scholarly journals Vein-hosted gold mineralization in the Wilding Lake area, central Newfoundland: structural geology and vein evolution

2020 ◽  
Author(s):  
I W Honsberger ◽  
W Bleeker ◽  
H A I Sandeman ◽  
D T W Evans ◽  
S L Kamo
Keyword(s):  
Structural Geology ◽  
Gold Mineralization ◽  
Lake Area

Regional setting of vein-style gold mineralization around the Goldlund mine, Sandybeach Lake area, northwestern Ontario

1990 ◽  
Vol 27 (12) ◽  
pp. 1590-1608 ◽  
Author(s):  
Lesley Chorlton
Keyword(s):  
Gold Mineralization ◽  
Shear Zones ◽  
Main Body ◽  
Lake Area ◽  
Lateral Shear ◽  
Quartz Veins ◽  
Northwestern Ontario ◽  
Stage 4 ◽  
Shear Sense ◽  
Stage 1

The Sandybeach Lake area was deformed in four stages. Stage 1 produced gently south-southeast-dipping foliations at low angles to bedding. Stage 2 involved draping of these planes and formation of contact-strain aureoles related to the emplacement of granitoid stocks. Stage 3 produced doubly plunging folds, steep foliations, and shear zones, which resulted from regional transpression, with a sinistral lateral shear sense along this arm of the Wabigoon greenstone belt. Stage 4 produced minor folds and shear displacements in some places and final tightening of stage 3 folds in others, compatible with final regional convergence.Regional quartz veins, including those carrying gold, appear to have filled tensional fractures related to bulk belt-perpendicular shortening and belt-parallel extension, sinistral shear, and tightening of folds in sheetlike competent bodies. Veins and mineralization thus coincided with late stage 3 deformation, possibly overlapping stage 4.Auriferous vein occurrences at the Goldlund mine display geometries similar to those of veins in the surrounding region. The main body of auriferous vein mineralization is hosted by a thick, composite metatonalite–metadiorite sheet. The vein system of this zone likely originated during the steepening and axial-plane transposition of the southeast-dipping limb near the southwest-plunging end of a stage 3 fold.

Geology and age of the Morrison porphyry Cu–Au–Mo deposit, Babine Lake area, British Columbia

2016 ◽  
Vol 53 (9) ◽  
pp. 950-978 ◽  
Author(s):  
Lijuan Liu ◽  
Jeremy P. Richards ◽  
Robert A. Creaser ◽  
S. Andrew DuFrane ◽  
Karlis Muehlenbachs ◽  
...  
Keyword(s):  
Meteoric Water ◽  
Gold Mineralization ◽  
Lake Area ◽  
Calc Alkaline ◽  
Porphyry Cu ◽  
High K ◽  
Vein Type ◽  
Intrusive Suite ◽  
Stage 1 ◽  
Porphyry Intrusion

The Morrison porphyry Cu–Au–Mo deposit is genetically and spatially related to Eocene plagioclase–hornblende–biotite porphyry intrusions. One porphyry intrusion yielded a U–Pb age of 52.54 ± 1.05 Ma. Mineralization occurs in three stages: (1) vein-type and disseminated chalcopyrite and minor bornite (associated with potassic alteration and gold mineralization); (2) vein-type molybdenite (associated with weak phyllic alteration); and (3) polymetallic sulfide–carbonate veins (dolomite ± quartz–sphalerite–galena–arsenopyrite–chalcopyrite, associated with weak sericite–carbonate alteration). Re–Os dating of molybdenite yielded ages of 52.54 ± 0.22 and 53.06 ± 0.22 Ma, similar to the age of the host porphyry intrusion. Stage 1 vein fluids were predominantly of magmatic origin: Th = 400–526 °C; salinity = 39.8–47.8 wt.% NaCl equiv.; δ18Ofluid = 3.7‰–6.3‰; disseminated chalcopyrite–pyrite δ34SCDT = 0.2‰ and −0.8‰ (CDT, Canyon Diablo Troilite). Stage 2 fluids were a mixture of magmatic and meteoric water: Th = 320–421 °C; salinity = 37.0–43.1 wt.% NaCl equiv.; δ18Ofluid values range from 0.3‰ to 3.4‰; molybdenite and pyrite δ34SCDT = −2.1‰ and −1.2‰. Stage 3 fluids were predominantly of meteoric water origin: Th = 163–218 °C; salinity = 3.1–3.9 wt.% NaCl equiv.; δ18Ofluid = −2.3‰ to 3.9‰ for early vein quartz, and 1.1‰ to 6.1‰ for late vein dolomite; sphalerite and pyrite δ34SCDT = −7.1‰ to −5.6‰. Morrison is interpreted to be a typical porphyry Cu–Au–Mo deposit related to a calc-alkaline to a high-K calc-alkaline diorite to granodiorite intrusive suite, generated in a continental arc in response to early Eocene subduction of the Kula–Farallon plate beneath North America.

scholarly journals Structural geology, central Sturgeon Lake area, Ontario

1998 ◽  
Author(s):  
M Sanborn-Barrie ◽  
T Skulski
Keyword(s):  
Structural Geology ◽  
Lake Area

scholarly journals Nature and significance of deformation zones on gold mineralization in the Detour Lake area: implications for exploration in Ontario and Quebec

2018 ◽  
Author(s):  
S Castonguay ◽  
B Dubé ◽  
P Mercier-Langevin ◽  
V J McNicoll ◽  
A DeLazzer ◽  
...  
Keyword(s):  
Gold Mineralization ◽  
Lake Area

Structural controls on hypozonal orogenic gold mineralization in the La Ronge Domain, Trans-Hudson Orogen, Saskatchewan

2004 ◽  
Vol 41 (12) ◽  
pp. 1453-1471
Author(s):  
Bruno Lafrance ◽  
Larry M Heaman
Keyword(s):  
Gold Mineralization ◽  
Shear Zones ◽  
Oceanic Lithosphere ◽  
Gold Deposits ◽  
Orogenic Gold ◽  
Lake Area ◽  
Structural Controls ◽  
Quartz Veins ◽  
Metavolcanic Rocks ◽  
Orogenic Gold Mineralization

The La Ronge Domain is a granite–greenstone belt in the Saskatchewan segment of the ca. 1.9–1.8 Ga Trans-Hudson Orogen. The La Ronge volcanic arc was accreted to the Archean Hearne craton from ca. 1.87 to 1.86 Ga. Subduction of oceanic lithosphere beneath the accreted La Ronge – Hearne margin produced a voluminous suite of continental-arc intrusions. In the Waddy Lake area, the 1852.6 ± 1.5 Ma Corner Lake stock and 1859 ± 4 Ma and 1861 ± 2 Ma feldspar porphyry dykes crystallized from magmas generated from melting of the subducted oceanic slab. During the ca. 1.83–1.80 Trans-Hudson collision of the Hearne craton with the Archean Sask and Superior cratons, a penetrative regional foliation and a steeply plunging lineation formed within the La Ronge Domain. During further contraction across the domain, the deformation became localized in dextral and oblique-slip shear zones that generally follow contacts between more competent and less competent rock units. Orogenic gold mineralization is associated with quartz veins that are surrounded by hypozonal potassic and sulfidic alteration zones. The Komis gold deposit, the only past-producing gold mine in the Waddy Lake area, formed in the strain shadow of the Round Lake stock during the development of the regional foliation and lineation. Mineralization is associated with quartz veins that cut through tonalite dykes that behaved more brittlely than the surrounding metavolcanic rocks. The Golden Heart and Corner Lake gold deposits are hosted by south-side-up oblique-slip shear zones, which belong to a regional system of structures that extend from Saskatchewan to Manitoba.

Structural geology of the Knife Lake area of northeastern Minnesota

1941 ◽  
Vol 52 (10) ◽  
pp. 1577-1642 ◽  
Author(s):  
J. W. GRUNER ◽  
C. E. Dutton ◽  
G. R. Gibson ◽  
F. F. Grout
Keyword(s):  
Structural Geology ◽  
Lake Area

Source and timing of gold and other mineralization in the Red Lake area, northwestern Ontario, based on lead-isotope investigations

1993 ◽  
Vol 30 (12) ◽  
pp. 2366-2379 ◽  
Author(s):  
Brian L. Gulson ◽  
Karen J. Mizon ◽  
Brian T. Atkinson
Keyword(s):  
Gold Mineralization ◽  
Volcanic Rocks ◽  
Hydrothermal Activity ◽  
Source Rocks ◽  
Lake Area ◽  
Pb Isotope ◽  
Multistage Processes ◽  
Red Lake ◽  
Felsic Volcanic ◽  
Isotope Analyses

The problems of the timing and source of gold mineralization and the sulfidation mechanism in the Red Lake area, north-western Ontario, have been addressed using more than 300 Pb-isotope analyses of more than 250 samples of sulfides, oxides, gold, and potential source rocks. Base metals and some gold from the Campbell and Dickenson mines are interpreted to have been mainly derived from the mafic–intermediate and felsic volcanic rocks of the lower sequence at ca. 2865 Ma, the model age calculated for samples of gold, chalcopyrite, pyrite, and galena. Other samples of gold are considered to have formed at younger ages, perhaps at ca. 2700 Ma. Differences in isotopic patterns for deposits in possibly different deformation zones but hosted by rocks of the same age and composition, e.g., Campbell–Dickenson, McFinley, Cochenour Willans, are interpreted to mean that some of the deposits formed at different times or from different sources or both (i.e., by multistage processes). The older period of gold mineralization is supported by a 2865 ± 10 Ma Pb–Pb isochron age (mean square of weighted deviates (MSWD) 2.9) for Cu–Ni and Fe sulfides and a similar model age for pyrite from the Bridget Lake prospect in the western sector. Younger mineralization at ca. 2700 Ma is represented by, for example, disseminated sulfides in the Dome stock, Balmer Lake arsenopyrite, the Red Summit mine in the Red Crest stock, sulfides and gold from the McFinley mine, and the model age for the Abino galena. A well-constrained Pb–Pb line for magnetites, mainly from 2700–2730 Ma felsic intrusions, gives an apparent age of 2660 ± 10 Ma (MSWD 3.7). This event may represent late-stage hydrothermal activity. Analyses of gold grains yield very complex isotopic patterns possibly because of remobilization and the very low contents of Pb in the gold grains. In environments such as Red Lake, Pb-isotope analyses of gold appear to give unreliable estimates of genesis and timing.

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