melt inclusions, and outgassing from the volcanic edifice. Our goal in this review is to provide straightforward example calculations that can be used to derive first-order estimates regarding processes that control the CO 2 budgets of magmas and that can be incorporated into global carbon cycle models.
Highlights
These example calculations follow the processes of 1) melting a carbon-bearing I source material, 2) melt evolution during fractional crystallization, volatile saturation, and exsolution R of CO2 into a separate fluid phase (degassing), and 3) mass transfer of the exsolved carbonC bearing fluid into the atmosphere (outgassing)
Our goal in this review is to provide straightforward example calculations that can be used to derive first-order estimates regarding processes that control the CO2 budgets of magmas and which can be incorporated into global carbon cycle models
Given the same melt production rate reported by Cayol et al (2000), this concentration suggests either that the melt inclusions trapped a partially degassed melt or that the average CO2 flux is approximately half of the value reported by Gerlach et al (2002) and is more consistent with fluxes reported by Greenland et al (1985; 0.58 Mt/y) and Hager et al (2008; 1.79 Mt/y)
Summary
These example calculations follow the processes of 1) melting a carbon-bearing I source material, 2) melt evolution during fractional crystallization, volatile saturation, and exsolution R of CO2 into a separate fluid phase (degassing), and 3) mass transfer of the exsolved carbonC bearing fluid into the atmosphere (outgassing).
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