Structural correlation within the Kapuskasing uplift

Abstract

Comparison of progressive deformation and metamorphic history within and between the tectonic domains of the Kapuskasing uplift indicates significant variation in age and style of deformation across this large segment of the central Superior Province; multiple stages of tonalite and granitoid intrusion, melt generation, polyphase diachronous deformation, and likely rapid deep burial of supracrustal rocks collectively produced the complex character of this example of Archean mid to deep crust. At least four Archean deformation phases are recognized, although not all are of regional extent. Dated structural chronology suggests that the locus of the earliest recorded deformations migrated to deeper crustal levels with time. Pre-2680 Ma deformation (local D1–D2) within high-level tonalites is correlated with deformation in the Michipicoten supracrustal belt. The apparent earliest deformational fabrics at deeper crustal levels in the granulite terrane of the Kapuskasing structural zone occurred between 2660 and 2640 Ma. Archean third and fourth phase deformation phases (~ 2667 to ~ 2629 Ma) are present at mid-crustal and deeper levels and deform post-2667 Ma metaconglomerate; these resulted in large-scale folding and subhorizontal ductile shear zones, which seem to represent an important transitional zone that separated a passive upper crust from continued ductile strain at deeper levels.Subsequent uplift of the high-grade rocks was accomplished in multiple stages, initiated prior to 2.45 Ga and likely culminated around 1.9 Ga, although continued movement occurred as late as 1.14 Ga. The Ivanhoe Lake fault zone, along which much of the uplift must have occurred, exhibits some evidence of ductile deep-thrust-related fabrics, but most of the observed structures are brittle to brittle–ductile and steeply inclined. A broad zone of pervasive cataclasis and brittle–ductile shear zones is a characteristic feature of the fault zone throughout its length, and both dextral and sinistral offset are locally present. Clear ground evidence for major transcurrent or thrust displacements, however, has not been recognized.

Pericontinental Crustal Growth of the Southwestern Abitibi Subprovince, Canada--U-Pb, Hf, and Nd Isotope Evidence

“…Movement on this and other Kapuskasing faults is postulated at various times during the latest Archean and Proterozoic, with both thrust and transcurrent displacements suggested (e.g., Halls et al, 1994). Although subvertical brittle faults that postdate ductile uplift are known within the Kapuskasing structural zone (Bursnall et al, 1994), a steeply dipping crustal-scale boundary between the Wawa and Abitibi subprovinces is not inferred by most workers. Although subvertical brittle faults that postdate ductile uplift are known within the Kapuskasing structural zone (Bursnall et al, 1994), a steeply dipping crustal-scale boundary between the Wawa and Abitibi subprovinces is not inferred by most workers.…”

Automated Gold Grain Counting. Part 1: Why Counts Matter!

“…The Borden gold deposit is located 160 km south-west of Timmins, in the Wawa Subprovince of the Archean Superior Province. The gold deposit occurs in the west trending Borden Lake greenstone belt, in the southern portion of the Kapuskasing Structural Zone [73][74][75][76]. The Borden Lake greenstone belt, which has undergone high-grade metamorphism (up to granulite facies), consists of mafic to ultramafic gneisses, pillow basalts, felsic meta-volcanic rocks, felsic porphyries, and tonalites that are overlain by a >30 m thick suite of Timiskaming-aged clastic metasedimentary rocks [77][78][79][80].…”

Automated Gold Grain Counting. Part 1: Why Counts Matter!

“…The Borden gold deposit is located 160 km south-west of Timmins, in the Wawa Sub-province of the Archean Superior Province. The gold deposit occurs in the west trending Borden Lake greenstone belt in the southern portion of the Kapuskasing Structural Zone [81][82][83]. The Borden Lake greenstone belt, which has undergone high-grade metamorphism (up to granulite facies), consists of mafic to ultramafic gneisses, pillow basalts, felsic meta-volcanic rocks, felsic porphyries, and tonalites that are overlain by a >30 m thick suite of Timiskaming-aged clastic metasedimentary rocks [84][85][86][87].…”