Petrogenesis of the 1.9 Ga mafic hanging wall sequence to the Flin Flon, Callinan, and Triple 7 massive sulphide deposits, Flin Flon, Manitoba, CanadaThis is a companion paper to DeWolfe, Y.M., Gibson, H.L., Lafrance , B., and Bailes, A.H. 2009. Volcanic reconstruction of Paleoproterozoic arc volcanoes: the Hidden and Louis formations, Flin Flon, Manitoba, Canada. Canadian Journal of Earth Sciences, <b>46</b>: this issue.

DeWolfe, Y.M.; Gibson, H. L.; Piercey, Stephen J.

doi:10.1139/e09-033

Cited by 17 publications

(9 citation statements)

References 33 publications

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“…The rocks of the Flin Flon arc assemblage have been altered by the hydrothermal activity that also led to VMS ore formation. Consequently, the Hidden and Louis formation rocks (DeWolfe et al 2009b) have a mineralogical assemblage that is comparable to other hydrothermally altered and metamorphosed (greenschist facies) Precambrian greenstone (e.g., Nakamura and Kato 2004;Polat et al 2012).…”

Section: Pre-weathering Submarine Alterationmentioning

confidence: 96%

“…Of the individual tectono-stratgraphic assemblages that make up the Amisk collage, the juvenile, arc-associated rocks of the Flin Flon arc assemblage (formerly the Amisk Group), are the most intensively studied, since they contain three major economic volcanogenic massive sulphide (VMS) deposits (e.g., Syme and Bailes 1993;Galley et al 2007). Recent investigations have resulted in a well-defined internal subdivision of the Flin Flon arc assemblage into footwall and hanging wall units with geologically and geochemically distinct "formations" and "members" (Syme and Bailes, 1993;Ames et al 2002;DeWolfe et al 2009aDeWolfe et al , 2009b. Three formations (Flin Flon, Louis, and Hidden) have been defined in the assemblage beginning with the minor rhyolitic volcanism that formed the ore-hosting units (the Flin Flon formation) during extensional arc-rifting (Syme and Bailes 1993;Syme et al 1999).…”

Section: Flin Flon Arc Assemblagementioning

confidence: 99%

“…Three formations (Flin Flon, Louis, and Hidden) have been defined in the assemblage beginning with the minor rhyolitic volcanism that formed the ore-hosting units (the Flin Flon formation) during extensional arc-rifting (Syme and Bailes 1993;Syme et al 1999). The succeeding hanging wall formations (the Hidden and Louis) appear to record the transition back to a convergent environment marked by a resurgence of basaltic volcanism following ore deposition (DeWolfe et al 2009a(DeWolfe et al , 2009b. The Hidden and Louis formations are of specific interest to the present study, since they were the most widely exposed to Paleoproterozoic subaerial weathering upon uplift of the assemblage.…”

Section: Flin Flon Arc Assemblagementioning

confidence: 99%

“…The Hidden and Louis formations are of specific interest to the present study, since they were the most widely exposed to Paleoproterozoic subaerial weathering upon uplift of the assemblage. The Hidden and Louis formations (DeWolfe et al 2009a(DeWolfe et al , 2009b are dominated by aphyric to plagioclase-pyroxene-porphyritic basaltic and basaltic andesite lava flows (pillowed and massive) and synvolcanic intrusions, along with volumetrically minor volcaniclastic units. Physical flow features such as pillows, flow-banding, and hyaloclastite are commonly recognisable in the units, but very little of the primary mineralogy remains.…”

Section: Flin Flon Arc Assemblagementioning

confidence: 99%

“…However, there is no part that is sufficiently unweathered to determine its initial mobile, major-element (Ca, Mg, Na, K) composition. Thus, constraints must be made from the chemistry of the immobile elements and through comparison with other volcanic rocks from the Hidden formation (DeWolfe et al 2009b). These data are plotted in the supplementary material section.…”

Section: Significance Of Separate Lava Flows In the Profilementioning

confidence: 99%

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The Flin Flon paleosol revisited

Babechuk

Kamber

2013

Can. J. Earth Sci.

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A ca. 1.85 Ga paleosol developed on seafloor-altered mafic rocks is preserved beneath continental sandstones and conglomerates of the Missi Group near Flin Flon, Manitoba. Previous work has focused on a locality where the paleosol is developed on pillowed greenstone (chlorite + albite + epidote + calcite + quartz + Fe–Ti oxides ± mica). This area has been revisited and a new (∼5 m) profile was excavated and sampled at a very high density for geochemical (major element; ∼60 samples) and mineralogical (petrography, X-ray diffraction) investigation. The high sampling density has revealed a relatively sharp immobile-element offset (e.g., Al/Ti) in the profile. This could reflect weathering across two separate parent rocks or preferential addition of allochthonous material into the top of the profile. Regardless, comparison with a wide suite of volcanic rocks in the stratigraphy suggests that the original concentration of Fe and probably also Ca and Mg in the greenstone on either side of the boundary was similar, permitting quantitative treatment of major-element trends. The profile shows pronounced upward loss of Ca, Mg, Mn2+, and Fe2+ and a corresponding increase in Al, Ti, and total Fe. Physical weathering features, such as corestones, are well preserved and show progressive alteration upwards in the profile in parallel with the chemical trends. Deep in the profile, Na and Ca are lower than the greenstone due to the weathering of albite and epidote, whereas Mg, Fe, and Mn were largely retained in chlorite and secondary dolomite. Upwards in the profile, the loss of chlorite and dolomite and the increase of illite – mixed-layer clays and white mica (probably 2:1 layer or mixed-layer clays originally) and hematite are accompanied by a transition from green to maroon colour. Above a well-defined depth in the profile, carbonate is virtually absent, and the paleosol is highly depleted in Ca. This transition in the paleosol coincides with the immobile-element offset. The significance of this coincidence remains to be explored. Reworking of regolith (e.g., rip-up clasts) occurred during deposition of the Missi sediments, and burial and subsequent metamorphism resulted in the upward enrichment of K and Na and the associated conversion of pedogenic clays to illite and micas (muscovite and paragonite). Crosscutting quartz and epidote veins and tourmaline formation near the unconformity contact implies minor post-burial fluid movement. Despite these complexities, there is consistent retention of Fe through formation of pedogenic Fe oxides, attested by the near-constant ∑Fe/Al ratio in the profile. There is very little evidence for subsequent Fe reduction by hydrothermal or organic fluids. Instead, trends in the Fe speciation are controlled predominantly by the modal variation of Fe–Ti oxides in the greenstone and spheroidal weathering textures in the paleosol.

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Section: Pre-weathering Submarine Alterationmentioning

confidence: 96%