A systematic rare-earth elements and yttrium study of Archean cherts at the Mount Goldsworthy greenstone belt in the Pilbara Craton: Implications for the origin of microfossil-bearing black cherts

Sugahara, Haruna; Sugitani, Kenichiro; Mimura, Koichi; Yamashita, Fumiaki; Yamamoto, Koshi

doi:10.1016/j.precamres.2009.10.005

Cited by 47 publications

(34 citation statements)

References 55 publications

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“…This technique failed for analysis of titania, which was below detection (<0.01 wt %) for the two samples (R4336 and R4337), but this sample level was analyzed previously in Japan (Sugahara et al, 2010, sample GFSV6) by XRF at 0.0053 wt %. Many chemical compositions were identical to those previously determined for these rocks by Sugitani et al (2003Sugitani et al ( , 2006, and Sugahara et al (2010). Cores from the abandoned Mt.…”

Section: Introductionsupporting

confidence: 73%

“…Evaporite sand crystals of nahcolite and barite, now pseudomorphed by silica, have been identified from microprobe analyses and crystallographic studies, and interpreted as evaporites of coastal salinas (Sugitani et al, 2003). The overlying Cleaverville Formation of laminated shale and banded iron formation is interbedded with pillow basalts of a volcanic island arc near Karratha in the western Pilbara craton (Shibuya et al, 2007), and includes submarine fan facies turbidites in the southern Pilbara block (Eriksson, 1982;Eriksson et al, 1994 Pool Chert (Sugahara et al, 2010). Two of the seventeen Farrel Quartzite cherts analyzed…”

Section: Sedimentary Paleoenvironmentsmentioning

confidence: 99%

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Archean coastal-plain paleosols and life on land

et al. 2016

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Coastal-plain paleosols in the 3.0 Ga Farrel Quartzite of Western Australia have organic surface (A horizon) and sulfate-rich subsurface (By) horizons, like soils of the Atacama Desert of Chile, Dry Valleys of Antarctica, and 3.7 Ga paleosols of Mars. Farrel Quartzite paleosols include previously described microfossils, permineralized by silica in a way comparable with the Devonian Rhynie Chert, a well known permineralized Histosol. Five microfossil morphotypes in the Farrel Quartzite include a variety of spheroidal cells (Archaeosphaeroides) as well as distinctive large spindles (new genus provisionally assigned to cf. Eopoikilofusa). Previously published cell-specific carbon isotopic analyses of the Farrel Quartzite microfossils, and unusually abundant sulfate considering a likely anoxic atmosphere, allow interpretation of these morphotypes as a terrestrial community of actinobacteria, purple sulfur bacteria, and methanogenic Archaea. Graphical abstract. (see figure) 1 Research highlights  There are coastal-plain paleosols in 3.0 Ga Farrel Quartzite, Western Australia  Paleosols have organic surface (A) and sulfate-rich subsurface (By) horizon. Comparable profiles are known from deserts of Chile, Antarctica, and Mars. Microfossils in paleosols included actinobacteria, sulfur bacteria, methanogens.

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Section: Introductionsupporting

confidence: 73%

Section: Sedimentary Paleoenvironmentsmentioning

confidence: 99%

Archean coastal-plain paleosols and life on land

et al. 2016

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“…3.02 Ga Cleaverville Formation of the Gorge Creek Group consists predominantly of chert with some intercalations of BIF ( Fig. 2A), black shale, and siltstone (Sugitani et al, 2006;Sugahara et al, 2010), and is similar to chert successions in Paleoarchean greenstone belts (see below). Shallow-water to subaerial quartz sandstone is overlain by finely laminated chert and iron formation, suggestive of a deepening-upward sequence.…”

Section: Mesoarchean To Neoarchean Bifsmentioning

confidence: 99%

“…Shallow-water to subaerial quartz sandstone is overlain by finely laminated chert and iron formation, suggestive of a deepening-upward sequence. Petrographic and geochemical evidence has been presented for a hydrothermal influence on deposition of this sequence (Sugitani et al, 2006;Sugahara et al, 2010).…”

Section: Mesoarchean To Neoarchean Bifsmentioning

confidence: 99%

Iron Formation: The Sedimentary Product of a Complex Interplay among Mantle, Tectonic, Oceanic, and Biospheric Processes

Bekker¹,

Krapež²,

Slack³

et al. 2010

Economic Geology

806

494

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Iron formations are economically important sedimentary rocks that are most common in Precambrian sedimentary successions. Although many aspects of their origin remain unresolved, it is widely accepted that secular changes in the style of their deposition are linked to environmental and geochemical evolution of Earth. Two types of Precambrian iron formations have been recognized with respect to their depositional setting. Algoma-type iron formations are interlayered with or stratigraphically linked to submarine-emplaced volcanic rocks in greenstone belts and, in some cases, with volcanogenic massive sulfide (VMS) deposits. In contrast, larger Superior-type iron formations are developed in passive-margin sedimentary rock successions and generally lack direct relationships with volcanic rocks. The early distinction made between these two iron-formation types, although mimimized by later studies, remains a valid first approximation. Texturally, iron formations were also divided into two groups. Banded iron formation (BIF) is dominant in Archean to earliest Paleoproterozoic successions, whereas granular iron formation (GIF) is much more common in Paleoproterozoic successions. Secular changes in the style of iron-formation deposition, identified more than 20 years ago, have been linked to diverse environmental changes. Geochronologic studies emphasize the episodic nature of the deposition of giant iron formations, as they are coeval with, and genetically linked to, time periods when large igneous provinces (LIPs) were emplaced. Superior-type iron formation first appeared at ca. 2.6 Ga, when construction of large continents changed the heat flux at the core-mantle boundary. From ca. 2.6 to ca. 2.4 Ga, global mafic magmatism culminated in the deposition of giant Superior-type BIF in South Africa, Australia, Brazil, Russia, and Ukraine. The younger BIFs in this age range were deposited during the early stage of a shift from reducing to oxidizing conditions in the ocean-atmosphere system. Counterintuitively, enhanced magmatism at 2.50 to 2.45 Ga may have triggered atmospheric oxidation. After the rise of atmospheric oxygen during the GOE at ca. 2.4 Ga, GIF became abundant in the rock record, compared to the predominance of BIF prior to the Great Oxidation Event (GOE). Iron formations generally disappeared at ca. 1.85 Ga, reappearing at the end of the Neoproterozoic, again tied to periods of intense magmatic activity and also, in this case, to global glaciations, the so-called Snowball Earth events. By the Phanerozoic, marine iron deposition was restricted to local areas of closed to semiclosed basins, where volcanic and hydrothermal activity was extensive (e.g., backarc basins), with ironstones additionally being linked to periods of intense magmatic activity and ocean anoxia.Late Paleoproterozoic iron formations and Paleozoic ironstones were deposited at the redoxcline where biological and nonbiological oxidation occurred. In contrast, older iron formations were deposited in anoxic oceans, where ferrous iron oxid...

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“…The Y/Ho ratios are also indicative of Mn sources . The Y/Ho ratios of Permian samples collected here vary from 25.9 to 44.4 (mean 36.1) (Table 3) (Liu et al, 2008;Yang et al, 2009), and fall among seawater ratios (range 44-47) (Bau et al, 1996), shales, chondrites, the lithosphere and most volcanic rocks ratios (range 25-28) (McLennan, 1989), and hydrothermal water (Y/Ho = 26-27) (Pack et al, 2007;Sugahara et al, 2010), indicating multiple sources.…”

Section: Sources Of Manganesementioning

confidence: 87%