Geological storage of CO2 within the oceanic crust by gravitational trapping
Version of Record online: 3 DEC 2013
©2013 The Authors. Geophysical Research Letters published by Wiley on behalf of the American Geophysical Union.
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Geophysical Research Letters
Volume 40, Issue 23, pages 6219–6224, 16 December 2013
How to Cite
2013), Geological storage of CO2 within the oceanic crust by gravitational trapping, Geophys. Res. Lett., 40, 6219–6224, doi:10.1002/2013GL058220., , and (
- Issue online: 30 DEC 2013
- Version of Record online: 3 DEC 2013
- Accepted manuscript online: 9 NOV 2013 12:00AM EST
- Manuscript Accepted: 4 NOV 2013
- Manuscript Received: 27 OCT 2013
|readme_final.docx||Word 2007 document||29K||Supporting information|
|Text01_final.docx||Word 2007 document||30K||Text01.docx = A detailed explanation of the methodology used in the paper to identify the potential locations where carbon dioxide can be geologically stored by gravitational and physical trapping in the ocean crust using the GDH1 plate model [Stein and Stein, 1992]. For comparison, the same calculation using the HSCM [Turcotte and Schubert, 2002] is considered, and we discuss why we have chosen to use the GDH1.|
|Fs01validation T.pdf||PDF document||1309K||Fs01.pdf = Comparison between estimated temperatures in the eastern equatorial Pacific Ocean (eePO) and the Juan de Fuca Plate (JdFP), and measured downhole temperatures at the sediment-basement interface. White squares: data from eePO [Alt et al., 1993; Teagle et al., 2006]; orange squares: data from JdFP [Davis et al., 1997]. Circles: estimated values in the eePO (blue), and on the JdFP (red with Ks = 1 W/m/K; orange with Ks = 2 W/m/K). The upper plot is Figure 1 in the manuscript, based on the GDH1 model; the lower plot is the corresponding calculation using HSCM.|
|Fs02thermal conductivity.pdf||PDF document||230K||Fs02.pdf = Histograms of thermal conductivity measurements for marine sediments, from the IODP-ODP database [Pribnow et al., 2000], and from Pollack et al., 1993. The red line shows the mean, which is close or equal to 1 W/m/K for both databases.|
|Fs03sed_HSCM.pdf||PDF document||253K||Fs03.pdf = Density difference between CO2 and seawater at the sediment-basement interface as a function of plate age and sediment thickness using the GDH1 model (left) or the HSCM (right) to determine both water depth and thermal conditions. Sediment thicknesses below the heavy black line show where positive density differences required for stable gravitational trapping are achieved.|
|Fs04_HSCMglobal map.pdf||PDF document||1820K||Fs04.pdf = An equal area map showing locations for stable geological sequestration of CO2, using the HSCM. Shading shows the difference in density between CO2 and seawater in areas where the sediment thickness is between 200 and 700 m and the CO2 is denser than seawater. Five potential reservoirs (a/b/c/d/e) have been identified. The red box indicates the area required to store 100 years of current anthropogenic emissions of CO2, assuming a pillow lava thickness of 300 m and 10% porosity [Carlson and Herrick, 1990; Jarrard et al., 2003; Johnson and Pruis, 2003]. Yellow boxes show the eePO and JdF regions.|
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