Stratigraphic and tectonic setting of early Proterozoic volcanogenic massive sulfide deposits, Flin Flon, Manitoba

Syme, E C; Bailes, A H

doi:10.2113/gsecongeo.88.3.566

Cited by 75 publications

(26 citation statements)

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“…VMS deposits of this age are known in the hinterland to the south of the Animikie Basin (Schulz and Cannon, 2007), in the Labrador Trough (Barrett et al, 1988), and in the Trans-Hudson orogen (Syme and Bailes, 1993). Submarine volcanic rocks of the Pembine-Wausau terrane of northern Wisconsin were deposited at ca.…”

Section: The Ca 188 Ga Resurgence In Iron Formationsmentioning

confidence: 98%

Iron formations: A global record of Neoarchaean to Palaeoproterozoic environmental history

Konhauser

Planavsky

Hardisty

et al. 2017

Earth-Science Reviews

379

257

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Section: The Ca 188 Ga Resurgence In Iron Formationsmentioning

confidence: 98%

Iron formations: A global record of Neoarchaean to Palaeoproterozoic environmental history

Konhauser

Planavsky

Hardisty

et al. 2017

Earth-Science Reviews

379

257

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“…The ca. 1.88 Ga VMS deposits are known in the hinterland to the south of the Animikie basin (Schulz and Cannon, 2007), in the Labrador trough (Barrett et al, 1988b), and in the Trans-Hudson orogen (Syme and Bailes, 1993). Recent geochronological studies of the host metavolcanic rocks to VMS deposits in the Pembine-Wausau terrane of northern Wisconsin indicate that these deposits formed at ca.…”

Section: Ca 193 To 185 Ga Iron Formations Coeval With Large Vms Dementioning

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

849

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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“…Geologists from the Manitoba and Saskatchewan Geological Surveys have published reports that summarize the detaiied stratigraphy sunoundhg these two deposits (Le., Syme and Bailes, 1993;Thomas, 1994) and the geology in the southern Flin Flon area (i.e. Thomas, 1992).…”

Section: -Flin Fion Arc Assemblagementioning

confidence: 99%

“…Previous studies ( Stauffer and Mukherjee, 1971;Bailes and Syme, 1989;Thomas, 1992Thomas, , 1994 have not focused on the basement-cover contact, and particularly, its dual role as both an unconformity md a thmst fault. Previous structural research (Stauffer and Stockwell, 1960;Bailes and Syme, 1989;Syme et al, 1993;Thomas, 1992Thomas, , 1994. Location of study area is outlined.…”

Section: -Introductionmentioning

confidence: 98%

“…1.1). The first is a package of juvenile isiand-arc tholeiitic volcanic rocks (Flin Flon arc assemblage) which host the ]Fiin Flon and Callinan Cu-Zn massive sulphide deposits (Bailes and Syme, 1989;Syme and Bailes, 1993). The second suite unconforrnably overlies these volcanic rocks, and consists of conglomerates and saridstones (Missi Group), deposited in a continental fluvial sedimentary environment ( Fig.…”

Section: -Introductionmentioning

confidence: 99%

See 1 more Smart Citation

Structural relations between the polydeformed Flin Flon arc assemblage and Missi Group sedimentary rocks, Flin Flon area, Manitoba and Saskatchewan

Gale¹,

Lucas

Dixon

1999

Can. J. Earth Sci.

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The structure of the Flin Flon area (Manitoba and Saskatchewan) has been examined through mapping of mesoscopic and macroscopic structures in both the ca. 1900 Ma Flin Flon arc assemblage volcanic basement and the unconformably overlying (or fault juxtaposed) ca. 1845 Ma Missi Group continental sedimentary cover sequence. The Flin Flon and Callinan volcanogenic massive sulphide orebodies occur within the basalt-dominated basement. The contact between the basement and the cover rocks was investigated in detail during this study. The cover sequence records three principal fold- and foliation-forming events. All deformation observed within the cover sequence is correlative with deformation observed within the volcanic basement. Significant low-angle overlap of basement on cover is attributed to development of a D1 north-verging nappe and subsequent thrust displacement on the overturned basement-cover contact. North-verging D1 structures provide evidence for a distinct post-Missi Group deformation event that preceded regional, southwestward D2 thrusting at peak metamorphic conditions across the southeastern Trans-Hudson Orogen. D2 deformation produced closed to tight, west-verging overturned folds with a well-developed axial planar cleavage and a pervasive extension lineation. D3 deformation generated open folds of the S2 and a weakly to moderately developed spaced axial planar S3 cleavage. D3 and D4 deformations produced sinistral-oblique, brittle-ductile reverse faults that offset all older features.

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Stratigraphic and tectonic setting of early Proterozoic volcanogenic massive sulfide deposits, Flin Flon, Manitoba

Cited by 75 publications

References 0 publications

Iron formations: A global record of Neoarchaean to Palaeoproterozoic environmental history

Iron formations: A global record of Neoarchaean to Palaeoproterozoic environmental history

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

Structural relations between the polydeformed Flin Flon arc assemblage and Missi Group sedimentary rocks, Flin Flon area, Manitoba and Saskatchewan

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