Experimental and theoretical determinations of hydrogen isotopic equilibrium in the system CH4H2H2O from 3 to 200 °C. (1st December 2021)

• Record Type: Journal Article
• Authors: Turner, Andrew C.; Korol, Roman; Eldridge, Daniel L.; Bill, Markus; Conrad, Mark E.; Miller, Thomas F.; Stolper, Daniel A.
• Is Part Of: Geochimica et cosmochimica acta. Volume 314(2021)
• Page Start: 223
• Page End: 269
• Publication Date: 2021-12-01
• Subjects: Experimental calibration -- Methane isotopic equilibrium -- Methane geochemistry -- Path Integral Monte Carlo calculations; Geochemistry -- Periodicals; Meteorites -- Periodicals; Géochimie -- Périodiques; Météorites -- Périodiques; Geochemie; Astrochemie; Electronic journals; 551.905
• DOI: 10.1016/j.gca.2021.04.026
• Languages: English
• ISSNs: 0016-7037

Abstract

Abstract: The stable isotopic composition of methane (CH4 ) is commonly used to fingerprint natural gas origins. Over the past 50 years, there have been numerous proposals that both microbial and thermogenic CH4 can form in or later attain hydrogen isotopic equilibrium with water (H2 O) and carbon isotopic equilibrium with carbon dioxide (CO2 ). Evaluation of such proposals requires knowledge of the equilibrium fractionation factors between CH4 and H2 O or CO2 at the temperatures where microbial and thermogenic CH4 form in or are found in the environment, which is generally less than 200 °C. Experimental determinations of these fractionation factors are only available above 200 °C, requiring extrapolation of these results beyond the calibrated range or the use of theoretical calculations at lower temperatures. Here, we provide a calibration of the equilibrium hydrogen isotopic fractionation factor for CH4 and hydrogen gas (H2 ) ( D αCH4(g)–H2(g) ) based on experiments using γ-Al2 O3 and Ni catalysts from 3 to 200 °C. Results were regressed as a 2 nd order polynomial of 1000 × ln D αCH4(g)–H2(g) vs. 1/T (K −1 ) yielding: 1000 × l n D α C H 4 ( g ) - H 2 ( g ) = 3.5317 × 10 7 T 2 + 2.7749 × 10 5 T - 179.48 We combine this calibration with previous experimental determinations of hydrogen isotope equilibrium between H2, H2 O(g), and H2 O(l) and we provide an interpolatable experimental calibration of 1000 × ln D αCH4(g)–H2O(l) from 3 to 200 °C. Our resulting 4th order polynomial is the following equation: 1000 × l n D α C H 4 ( g ) - H 2 O l = - 7.9443 × 10 12 T 4 + 8.7772 × 10 10 T 3 - 3.4973 × 10 8 T 2 + 5.4398 × 10 5 T - 382.05 At 3 °C, the value from our calibration differs by 93‰ relative to what would be calculated based on the extrapolation of the only experimental calibration currently available to temperatures below its calibrated range (lowest temperature of 200 °C; Horibe and Craig, 1995). We additionally provide new theoretical estimates of hydrogen isotopic equilibrium between CH4 (g), H2 (g), and H2 O(g) and carbon isotopic equilibrium between CH4 (g) and CO2 (g) using Path Integral Monte Carlo (PIMC) calculations. Our PIMC calculations for hydrogen isotopic equilibrium between CH4 and H2 agree 1:1 with our experiments. Finally, we compile carbon and hydrogen isotopic measurements of CH4, CO2, and H2 O from various environmental systems and compare observed differences between carbon and hydrogen isotopes to those expected based on isotopic equilibrium. We find that isotopic compositions of some microbial gases from marine sedimentary, coalbed, and shale environments are consistent with those expected for CH4 H2 O(l) hydrogen and CH4 CO2 carbon isotopic equilibrium. In contrast, microbial terrestrial and pure culture gases are not consistent with both CH4 H2 O(l) hydrogen and CH4 CO2 carbon isotopic equilibrium. These results are explained qualitatively using previously developed conceptual models that link free energy gradients available to microorganisms to the degree that their enzymes can promote isotope-exchange reactions between CH4, CO2, and H2 O.