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Ma préoccupation au début de cette recherche était de voir comment se présentait la vie associative des personnes âgées considérant les valeurs culturelles et les bouleversements socio-administratifs considérables auxquels sont confrontés les Amérindiens depuis quelques décades. Mes lectures et mes observations sur le terrain m'amenèrent à des réflexions encore plus générales. La récente publication Vieillir à travers le monde (Santerre et Létourneau 1989) m'a incité à revoir ma trajectoire, en m'invitant à considérer l'influence de la modernisation sur les personnes âgées. Même si la modernisation et l'urbanisation rapide du Québec datent du début du siècle, les effets manifestes sur les personnes âgées ne se font sentir que depuis quelques dizaines d'années. Après avoir investi massivement dans les services aux personnes âgées, l'État québécois constate depuis quelques années son incapacité financière à répondre seul aux besoins grandissants des personnes âgées. C'est ainsi que les organismes communautaires furent sollicités pour assumer des responsabilités nouvelles et plus intenses. Trop absorbés à répondre d'urgence aux besoins des aînés en perte d'autonomie, autant l'État que les citoyens donnent l'impression de considérer les personnes âgées comme un fardeau plutôt comme des collaborateurs au développement social et économique. Il s'agit d'une grave lacune car le retrait trop hâtif des personnes âgées constitue un "manque à gagner" important autant dans le domaine culturel que dans le domaine économique.

The map shows the predominantly Precambrian geology of this area. It includes mining claims and properties. There is also a summary of metal production in the Cobalt Silver area between 1904 and 1962., The map shows the predominantly Precambrian geology of this area. It includes mining claims and properties. There is also a summary of metal production in the Cobalt Silver area between 1904 and 1962.

The map shows the predominantly Precambrian geology of this area. It includes mining claims and properties. There is also a summary of metal production in the Cobalt Silver area between 1904 and 1962., The map shows the predominantly Precambrian geology of this area. It includes mining claims and properties. There is also a summary of metal production in the Cobalt Silver area between 1904 and 1962.

The area lies in a gold mining district. Relatively low values of this metal as well as occurrences of copper, lead, zinc and silver have been reported. Continued exploration is recommended both in the exposed west central Archaean fold belt and in the basement complex underlying Coleman Member., The area lies in a gold mining district. Relatively low values of this metal as well as occurrences of copper, lead, zinc and silver have been reported. Continued exploration is recommended both in the exposed west central Archaean fold belt and in the basement complex underlying Coleman Member.

The map shows the predominantly Precambrian geology of this area. It includes mining claims and properties. There is also a summary of metal production in the Cobalt Silver area between 1904 and 1962., The map shows the predominantly Precambrian geology of this area. It includes mining claims and properties. There is also a summary of metal production in the Cobalt Silver area between 1904 and 1962.

Basement rocks are early and middle Precambrian, overlain by sand, gravel, swamp, and stream deposits of Pleistocene age. The metamorphosed precambrian rocks are intruded by porphyritic granites and dolerite dykes. Mineralisation in the area consists of gold, silver, nickel, copper, cobalt, and asbestos. These all occur as vein-type deposits, with the exception of nickel which occurs as a concordant stratabound deposit associated with komatiitic rocks., Basement rocks are early and middle Precambrian, overlain by sand, gravel, swamp, and stream deposits of Pleistocene age. The metamorphosed precambrian rocks are intruded by porphyritic granites and dolerite dykes. Mineralisation in the area consists of gold, silver, nickel, copper, cobalt, and asbestos. These all occur as vein-type deposits, with the exception of nickel which occurs as a concordant stratabound deposit associated with komatiitic rocks.

Gold prospecting activity has taken place in northern Yarrow Township, where a lead mine was also briefly in production. This area lies to the south of the probable western extension of the Kirkland Lake-Larder Lake fault zone. Barite is currently produced in western Yarrow Township., Gold prospecting activity has taken place in northern Yarrow Township, where a lead mine was also briefly in production. This area lies to the south of the probable western extension of the Kirkland Lake-Larder Lake fault zone. Barite is currently produced in western Yarrow Township.

The Keewatin and Timiskaming metasediments of the Porcupine Syncline form three northeast-plunging synclinal structures. The synclines are hook-shaped, each with a long north limb and short south limb. The most northerly fold is the principal fold of the Porcupine Syncline, and is defined by surface exposures. The two southerly synclines are exposed in the Dome mine. The morphology of the synclines and the nature of the boundaries between them suggests that the structures were initiated during the development of the volcanic-turbidite basin, and that they were modified by later tectonic deformation. Volcanic flow rocks interfinger with volcanic metasediments and chemogenic metasediments at the "Greenstone nose". However these metasediments do not pass laterally to the south-facing turbidite sequence. Thus the volcanic rocks do not face south but are more reasonably interpreted as a north-facing sequence. The gold-bearing units include: quartz-carbonate veins, ankerite-rich chemogenic and fine-grained metasediments related to carbonatized mafic flows, and bedded lenticular units of conglomerate with quartz carbonate matrix., The Keewatin and Timiskaming metasediments of the Porcupine Syncline form three northeast-plunging synclinal structures. The synclines are hook-shaped, each with a long north limb and short south limb. The most northerly fold is the principal fold of the Porcupine Syncline, and is defined by surface exposures. The two southerly synclines are exposed in the Dome mine. The morphology of the synclines and the nature of the boundaries between them suggests that the structures were initiated during the development of the volcanic-turbidite basin, and that they were modified by later tectonic deformation. Volcanic flow rocks interfinger with volcanic metasediments and chemogenic metasediments at the "Greenstone nose". However these metasediments do not pass laterally to the south-facing turbidite sequence. Thus the volcanic rocks do not face south but are more reasonably interpreted as a north-facing sequence. The gold-bearing units include: quartz-carbonate veins, ankerite-rich chemogenic and fine-grained metasediments related to carbonatized mafic flows, and bedded lenticular units of conglomerate with quartz carbonate matrix.

Structural and geochronological data are presented which more precisely define the stratigraphy and the generation, timing and effects of deformation in the area. There were several phases of Au mineralisation. Clasts of ankerite veins occur in Timiskaming assemblage conglomerate at the Dome mine, and D3 foliation and folds crosscut early ankerite veining and alteration and some quartz veining. Low-grade mineralisation and possibly the quartz-fuchsite veins predate Timiskaming sedimentation and most of the Au postdates Timiskaming sedimentation. Quartz-carbonate-tourmaline-Au veins fanned within Timiskaming assemblage and Tisdale assemblage rocks. The Au deposits developed largely as oblique slip and extensional vein arrays formed during north-south shortening and local strike-slip faulting. Younger deposits are associated with D4 dip-slip faulting and were weakly deformed during late D4. The lode Au camp formed throughout protracted orogenesis consisting of a broadly transpressional regime with unusually well-developed early thrusting., Structural and geochronological data are presented which more precisely define the stratigraphy and the generation, timing and effects of deformation in the area. There were several phases of Au mineralisation. Clasts of ankerite veins occur in Timiskaming assemblage conglomerate at the Dome mine, and D3 foliation and folds crosscut early ankerite veining and alteration and some quartz veining. Low-grade mineralisation and possibly the quartz-fuchsite veins predate Timiskaming sedimentation and most of the Au postdates Timiskaming sedimentation. Quartz-carbonate-tourmaline-Au veins fanned within Timiskaming assemblage and Tisdale assemblage rocks. The Au deposits developed largely as oblique slip and extensional vein arrays formed during north-south shortening and local strike-slip faulting. Younger deposits are associated with D4 dip-slip faulting and were weakly deformed during late D4. The lode Au camp formed throughout protracted orogenesis consisting of a broadly transpressional regime with unusually well-developed early thrusting.

The Larder Lake-Cadillac deformation zone (LLCDZ) is a major deformation zone within the southern Abitibi subprovince of the Archaean Superior Province. It hosts several gold deposits, including the Cheminis and the giant Kerr Addison - Chesterville deposits in Ontario. The two deposits occur along a strongly deformed band of Fe-rich tholeiitic basalt and komatiite of the Larder Lake Group (ca. 2 705 Ma), bounded on both sides by younger, less deformed, Timiskaming turbidite (2 680-2 670 Ma). Gold was emplaced during D2 closure of an extensional Timiskaming basin, following the formation of early F1 folds. D2 deformation was a progressive compressive deformation event that began with regional F2 folding and the formation of a regional S2 cleavage, and ended with the localisation of the deformation along the band of older volcanic rocks, the formation of the LLCDZ, and the introduction of gold during south-side-up reverse-slip faulting along the LLCDZ. The presence of weakly deformed syenite dykes suggests a minor magmatic contribution to the gold-bearing hydrothermal fluids. Thus, gold was deposited as hydrothermal fluids flowed upward along the LLCDZ during D2 south-side-up shearing. (Author.), The Larder Lake-Cadillac deformation zone (LLCDZ) is a major deformation zone within the southern Abitibi subprovince of the Archaean Superior Province. It hosts several gold deposits, including the Cheminis and the giant Kerr Addison - Chesterville deposits in Ontario. The two deposits occur along a strongly deformed band of Fe-rich tholeiitic basalt and komatiite of the Larder Lake Group (ca. 2 705 Ma), bounded on both sides by younger, less deformed, Timiskaming turbidite (2 680-2 670 Ma). Gold was emplaced during D2 closure of an extensional Timiskaming basin, following the formation of early F1 folds. D2 deformation was a progressive compressive deformation event that began with regional F2 folding and the formation of a regional S2 cleavage, and ended with the localisation of the deformation along the band of older volcanic rocks, the formation of the LLCDZ, and the introduction of gold during south-side-up reverse-slip faulting along the LLCDZ. The presence of weakly deformed syenite dykes suggests a minor magmatic contribution to the gold-bearing hydrothermal fluids. Thus, gold was deposited as hydrothermal fluids flowed upward along the LLCDZ during D2 south-side-up shearing. (Author.)

The Canadian Malartic Mine consists of an Archaean low-grade bulk tonnage gold deposit (reserves of 10.7 Moz Au at 0.97 g/t) hosted by clastic metasedimentary rocks of the Pontiac Group and subalkaline porphyritic quartz monzodiorite and granodiorite located immediately south of the Larder Lake-Cadillac Fault Zone. Gold mineralisation is characterised by zones of quartz-carbonate vein stockwork and disseminated pyrite with a Au-Te-W-S-Bi-Ag±Pb±Mo metallic signature. Molybdenite from highgrade ore yielded a Re-Os age of ca. 2 664 Ma. A syn-Timiskaming magmatic-hydrothermal early phase of gold mineralisation can be inferred by the metallic signature or the ore, the presence of mineralised stockworks, the potassic alteration (biotite/microcline), and association with porphyritic intrusions. The main characteristics of the Canadian Malartic deposit is best explained by syn-D2 deformation gold (ca. 2 670-2 660 Ma) superimposed onto, or remobilised from, a gold-bearing magmatic/hydrothermal system related to Timiskaming-age porphyritic intrusions emplaced along a major fertile fault zone., The Canadian Malartic Mine consists of an Archaean low-grade bulk tonnage gold deposit (reserves of 10.7 Moz Au at 0.97 g/t) hosted by clastic metasedimentary rocks of the Pontiac Group and subalkaline porphyritic quartz monzodiorite and granodiorite located immediately south of the Larder Lake-Cadillac Fault Zone. Gold mineralisation is characterised by zones of quartz-carbonate vein stockwork and disseminated pyrite with a Au-Te-W-S-Bi-Ag±Pb±Mo metallic signature. Molybdenite from highgrade ore yielded a Re-Os age of ca. 2 664 Ma. A syn-Timiskaming magmatic-hydrothermal early phase of gold mineralisation can be inferred by the metallic signature or the ore, the presence of mineralised stockworks, the potassic alteration (biotite/microcline), and association with porphyritic intrusions. The main characteristics of the Canadian Malartic deposit is best explained by syn-D2 deformation gold (ca. 2 670-2 660 Ma) superimposed onto, or remobilised from, a gold-bearing magmatic/hydrothermal system related to Timiskaming-age porphyritic intrusions emplaced along a major fertile fault zone.

The world-class Roberto gold deposit is a major discovery in the James Bay region. Hosted by less than 2 675Ma (Timiskaming) sedimentary rocks, the deposit is located a few kilometres south of the tectonometamorphic contact between the Opinaca (paragneiss to migmatite) and the La Grande subprovinces. Multiple deformation events, long-lived metamorphic event(s), and magmatic activity constitute a geological context that is favourable for long-lived hydrothermal systems or multiple mineralising and/or remobilisation events. Detailed underground and surface mapping of the ore zones and host rocks of the Roberto gold deposit (Éléonore mine) provide new insights into host-rock variations, relationships between metamorphism and ore zones, syn- to post-mineralisation structural events, and magmatic activity. These have led to a diversity of mineralisation styles including: stockwork of quartz, dravit veinlets with microcline, phlogopite replacement zones with pyrrhotite, arsenopyrite, and löllingite (Roberto zone): quartz, diopside, schorl, arsenopyrite veins (East-Roberto zone); and more atypical ore zones in migmatitic rocks or in biotite, amphibole schist (Lake zone). All of the mineralised zones are deformed and some (e.g. Roberto zone) are locally strongly metamorphosed. The timing of the mineralisation relative to peak metamorphism and the complex geological setting are the dominant factors that influenced the nature of the Roberto deposit., The world-class Roberto gold deposit is a major discovery in the James Bay region. Hosted by less than 2 675Ma (Timiskaming) sedimentary rocks, the deposit is located a few kilometres south of the tectonometamorphic contact between the Opinaca (paragneiss to migmatite) and the La Grande subprovinces. Multiple deformation events, long-lived metamorphic event(s), and magmatic activity constitute a geological context that is favourable for long-lived hydrothermal systems or multiple mineralising and/or remobilisation events. Detailed underground and surface mapping of the ore zones and host rocks of the Roberto gold deposit (Éléonore mine) provide new insights into host-rock variations, relationships between metamorphism and ore zones, syn- to post-mineralisation structural events, and magmatic activity. These have led to a diversity of mineralisation styles including: stockwork of quartz, dravit veinlets with microcline, phlogopite replacement zones with pyrrhotite, arsenopyrite, and löllingite (Roberto zone): quartz, diopside, schorl, arsenopyrite veins (East-Roberto zone); and more atypical ore zones in migmatitic rocks or in biotite, amphibole schist (Lake zone). All of the mineralised zones are deformed and some (e.g. Roberto zone) are locally strongly metamorphosed. The timing of the mineralisation relative to peak metamorphism and the complex geological setting are the dominant factors that influenced the nature of the Roberto deposit.