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

1999 ◽  
Vol 36 (11) ◽  
pp. 1901-1915 ◽  
Author(s):  
D F Gale ◽  
S B Lucas ◽  
J M Dixon
Keyword(s):  
Sedimentary Cover ◽  
Sedimentary Rocks ◽  
Massive Sulphide ◽  
Volcanogenic Massive Sulphide ◽  
Deformation Event ◽  
Flin Flon ◽  
Structural Relations

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.

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

2009 ◽  
Vol 46 (7) ◽  
pp. 481-508 ◽  
Author(s):  
Y. M. DeWolfe ◽  
H. L. Gibson ◽  
B. Lafrance ◽  
A. H. Bailes
Keyword(s):  
Hanging Wall ◽  
Massive Sulphide ◽  
Gradual Change ◽  
Shield Volcano ◽  
Ore Formation ◽  
Massive Sulphide Deposits ◽  
Volcanogenic Massive Sulphide ◽  
Volcaniclastic Rocks ◽  
Flin Flon ◽  
Sulphide Deposits

The hanging wall to the Flin Flon, Callinan, and Triple 7 volcanogenic massive sulphide deposits of the Flin Flon district is composed of the Hidden and Louis formations. The contact between these formations is marked by mafic tuff that represents a hiatus in effusive volcanism. The formations form a composite volcanic edifice that was erupted and grew within a large, volcanic–tectonic subsidence structure (hosting the deposits) that developed within a rifted-arc environment. The formations are evidence of resurgent effusive volcanism and subsidence following a hiatus in volcanism marked by ore formation since they consist of dominantly basaltic flows, sills, and volcaniclastic rocks with subordinate basaltic andesite and rhyodacitic flows and volcaniclastic rocks. The Hidden formation is interpreted to represent a small shield volcano and the Louis formation a separate shield volcano that developed on its flank. Both the Hidden and Louis volcanic edifices were constructed by continuous, low-volume eruptions of pillow lava. A gradual change from a dominantly extensional environment during the formation of the footwall Flin Flon formation to a progressively more dominant convergent environment during the emplacement of the hanging wall suggests that the Hidden and Louis formations are unlikely to host significant volcanogenic massive sulphide-type mineralization. However, synvolcanic structures in the formations define structural corridors that project downwards into the footwall where they encompass massive sulphide mineralization, indicating their control on ore formation, longevity,and reactivation as magma and fluid pathways during the growth of the Hidden and Louis volcanoes.

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, 46: this issue.

2009 ◽  
Vol 46 (7) ◽  
pp. 509-527 ◽  
Author(s):  
Y. M. DeWolfe ◽  
H. L. Gibson ◽  
S. J. Piercey
Keyword(s):  
Oceanic Crust ◽  
Basaltic Andesite ◽  
Hanging Wall ◽  
Volcanic Rocks ◽  
Companion Paper ◽  
Massive Sulphide ◽  
Massive Sulphide Deposits ◽  
Volcanogenic Massive Sulphide ◽  
Flin Flon ◽  
Sulphide Deposits

A detailed study of the geochemical and isotopic characteristics of the volcanic rocks of the Hidden and Louis formations, which make up the hanging wall to the volcanogenic massive sulphide deposits at Flin Flon, Manitoba, was carried out on a stratigraphically controlled set of samples. The stratigraphy consists of the lowermost, dominantly basaltic, Hidden formation, and the overlying, dominantly basaltic, Louis formation. Of importance petrogenetically, is the 1920 unit a basaltic andesite with Nb/Thmn = 0.54–0.62, εNd(1.9Ga) = +3.6–+5.9, εHf(1.9Ga) = +8.5–+9.6, and 204Pb/206Pb = 23.9. The basaltic flows that dominate the Hidden formation have Nb/Thmn = 0.16–0.29, εNd(1.9Ga) = +1.7–+4.4, εHf(1.9Ga) = +7.0–+11.8 and 204Pb/206Pb = 16.9–18.6). The Carlisle Lake basaltic–andesite (top of Hidden formation) is characterized by Nb/Thmn = 0.16–0.14, and 204Pb/206Pb = 21.4. The rhyodacitic Tower member (bottom of Louis formation) has Nb/Thmn = 0.23, εNd1.9Ga = +4.6, εHf1.9Ga = +9.3, and 204Pb/206Pb = 22.2. The basaltic flows that dominate the Louis formation have Nb/Thmn = 0.18–0.25, εNd(1.9Ga) = +3.6–+4.2, εHf(1.9Ga) = +8.4–+11.3 and 204Pb/206Pb = 17.9. The Hidden and Louis formations show dominantly transitional arc tholeiite signatures, with the 1920 unit having arc tholeiite characteristics. It is interpreted to have formed through extensive fractional crystallization of differentiated magmas at shallow levels in oceanic crust. Given the geological, geochemical, and isotopic characteristics of the Hidden and Louis formations, they are interpreted to represent subducted slab metasomatism with minor contamination from subducted sediments.

Mode-converted volcanogenic massive sulphide ore lens reflections in vertical seismic profiles from Flin Flon, Manitoba, Canada

2015 ◽  
Vol 63 (4) ◽  
pp. 849-860 ◽  
Author(s):  
D.M. Melanson ◽  
D.J. White ◽  
C. Samson ◽  
G. Bellefleur ◽  
E. Schetselaar ◽  
...  
Keyword(s):  
Massive Sulphide ◽  
Seismic Profiles ◽  
Vertical Seismic Profiles ◽  
Sulphide Ore ◽  
Volcanogenic Massive Sulphide ◽  
Flin Flon

Evolution of the Paleoproterozoic Snow Lake arc assemblage and geodynamic setting for associated volcanic-hosted massive sulphide deposits, Flin Flon Belt, Manitoba, Canada

1999 ◽  
Vol 36 (11) ◽  
pp. 1789-1805 ◽  
Author(s):  
Alan H Bailes ◽  
Alan G Galley
Keyword(s):  
High Heat ◽  
Massive Sulphide ◽  
Geodynamic Setting ◽  
Hydrous Melting ◽  
Volcanogenic Massive Sulphide ◽  
Vms Deposits ◽  
Mantle Sources ◽  
Flin Flon ◽  
East End ◽  
Fault Scarps

The majority of volcanogenic massive sulphide (VMS) deposits at the east end of the Paleoproterozoic Flin Flon "greenstone" belt occur in the 1.89 Ga Snow Lake arc assemblage. VMS deposits in this isotopically juvenile oceanic arc sequence are hosted within a 6 km thick monoclinal section that records in its stratigraphy and geochemistry a temporal evolution in arc development from primitive, through mature, to arc rift. VMS deposits occur in both the primitive and mature arc sequences and are interpreted to be products of arc extension and accompanying anomolously high heat flow, fracturing, and fluid circulation. Boninites, low-Ti tholeiites, and isotopically juvenile rhyolite flows, a rock association that has been attributed in both modern and Phanerozoic arcs to high-temperature hydrous melting of refractory mantle sources in an extensional and (or) proto-arc environment, forms the primitive arc. Indication that the mature arc also underwent extension includes voluminous volcaniclastic detritus (from fault scarps?), prominent synvolcanic dykes, isotopically juvenile rhyolite flows, and the fact that the mature arc is stratigraphically overlain by arc-rift basalts with MORB-like geochemistry. Interpretation of VMS deposits at Snow Lake as products of an extensional geodynamic setting suggests that the traditional Flin Flon Belt exploration model, invoking "pluton-generated" convective seawater, be augmented by the search for evidence of rifting. Economically significant rock associations at Snow Lake include geochemically primitive refractory mafic magmas (e.g., boninites), isotopically juvenile felsic magmas, bimodal basalt-rhyolite sequences, and arc-rift basalts.

KERCH STRAIT IN KAMYSH-BURUN SPIT AREA: HIGH-RESOLUTION SEISMOACOUSTIC APPROACH

2018 ◽  
Author(s):  
В. Зинько ◽  
V. Zin'ko ◽  
А. Зверев ◽  
A. Zverev ◽  
М. Федин ◽  
...  
Keyword(s):  
High Resolution ◽  
Fracture Zone ◽  
Sedimentary Cover ◽  
Sedimentary Rocks ◽  
The West ◽  
Early Generation ◽  
The Third ◽  
Azov Sea ◽  
Kerch Strait ◽  
Made In

The seismoacoustical investigations was made in the western part of the Kerch strait (Azov sea) near Kamysh-Burun spit. The fracture zone with dislocated sedimentary rocks layers and buried erosional surface was revealed to the west of spit. Three seismofacial units was revealed to the east of spit. The first unit was modern sedimentary cover. The second ones has cross-bedding features and was, probably, the part of early generation of Kamysh-Burun spit, which lied to the east of its modern position. The lower border of the second unit is the erosional surface supposed of phanagorian age. The third unit is screened by acoustic shedows in large part.

scholarly journals The Coulon deposit: quantifying alteration in volcanogenic massive sulphide systems modified by amphibolite-facies metamorphism

2016 ◽  
Vol 53 (12) ◽  
pp. 1443-1457 ◽  
Author(s):  
Lucie Mathieu ◽  
Rose-Anne Bouchard ◽  
Vital Pearson ◽  
Réal Daigneault
Keyword(s):  
Mass Balance ◽  
Massive Sulphide ◽  
Amphibolite Facies ◽  
High Grade ◽  
Bay Area ◽  
Volcanogenic Massive Sulphide ◽  
High Grade Metamorphism ◽  
And Performance ◽  
Superior Craton ◽  
Ore Zones

The Coulon deposit is a volcanogenic massive sulphide (VMS) system in the James Bay area, Superior craton, Quebec, that was metamorphosed to amphibolite-facies conditions. The chemistry and mineralogy of the VMS-related alteration halo proximal to the mineralized sulphide lenses are investigated, using samples collected in the field and 5583 chemical analyses provided by Osisko Ltd. Alteration is quantified using mass balance and normative calculations, and the application and performance of these methods in an exploration context are investigated. In VMS systems, altered rocks proximal to the ore zones are characterized by multi-element metasomatism, which is best quantified by mass balance methods that have been successfully applied in the study area. However, mass balance calculations necessitate the documentation of a precursor, which is not always possible in an exploration context; therefore, an alternative method (i.e., alteration indices) was also evaluated. In most VMS systems, proximal alteration is characterized by chlorite (chloritization), muscovite (sericitization), and quartz (silicification), while at the Coulon deposit, altered rocks contain mostly cordierite, biotite, sillimanite, and quartz. Alteration indices were calculated using observed and normative minerals, and provide satisfactory results similar to those obtained with mass balance calculations. Using these results, recommendations are made to estimate the intensity of alteration in the core shack using the proportions of observed minerals. Alteration indices are sensitive to the composition of precursors; and because of high-grade metamorphism, chloritization and sericitization are not precisely quantified. Recognizing these limitations is essential to successful quantification of alteration in areas metamorphosed to high-grade conditions.

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