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New Developments in Grenville Geology and Remote Sensing Fort-Coulonge Region, Western Quebec

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New Developments in Grenville Geology and Remote Sensing Fort-Coulonge Region, Western Quebec GM 66922 NEW DEVELOPMENTS IN GRENVILLE GEOLOGY AND REMOTE SENSING, GUIDEBOOK FIELD TRIP B3, FORT-COULONGE REGION, WESTERN QUEBEC NEW DEVELOPMENTS IN GRENVILLE GEOLOGY AND REMOTE SENSING FORT-COULONGE REGION, WESTERN QUEBEC GM 6 692 2 By Kamal N.M. Sharma', Vernon H. Singhroy2 Louis Madore', Josée Lévesque2 Emmanuelle Giguère', Jules Cimon' 1 - Ministère des Ressources naturelles du Québec 2 - Canada Centre for Remote sensing GUIDEBOOK FIELD TRIP B3 OTTAWA '97 GAC/MAC Annual Meeting Ressources naturelles et Faune, Québec 1 3 MARS 2013 DIR. INFORM. GÉOL. 2 INTRODUCTION Due to its geographic location, the Fort-Coulonge region (Figure 1) stretching from the Ottawa River in the south to the Cabonga Reservoir in the north, occupies a structurally unique and interesting position within the western part of the Grenville Province in Québec. It includes parts of two major lithotectonic domains : the western portion of the Central Metasedimentary Belt (CMB), and west of it, an extensive portion of the Central Gneiss Belt (CGB). The nomenclature used is the one introduced by Wynne-Edwards (1972). The Cayamant Lineament (Sharma et al. 1992) marks the limit between the Grenville Supergroup supracrustal rocks of the CMB to the east and the tonalitic - dioritic - granodioritic - granitic gneiss complexes and amphibolites of the CGB to the west. The Baskatong-Desert Lineament subdivides the CGB into two terranes, the Baskatong-Dozois Terrane and the Pythonga Terrane, respectively to the north and to the south of the lineament (Sharma, 1991 and Sharma et al., 1992. The present level of erosion lies very close to the surface or surfaces along which the supracrustal sequence of the CMB was transported towards NW and overthrust upon the adjacent gneissic terranes of the CGB. The sectors situated west of the Cayamant Lineament are thus dominated by the gneiss complexes of the CGB overlain by the metasedimentary rocks once part of the main body of the CMB. Consequently, the metasedimentary rocks and associated anorthositic rocks are present to the west of the Cayamant Lineament only as parts of the thrust nappes and in numerous small bodies representing the erosional relics of nearly entirely eroded nappes. The larger nappes consisting of supracrustal rocks are exemplified by the Fort-Coulonge and Cabonga nappes. During the northwest overthrusting of the metasedimentary pile over the adjacent gneissic terranes, the gneiss complexes composing these terranes did not remain unaffected, nor did they behave passively. In fact, these gneisses suffered intense deformation and were themselves thrust towards NW along subhorizontal to gently dipping decollements within the gneiss complexes, resulting in numerous thrust nappes consisting of gneiss complex rocks. It is within these deformation zones that numerous tectonic slivers of ultramafic rocks have been observed in the Fort-Coulonge area, as well as further northwestward in the Temiscaming region. 1 3 4 The field excursion is devoted to the observations of the structural and lithological characteris- tics of the Cayamant Lineament, Pythonga Terrane, thrust nappes consisting of the supracrustal rocks and of the gneiss complex rocks, and the occurrence of the ultramafic rocks. PREVIOUS WORK The earliest geological observations made in the area were in 1845 by Sir William Logan (1847) who examined the rocks along the Ottawa river during the reconnaissance work between Bytown (Ottawa) and Lake Temiscamang (Témiscamingue). In 1876, Henry G. Vennor and his assistant Lewis R. Ord carried out investigations along the Ottawa river and the southern portions of the Coulonge and Black (Noire) rivers. R.W. Ells (1907) made longer traverses along the Black (Noire) and Coulonge rivers up to a distance of about 70 miles northward from their junction with the Ottawa river. More recently, the geological mapping done within parts of the area covered by the excursion include : reconnaissance mapping at 1:253 440 scale along Coulonge and Black (Noire) rivers by Retty (1933). j mapping of Portage-du-Fort and lac Saint-Patrice area at 1:F6 720 scale by Katz (1976). excellent detail mapping of Fort-Coulonge - Otter lake - Kazabazua area at 1:63 360 scale by Kretz (1977). MAJOR STRUCTURES AND TECTONIC SUBDIVISIONS We started our field observations in the Fort-Coulonge region in 1989 with the objective to revise and reinterpret the pre-existing geological maps. Between 1989 and 1992, an equivalent of about two summer's work was devoted to a vast reconnaissance program to familiarize ourselves with the area and to outline the problems. At the same time we undertook a detailed structural interpretation of the satellite SEASAT-RADAR images covering 200 km x 100 km, 5 and of the Airborne - RADAR images covering 200 km x 18 km (Figure 2). The high-reso- lution Airborne-RADAR images were flown especially for us in 1989 by the Canada Centre for Remote Sensing to study the nature of the limit between the supracrustal rocks of the CMB and the gneiss complexes of the CGB. These interprations (Figure 3) provided high quality structural information, and have been instrumental to bring out several major structures, of fundamental importance, and which were previously unknown, e.g. Cayamant Lineament, Baskatong-Desert Lineament, NW-trending nappe structures, rare NE-trending nappe structure, brittle fractures related to the Ottawa-Bonnechère graben system etc. All these structures were well understood by 1991 (Lévesque and Sharma, 1991 ; Sharma, 1991). Following these studies, a systematic mapping program has been in progress since 1993 to present involving K.N.M. Sharma, Louis Madore, Emmanuelle Giguère, Jules Cimon, Josée Lévesque, and Vernon H. Singhroy. Between 1993 and 1996 an area covering approximately 10 000 km2 has been systematically mapped from the Ottawa River in the south to the Baskatong-Desert Lineament towards north (Figure 1). Cavamant Lineament The two major lithotectonic domains - the Central Metasedimentary Belt and the Central Gneiss Belt - are juxtaposed along the Cayamant Lineament or the Cayamant Shear Zone (Figures 1 and 3). This lineament is significant for several reasons, the most important being that in addition to marking the western limit of the main body of the CMB, it also represents a major shear zone resulting from the overthrusting, towards W and NW, of the supracrustal pile, transported from the CMB, on top of the adjacent gneissic terranes (Pythonga and Baskatong- Dozois Terranes, subdivisions of the CGB). The Cayamant- Lineament thus constrains the western side of the «Central Metasedimentary Belt Boundary». This term must be reserved exclusively for the limits of the main body of the CMB. The southern side of the CMB Boundary is mostly hidden beneath the Paleozoics in Ontario. Our task now is to constrain the northern and eastern sides of the CMB Boundary which are not well understood at the present time. 6 7 8 Most importantly, as a major shear zone, the Cayamant Shear Zone is the first visible manifes- tation of the Basal Thrust Zone. The erosional remnants of this zone are well preserved in numerous exposures all along the Cayamant Lineament. Although the individual exposures may show minor local variations, the Waltham-type Zone is quite representative of the Basal Thrust Zone. Its upper part is composed of strongly tectonized straight-banded diverse litholo- gies including calc-silicate rocks, carbonate injections, and pegmatitic injections. The carbonate injections originate as a result of the remobilization and migration of the marbles originally present within the overlying tectonic pile. The lower part of the zone is characterized by straight-banded lithologies with diverse protoliths, such as granite, pegmatite, tonalite, diorite etc. and only little carbonate injections and calc-silicate rocks. Elsewhere, in its simplest form, the Basal Thrust Zone may simply consist of strongly tectonized metasedimentary rocks above and the gneiss complex rocks below, with a sharp contact between the two. In such cases the gneiss complexes usually show considerable migmatization. Because of erosion it is difficult to estimate as to what could have been the total thickness of the Basal Thrust Zone. The field observations suggest that it must be in the order of several hundred metres. These observations eloquently point out an important fact that the present level of erosion lies very close to the surface or surfaces along which the supracrustal sequence of the CMB was transported towards W and NW and overthrust upon the adjacent gneissic terranes of the CGB. During this event, and at this level, both groups of rocks underwent upper amphibolite to granulite grade metamorphic conditions. This would mean that the present level of observation corresponds to the depth where once the conditions of upper amphibolite to granulite facies predominated. In other words, we are now able to examine quite a deep section — mid-crustal or deeper — through the Grenvillian crust. Such an inference is nothing new. It was already postulated by Wynne-Edwards more than two decades ago : « ... the Grenville Province is a deep section part of an orogenic belt eroded to a level at which reworked sialic basement is the dominant rock-type exposed. » — Wynne-Edwards, 1972. Essentially the same message has been reiterated by Hanmer (1988), Davidson (1986) and others. 9 Now let us move westward from the Cayamant Lineament into the CGB. Central Gneiss Belt and « Tectonic outliers » of supracrustal and anorthositic rocks The presence
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