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NARROW
GeoRef Subject
-
all geography including DSDP/ODP Sites and Legs
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Africa
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East Africa
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Zambia (1)
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North Africa
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Egypt
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Aswan Dam (1)
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Southern Africa
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Zimbabwe (1)
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Asia
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Arabian Peninsula
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Far East
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China
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Sichuan Basin (1)
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Japan
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Hokkaido (1)
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Honshu
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Aichi Japan (1)
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Kanagawa Japan (1)
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Malay Peninsula
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West Malaysia
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Malaysia
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Indian Peninsula
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Main Central Thrust (1)
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Atlantic Ocean
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South Atlantic
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Australasia
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Oceania
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Pacific Ocean
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Mesozoic
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Proterozoic
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Primary terms
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Africa
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Zambia (1)
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North Africa
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Egypt
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Southern Africa
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Zimbabwe (1)
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Asia
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Arabian Peninsula
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Far East
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China
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Sichuan Basin (1)
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Japan
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Hokkaido (1)
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Aichi Japan (1)
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Maharashtra India
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Koyna Dam (1)
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-
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Main Central Thrust (1)
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Atlantic Ocean
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Gulf of Mexico
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Mississippi Canyon (1)
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South Atlantic
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atmosphere (2)
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Australasia
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Canada
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Quebec (2)
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carbon
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catalogs (1)
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Cenozoic
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Quaternary
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Pleistocene
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Bishop Tuff (2)
-
-
-
Tertiary
-
Neogene
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Miocene
-
Topopah Spring Member (1)
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upper Miocene (1)
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-
-
Paleogene
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Eocene
-
upper Eocene (1)
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Oligocene (1)
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-
-
-
Central America
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Costa Rica
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Irazu (1)
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chemical analysis (2)
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clay mineralogy (3)
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climate change (1)
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construction materials (1)
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core (1)
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crust (3)
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crystal chemistry (7)
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crystal growth (5)
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crystal structure (4)
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data processing (7)
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Deep Sea Drilling Project
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IPOD
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Leg 64
-
DSDP Site 477 (1)
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DSDP Site 481 (1)
-
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deformation (2)
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diagenesis (1)
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earthquakes (3)
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East Pacific Ocean Islands
-
Hawaii
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Hawaii County Hawaii
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Kilauea (2)
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Puu Oo (1)
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Mauna Loa (2)
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-
-
ecology (2)
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Europe
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Germany
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Laacher See (1)
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Poland (2)
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Jutland (6)
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Pannonian Basin (1)
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Croatia (1)
-
Italy
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Vesuvius (1)
-
-
Sicily Italy
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Lipari Islands
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Stromboli (1)
-
-
Mount Etna (1)
-
-
-
-
Western Europe
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Scandinavia
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Sjaelland (4)
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Norway (1)
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United Kingdom
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England (1)
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geochemistry (15)
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geochronology (6)
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geophysical methods (6)
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heat flow (5)
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hydrogen
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deuterium (4)
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hydrogeology (1)
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hydrology (9)
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igneous rocks
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plutonic rocks
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granites
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I-type granites (1)
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pegmatite (1)
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ultramafics
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peridotites
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harzburgite (1)
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spinel lherzolite (1)
-
-
-
-
volcanic rocks
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basalts
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alkali basalts
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hawaiite (1)
-
-
flood basalts (1)
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basanite (1)
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glasses
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perlite (1)
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phonolites (2)
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inclusions
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industrial minerals (1)
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intrusions (5)
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isotopes
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radioactive isotopes
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Tc-99 (1)
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stable isotopes
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C-13/C-12 (3)
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D/H (1)
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deuterium (4)
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Fe-56/Fe-54 (1)
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He-3 (1)
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He-4 (1)
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Mg-26/Mg-24 (1)
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N-15/N-14 (1)
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Ne-20 (1)
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land use (2)
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lava (3)
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mantle (13)
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Mesozoic
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Cretaceous
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Upper Cretaceous
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Tuolumne Intrusive Suite (1)
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Triassic (1)
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metal ores
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molybdenum ores (2)
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platinum ores (1)
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diffusivity
Diffusion in Melts and Magmas
Hydrogen diffusion mechanisms in quartz: insights from H–Li, 2 H–H and 2 H–H–Li exchange experiments
Behavior and origin of hydrogen defects in natural orthopyroxene during high-temperature processes
Macrostructural and Microstructural Properties of Residual Soils as Engineered Landfill Liner Materials
Br diffusion in phonolitic melts: Comparison with fluorine and chlorine diffusion
Abstract Stable isotope composition of gas is widely used in hydrocarbon exploration to determine the composition and thermal maturity of source rocks. Many isotope classification systems used for gas to source rock correlation and thermal maturity determination are primarily based on empirical observations made in conventional reservoirs and the kinetic isotope effects observed during pyrolysis experiments performed on source rocks. However, such relationships may not be readily applicable to onshore unconventional reservoirs due to the strong molecular and isotope fractionation that occur during extensive gas expulsion associated with basin uplift and depressurization. Degassing studies of freshly recovered core samples can provide useful insight into the behaviour of gas molecules in unconventional reservoirs during basin uplift. The analyses of Australian coal and marine shale samples demonstrate that during desorption both molecular and isotopic compositions of gas change at variable rates. Gas initially desorbed from the samples is mostly CH 4 , whereas later desorbed gas becomes increasingly enriched in C 2 H 6 and higher hydrocarbons. Hydrocarbon molecules also fractionate according to their isotopic composition, where the early released gas is enriched in 12 C causing the remaining gas in the reservoir to be enriched in the heavier 13 C isotope. During the release of gas from the Bowen Basin coals the C isotope ratio of CH 4 ( δ 13 C 1 ) changes by up to 21‰ (VPDB), whereas that for C 2 H 6 ( δ 13 C 2 ) and C 3 H 8 ( δ 13 C 3 ) changes by <6‰. Similar changes in the isotope composition can be seen during the release of gas from marine source rocks of the Beetaloo Sub-basin. In a fully gas-mature middle Velkerri shale sample, δ 13 C 1 changes by up to 28‰ and δ 13 C 2 by up to 3‰ with no appreciable change occurring in δ 13 C 3 . The extent of molecular fractionation during gas flow through carbonaceous rocks is primarily related to the adsorption–desorption properties of organic matter and diffusivity through the overall rock matrix. Using the current dataset, the magnitude of the contributions exerted by the desorption and diffusion processes cannot be readily distinguished. However, both Bowen Basin coals and Beetaloo Sub-basin shale show similar fractionation effects during gas flow, where the heavier alkane molecules, including those containing more 13 C, desorb and move slowly compared with the lighter components, in particular CH 4 . Different rates of isotope fractionation between hydrocarbon molecules during gas flow cause the shape of compound-specific-isotope (CSI) curve to change with time. Early released gas is characterized by a normal CSI trend where the short-chain hydrocarbons are isotopically lighter compared with the longer-chain hydrocarbons. Because CH 4 and C 2 H 6 molecules enriched in 12 C desorb and diffuse more readily than the heavier hydrocarbons (including those enriched 13 C), the gas remaining in the coal and shale samples after extensive desorption shows a reversed CSI trend where CH 4 and C 2 H 6 are isotopically heavier compared with the longer chain hydrocarbons. Reversed isotope trends may also develop over geological time, particularly where the source rock is fully gas-mature and has expelled hydrocarbons due to prolonged degassing. As seen in the Beetaloo Sub-basin, the CSI trend in the dry-gas-mature Velkerri shale is reversed, possibly due to the loss of a large proportion of originally generated CH 4 during post-Cambrian basin uplift.