Geology and ore deposits of the Iron River-Crystal Falls district, Iron County, Michigan

James, Harold L.; Dutton, Christopher J.; Pettijohn, F. J.; Wier, K.L.

doi:10.3133/pp570

Cited by 33 publications

(30 citation statements)

References 18 publications

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“…In the 36 Figure 2B. Simplified geologic map of study area (after Gair and Weir, 1956;Bayley, 1959;James and others, 1966;Weir, 1967;James and others, 1968;Dutton, 1971). …”

Section: Regional Geologymentioning

confidence: 99%

“…Unlike the aforementioned groups, the Paint River Group occurs exclusively in the Crystal Falls and Florence areas and nowhere else in the Lake Superior region (what will later be called the Crystal Falls terrane and Florence-Niagara terrane). James and others (1968) argued that the Paint River Group is stratigraphically the youngest early Proterozoic succession in the Lake Superior region. Cambray (1978) suggested that the Paint River Group strata and underlying pillow basalts are the equivalent of the Menominee Group.…”

Section: Regional Geologymentioning

confidence: 99%

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Early Proterozoic tectonics of the Lake Superior region: Tectonostratigraphic terranes near the purported collision zone

Larue

1983

Early Proterozoic Geology of the Great Lakes Region

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Two assemblages of early Proterozoic rocks are present in the Lake Superior region: a northern miogeoclinal assemblage of stratified rocks overlying Archean basement; and a southern magmatic arc terrane composed of granitoid and volcanic rocks. The structural contact between the miogeoclinal assemblage and the magmatic terrane in northeastern Wisconsin and upper Michigan is the Florence-Niagara fault. Miogeoclinal assemblage rocks directly north of the Florence-Niagara fault in the study area are subdivided into two fault-bound, tectonostratigraphic terranes: the Crystal Falls terrane (or terrane 1); and the Florence-Niagara terrane (or terrane 3). These structural blocks are segregated from the miogeocline proper (terrane 2) to the north because of differences in sedimentary facies, and/or structure. I interpret the Penokean Orogeny (1.8-1.9 b.y.) as a product of the collision between the magmatic terrane and the miogeocline: terranes 1 and 3 probably were emplaced during or after this collision but may have been discrete from the miogeocline prior to collision. It is probable that the early Proterozoic evolution of the Lake Superior region is much like that of Phanerozoic orogens, but gross similarities are obfuscated by the presence of, and the deformation associated with emplacement of, tectonostratigraphic terranes, which occur both in the Phanerozoic and the Precambrian.

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“…In the 36 Figure 2B. Simplified geologic map of study area (after Gair and Weir, 1956;Bayley, 1959;James and others, 1966;Weir, 1967;James and others, 1968;Dutton, 1971). …”

Section: Regional Geologymentioning

confidence: 99%

Section: Regional Geologymentioning

confidence: 99%

Early Proterozoic tectonics of the Lake Superior region: Tectonostratigraphic terranes near the purported collision zone

Larue

1983

Early Proterozoic Geology of the Great Lakes Region

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“…1880 Ma iron formations of the Animikie basin and were likely deposited in deeperwater, below fair-weather and, probably, storm wave base settings. They are present in the: (1) Marquette Iron Range, Michigan (~60-m-thick Bijiki Iron-Formation Member of the Michigamme Slate containing siderite, chert, iron oxides, and silicates; Ojakangas, 1994;Ojakangas et al, 2001;Cannon et al, 2010), (2) Iron River-Crystal Falls Iron Ranges (~15-m-thick chert-siderite slate of the Stambaugh Formation; James et al, 1968), (3) Gogebic Iron Range, Wisconsin (~47-m-thick iron formation of the Tyler Formation consisting of chert and siderite; Schmidt, 1980;Cannon et al, 2008), and (4) Mesabi Iron Range, Minnesota (~27-m-thick chertsiderite iron formation in the lower part of the Virginia Formation; Lucente and Morey, 1983). Deposition of these iron formations might be genetically related to submarine mafic volcanism in the Animikie basin based on spatial association with, for example, the Badwater Greenstone, but this relationship has not been documented in detail.…”

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

834

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 southern more mobile segments have thicker sequences of sediments interbedded with volcanics (Sims et al 1980). The thickness of the Negaunee Iron Formation is 7500 m in the south and thins northward to 2000 m (James et al 1968). …”

Section: Introductionmentioning

confidence: 96%

Sedimentary and metamorphic lithofacies of the Lower Negaunee Iron Formation, Marquette District, Michigan, USA

Pietrzak-Renaud

2013

Can. J. Earth Sci.

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The base of the Proterozoic Negaunee Iron Formation is exposed in the open pit at Tilden Mine, Marquette, Michigan. Juxtaposed against the Archean-aged Palmer Gneiss, it is bounded by the regional-scale Southern Shear Zone and cut by two sets of dykes: an older chloritic and schistose set and a younger 1.1 Ga Keweenawan set. Tilden Mine is dominated by a 100 m scale plunging northwest-anticline and is cut by a growth fault locally termed the Tower Hill Fault that intersects the Southern Shear Zone. The base of the exposed iron formation is composed of three lithofacies, including lower clastics that grade into the overlying banded iron formation that in turn grades upward into granular iron formation. This succession is capped by chloritic metadiabases locally termed the Summit Hill Sill and Pillar Intrusive. Petrographic and mineral chemical investigations document primary or early diagenetic hematite, siderite and possibly ferri-hydrite, metamorphic and related hydrothermal magnetite, chlorite, late martite overgrowing earlier magnetite and growth of specularite. All three lithofacies are cut by brittle fractures and late quartz veins. Brittle fractures are coated with chlorite, carbonate minerals, fluor-apatite, and sparse Cusulphides. These lithofacies document initial clastic sedimentation of strained detrital quartz into a subsiding fault trough. Over time, as subsidence slowed or sea level fluctuated, clastic deposition competed with quiescent chemical sedimentation, leading to deposition of the banded iron formation facies. As a stable shelf platform emerged, the granular iron formation facies was deposited via wave reworking of hardgrounds. Subsequent diagenesis initiated dissolution of carbonate and chert and promoted diagenetic replacement of primary iron minerals and chert. Regional metamorphism during Penokean orogeny at 1875-1835 Ma produced a suite of secondary metamorphic and related hydrothermal minerals. Metamorphism and hydrothermal flux related to the 1750 Ma development of the Republic Metamorphic Node overprinted the iron formation at Tilden to greenschist facies and infilled brittle fractures with a unique mineral assemblage. This unique mineral assemblage exhibits some striking similarities to Mn, Au, and Cu-sulphides documented at Champion Mine, west of Tilden, and proximal to the core of the Republic Node.Résumé : La base de la Formation de fer Negaunee (Protérozoïque) affleure dans la mine Tilden, une fosse à ciel ouvert à Marquette, au Michigan. Juxtaposée au gneiss de Palmer (Archéen), elle est limitée par la zone de cisaillement Southern d'échelle régionale et par deux ensembles de dykes : un ensemble chloriteux et schisteux et un autre plus jeune datant du Keweenawan, 1,1 Ga. La mine Tilden est dominée par un anticlinal d'environ 100 m plongeant vers le nord-ouest et elle est recoupée par une faille synsédimentaire, appelée localement la faille de Tower Hill, qui coupe la zone de cisaillement Southern. La base de la formation de fer qui affleure comprend trois lithofaciès, incluant ...

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Geology and ore deposits of the Iron River-Crystal Falls district, Iron County, Michigan

Cited by 33 publications

References 18 publications

Early Proterozoic tectonics of the Lake Superior region: Tectonostratigraphic terranes near the purported collision zone

Early Proterozoic tectonics of the Lake Superior region: Tectonostratigraphic terranes near the purported collision zone

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

Sedimentary and metamorphic lithofacies of the Lower Negaunee Iron Formation, Marquette District, Michigan, USA

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