Tracing the sources and evolution processes of shale gas by coupling stable (C,H) and noble gas isotopic compositions: Cases from Weiyuan and Changning in Sichuan Basin, China.

The source and thermal evolution history of organic matter for the Longmaxi shale are still debated. This study analyzed the molecular and stable carbon isotopic compositions of hydrocarbons (CH ₄, C ₂H ₆, and C ₃H ₈) and CO ₂ as well as the stable hydrogen isotopic compositions of methane, ethane, and noble gases (He, Ne, Ar, Kr, and Xe). Shale gases in the WY and CN areas show an extremely-low-wetness with CH ₄ concentrations range from 93.41% to 99.01%. Non-hydrocarbon gases are mainly N ₂ (0.22%–2.81%) and CO ₂ (0.03%–1.35%). H ₂S have not been detected. Different δ ¹³C ₁ and δ ¹³C ₂ values in WY and CN shale gases (WY: −37.3‰ to −35.0‰ and −40.3‰ to −38.3‰, CN: −29.8‰ to −26.3‰ and −35.3‰ to −32.7‰) and various carbon isotope-composition distribution patterns (δ ¹³C ₁>δ ¹³C ₂<δ ¹³C ₃ and δ ¹³C ₁>δ ¹³C ₂>δ ¹³C ₃) of hydrocarbons indicate a complex evolution process. WY shale gases include more oil-cracking gas than CN shale gases, suggesting WY shale gases more like come from Type I-II organic matter. In shale gas systems, methane content and δ ¹³C ₁ ratios vary with the degree of thermal evolution, so the origin of shale gas cannot be determined using carbon isotope data alone. The wide range of δ ¹³C _CO2 values (−8.9‰ to −0.8‰) and N ₂/ ⁴⁰Ar ratios (20.8–165.1) suggests multiple origins of the gases. Emeishan mantle plume provides the source of heat for some thermo-genic gas. Noble gas isotopic compositions ( ³He/ ⁴He: 0.001Ra to 0.019Ra) indicate air and crustal origins with no significant contribution from the mantle. ⁴⁰Ar/ ³⁶Ar ratios (1194.3–4604.5) are consistent with the age of Longmaxi strata calculated by accumulative effect of Ar isotope. The shale gas humidity, carbon isotope ratios, and the carbon isotope-composition distribution patterns may contain information indicating the shale gas sweet spot.