Carbon isotopes and petrography of kerogens in ∼3.5-Ga hydrothermal silica dikes in the North Pole area, Western Australia

Yuichiro Ueno, Hideyoshi Yoshioka, Shigenori Maruyama, Yukio Isozaki

Research output: Contribution to journalArticle

108 Citations (Scopus)

Abstract

More than 600 specimens of ∼3.5 Ga-old hydrothermal silica dikes from the North Pole area, Pilbara craton, Western Australia, have been studied petrographically. The kerogens in 44 samples have been analyzed isotopically (C and N) and chemically (C, N, and H). The silica dikes are composed mainly of fine-grained silica (modal abundance: >97%) and are classified into two types by minor mineral assemblages: B(black)-type and G(gray)-type. The B-type silica dikes contain kerogen (0.37 to 6.72 mgC/g; average 2.44 mgC/g, n = 21) and disseminated sulfides, dominantly pyrite and Fe-poor sphalerite. In some cases, carbonate and apatite are also present. Their silica-dominated and sulfide-poor mineral assemblages suggest precipitation from low-temperature reducing hydrothermal fluid (likely 100-200°C). On the other hand, the G-type silica dikes are sulfide-free and concentrations of kerogen are relatively low (0.05 to 0.41 mgC/g; average 0.17 mgC/g, n = 13). They typically contain Fe-oxide (mainly hematite) which commonly replaces cubic pyrite and rhombic carbonate. Some G-types occur along secondary quartz veins. These textures indicate that the G-type silica dikes were formed by postdepositional metasomatism (oxidation) of the B-types, and that the B-types probably possess premetasomatic signatures. The δ13C values of kerogen in the B-types are -38.1 to -33.1‰ (average -35.9‰, n = 21), which are ∼4‰ lower than those of the G-types (-34.5 to -30.0‰; average -32.2‰, n=19), and ∼6‰ lower than bedded chert (-31.2 to -29.4‰; average -30.5‰, n= 4). This indicates the preferential loss of 12C during the metasomatism (estimated fractionation factor: 0.9985). Considering the metasomatic effect on carbon isotopes with probably minor diagenetic and metamorphic overprints, we conclude that the original δ13C values of the kerogen in the silica dikes would have been heterogeneous (∼5‰) and at least some material had initial δ13C values of ≤ -38‰. The inferred 13C-depletions of organic carbon could have been produced by anaerobic chemoautotrophs such as methanogen, but not by aerobic p hotoautotrophs. This is consistent with the estimated physical and chemical condition of the hydrothermal fluid, which was probably habitable for anaerobic and thermophilic/hyperthermophilic chemoautotrophs. Alternatively, the organic matter may have been possibly produced by abiological reaction such as Fischer-Tropsch Type (FTT) synthesis under the hydrothermal condition. However, the estimated condition is inconsistent with the presence of the effective catalysts for the FTT reaction (i.e., Fe-Ni alloy, magnetite, and hematite). These lines of evidence suggest the possible existence of biosphere in the ∼3.5 Ga sub-seafloor hydrothermal system.

Original languageEnglish
Pages (from-to)573-589
Number of pages17
JournalGeochimica et Cosmochimica Acta
Volume68
Issue number3
DOIs
Publication statusPublished - Feb 1 2004
Externally publishedYes

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Carbon Isotopes
Petrography
Kerogen
Levees
kerogen
petrography
Silicon Dioxide
carbon isotope
dike
Poles
silica
sulfide
Sulfides
metasomatism
hydrothermal fluid
hematite
pyrite
Ferrosoferric Oxide
Methanogens
Sulfide minerals

ASJC Scopus subject areas

  • Geochemistry and Petrology

Cite this

Carbon isotopes and petrography of kerogens in ∼3.5-Ga hydrothermal silica dikes in the North Pole area, Western Australia. / Ueno, Yuichiro; Yoshioka, Hideyoshi; Maruyama, Shigenori; Isozaki, Yukio.

In: Geochimica et Cosmochimica Acta, Vol. 68, No. 3, 01.02.2004, p. 573-589.

Research output: Contribution to journalArticle

Ueno, Yuichiro ; Yoshioka, Hideyoshi ; Maruyama, Shigenori ; Isozaki, Yukio. / Carbon isotopes and petrography of kerogens in ∼3.5-Ga hydrothermal silica dikes in the North Pole area, Western Australia. In: Geochimica et Cosmochimica Acta. 2004 ; Vol. 68, No. 3. pp. 573-589.
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abstract = "More than 600 specimens of ∼3.5 Ga-old hydrothermal silica dikes from the North Pole area, Pilbara craton, Western Australia, have been studied petrographically. The kerogens in 44 samples have been analyzed isotopically (C and N) and chemically (C, N, and H). The silica dikes are composed mainly of fine-grained silica (modal abundance: >97{\%}) and are classified into two types by minor mineral assemblages: B(black)-type and G(gray)-type. The B-type silica dikes contain kerogen (0.37 to 6.72 mgC/g; average 2.44 mgC/g, n = 21) and disseminated sulfides, dominantly pyrite and Fe-poor sphalerite. In some cases, carbonate and apatite are also present. Their silica-dominated and sulfide-poor mineral assemblages suggest precipitation from low-temperature reducing hydrothermal fluid (likely 100-200°C). On the other hand, the G-type silica dikes are sulfide-free and concentrations of kerogen are relatively low (0.05 to 0.41 mgC/g; average 0.17 mgC/g, n = 13). They typically contain Fe-oxide (mainly hematite) which commonly replaces cubic pyrite and rhombic carbonate. Some G-types occur along secondary quartz veins. These textures indicate that the G-type silica dikes were formed by postdepositional metasomatism (oxidation) of the B-types, and that the B-types probably possess premetasomatic signatures. The δ13C values of kerogen in the B-types are -38.1 to -33.1‰ (average -35.9‰, n = 21), which are ∼4‰ lower than those of the G-types (-34.5 to -30.0‰; average -32.2‰, n=19), and ∼6‰ lower than bedded chert (-31.2 to -29.4‰; average -30.5‰, n= 4). This indicates the preferential loss of 12C during the metasomatism (estimated fractionation factor: 0.9985). Considering the metasomatic effect on carbon isotopes with probably minor diagenetic and metamorphic overprints, we conclude that the original δ13C values of the kerogen in the silica dikes would have been heterogeneous (∼5‰) and at least some material had initial δ13C values of ≤ -38‰. The inferred 13C-depletions of organic carbon could have been produced by anaerobic chemoautotrophs such as methanogen, but not by aerobic p hotoautotrophs. This is consistent with the estimated physical and chemical condition of the hydrothermal fluid, which was probably habitable for anaerobic and thermophilic/hyperthermophilic chemoautotrophs. Alternatively, the organic matter may have been possibly produced by abiological reaction such as Fischer-Tropsch Type (FTT) synthesis under the hydrothermal condition. However, the estimated condition is inconsistent with the presence of the effective catalysts for the FTT reaction (i.e., Fe-Ni alloy, magnetite, and hematite). These lines of evidence suggest the possible existence of biosphere in the ∼3.5 Ga sub-seafloor hydrothermal system.",
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T1 - Carbon isotopes and petrography of kerogens in ∼3.5-Ga hydrothermal silica dikes in the North Pole area, Western Australia

AU - Ueno, Yuichiro

AU - Yoshioka, Hideyoshi

AU - Maruyama, Shigenori

AU - Isozaki, Yukio

PY - 2004/2/1

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N2 - More than 600 specimens of ∼3.5 Ga-old hydrothermal silica dikes from the North Pole area, Pilbara craton, Western Australia, have been studied petrographically. The kerogens in 44 samples have been analyzed isotopically (C and N) and chemically (C, N, and H). The silica dikes are composed mainly of fine-grained silica (modal abundance: >97%) and are classified into two types by minor mineral assemblages: B(black)-type and G(gray)-type. The B-type silica dikes contain kerogen (0.37 to 6.72 mgC/g; average 2.44 mgC/g, n = 21) and disseminated sulfides, dominantly pyrite and Fe-poor sphalerite. In some cases, carbonate and apatite are also present. Their silica-dominated and sulfide-poor mineral assemblages suggest precipitation from low-temperature reducing hydrothermal fluid (likely 100-200°C). On the other hand, the G-type silica dikes are sulfide-free and concentrations of kerogen are relatively low (0.05 to 0.41 mgC/g; average 0.17 mgC/g, n = 13). They typically contain Fe-oxide (mainly hematite) which commonly replaces cubic pyrite and rhombic carbonate. Some G-types occur along secondary quartz veins. These textures indicate that the G-type silica dikes were formed by postdepositional metasomatism (oxidation) of the B-types, and that the B-types probably possess premetasomatic signatures. The δ13C values of kerogen in the B-types are -38.1 to -33.1‰ (average -35.9‰, n = 21), which are ∼4‰ lower than those of the G-types (-34.5 to -30.0‰; average -32.2‰, n=19), and ∼6‰ lower than bedded chert (-31.2 to -29.4‰; average -30.5‰, n= 4). This indicates the preferential loss of 12C during the metasomatism (estimated fractionation factor: 0.9985). Considering the metasomatic effect on carbon isotopes with probably minor diagenetic and metamorphic overprints, we conclude that the original δ13C values of the kerogen in the silica dikes would have been heterogeneous (∼5‰) and at least some material had initial δ13C values of ≤ -38‰. The inferred 13C-depletions of organic carbon could have been produced by anaerobic chemoautotrophs such as methanogen, but not by aerobic p hotoautotrophs. This is consistent with the estimated physical and chemical condition of the hydrothermal fluid, which was probably habitable for anaerobic and thermophilic/hyperthermophilic chemoautotrophs. Alternatively, the organic matter may have been possibly produced by abiological reaction such as Fischer-Tropsch Type (FTT) synthesis under the hydrothermal condition. However, the estimated condition is inconsistent with the presence of the effective catalysts for the FTT reaction (i.e., Fe-Ni alloy, magnetite, and hematite). These lines of evidence suggest the possible existence of biosphere in the ∼3.5 Ga sub-seafloor hydrothermal system.

AB - More than 600 specimens of ∼3.5 Ga-old hydrothermal silica dikes from the North Pole area, Pilbara craton, Western Australia, have been studied petrographically. The kerogens in 44 samples have been analyzed isotopically (C and N) and chemically (C, N, and H). The silica dikes are composed mainly of fine-grained silica (modal abundance: >97%) and are classified into two types by minor mineral assemblages: B(black)-type and G(gray)-type. The B-type silica dikes contain kerogen (0.37 to 6.72 mgC/g; average 2.44 mgC/g, n = 21) and disseminated sulfides, dominantly pyrite and Fe-poor sphalerite. In some cases, carbonate and apatite are also present. Their silica-dominated and sulfide-poor mineral assemblages suggest precipitation from low-temperature reducing hydrothermal fluid (likely 100-200°C). On the other hand, the G-type silica dikes are sulfide-free and concentrations of kerogen are relatively low (0.05 to 0.41 mgC/g; average 0.17 mgC/g, n = 13). They typically contain Fe-oxide (mainly hematite) which commonly replaces cubic pyrite and rhombic carbonate. Some G-types occur along secondary quartz veins. These textures indicate that the G-type silica dikes were formed by postdepositional metasomatism (oxidation) of the B-types, and that the B-types probably possess premetasomatic signatures. The δ13C values of kerogen in the B-types are -38.1 to -33.1‰ (average -35.9‰, n = 21), which are ∼4‰ lower than those of the G-types (-34.5 to -30.0‰; average -32.2‰, n=19), and ∼6‰ lower than bedded chert (-31.2 to -29.4‰; average -30.5‰, n= 4). This indicates the preferential loss of 12C during the metasomatism (estimated fractionation factor: 0.9985). Considering the metasomatic effect on carbon isotopes with probably minor diagenetic and metamorphic overprints, we conclude that the original δ13C values of the kerogen in the silica dikes would have been heterogeneous (∼5‰) and at least some material had initial δ13C values of ≤ -38‰. The inferred 13C-depletions of organic carbon could have been produced by anaerobic chemoautotrophs such as methanogen, but not by aerobic p hotoautotrophs. This is consistent with the estimated physical and chemical condition of the hydrothermal fluid, which was probably habitable for anaerobic and thermophilic/hyperthermophilic chemoautotrophs. Alternatively, the organic matter may have been possibly produced by abiological reaction such as Fischer-Tropsch Type (FTT) synthesis under the hydrothermal condition. However, the estimated condition is inconsistent with the presence of the effective catalysts for the FTT reaction (i.e., Fe-Ni alloy, magnetite, and hematite). These lines of evidence suggest the possible existence of biosphere in the ∼3.5 Ga sub-seafloor hydrothermal system.

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