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Ottawa Ontario
MEIOFAUNAL BIOTURBATION OF LATE PLEISTOCENE–HOLOCENE GLACIOMARINE MUD IN THE CHAMPLAIN SEA BASIN, EASTERN CANADA: ORIGIN OF BURROWS, THEIR GEOCHEMICAL IMPLICATIONS, AND PALEOENVIRONMENTAL CONTROLS
Coseismic Coulomb stress changes on intraplate faults in the western Quebec seismic zone following three major earthquakes in the past century
ABSTRACT Prolonged slow cooling (average 1–3 °C/m.y.) of Ottawan phase granulite-facies gneisses (peak temperature ≥850 °C ca. 1090–1080 Ma) through the argon closure temperatures ( T C ) of hornblende ca. 980–920 Ma and biotite ca. 890–820 Ma in the western Grenville Province and in an inlier in the central Appalachians is well established, but its tectonic setting has not been systematically investigated. Here, the case is made that this slow cooling occurred in the suprasolidus cores of large metamorphic core complexes that were exhumed during mid-Ottawan (ca. 1050 Ma) extensional orogenic collapse. The ductile midcrustal metamorphic cores of the large metamorphic core complexes are overlain across gently dipping extensional detachments by a brittle-ductile cover composed of upper orogenic crust, parts of which preserve evidence of relict pre-Ottawan fabrics and peak prograde Ottawan temperatures of <500 °C ( T C of Ar in hornblende), collectively implying thermal, structural, and rheological decoupling across the detachments. Slow average rates of cooling of the orogenic midcrust for >150 m.y. imply an anomalously hot upper mantle and mask short periods of more rapid cooling indicated by analyses of retrograde diffusional mineral zoning patterns. It is suggested that these slow average rates of cooling, coupled with slow average rates of exhumation of ≤0.1 km/m.y. modeled for one data set, were a result of decompression melting of rising asthenosphere and emplacement of voluminous mafic intrusions within or at the base of the crust, which reduced the buoyancy of the residual thinned lithosphere. This process is compatible with either delamination of subcontinental lithospheric mantle or slab rollback. The high-strain extensional detachments of the large metamorphic core complexes are sites of amphibolite-facies retrogression, suggesting a feedback between ingress of hydrous fluid, which was likely derived from beneath the detachment during crystallization of migmatite, and strain. Extensional juxtaposition of the hot midcrust ( T >850 °C) and cooler cover ( T <500 °C) across the detachments led to conductive heating of the base of the cover, locally raising its temperature above 500 °C, as recorded by amphibolite-facies metamorphism and young cooling ages. The slow cooling and exhumation of Grenvillian large metamorphic core complexes contrast with much faster rates in smaller metamorphic core complexes in other settings (e.g., North American Cordillera). The slow rates of these processes in large metamorphic core complexes are attributed to the prolonged high temperature and low viscosity of their metamorphic cores due to proximity of the asthenosphere, and to the intrusion of voluminous asthenospheric mafic magmas that both advected heat and reduced lithospheric buoyancy.
Positive Correlation between DYFI Intensity Data and Microzonation Site Classes for Ottawa, Quebec City, and the Metropolitan Area of Montreal
Cambrian–Lower Ordovician of SW Quebec–NE New York
ABSTRACT The Ottawa aulacogen/graben on the NE US—Canadian (SW Quebec and eastern Ontario) border is a long ENE-trending structure formed with initial late Neo proterozoic rifting of the Rodinia supercontinent. This rifting formed the active spreading arms (New York Promontory and Quebec Reentrant) along the (presently) NE margin of the new Laurentia paleocontinent, with the Ottawa aulacogen commonly regarded as a failed arm of the rifting. However, no sediment accumulation in the aulacogen is recorded until the late early Cambrian subsidence of a SE- trending belt that includes the aulacogen and its extension, the Franklin Basin, in NW Vermont. Late early Cambrian marine onlap (Altona Formation) followed by more rapid late middle Cambrian subsidence and deposition of fluviatile arkoses (Covey Hill Formation of SW Quebec and Ausable Formation/Member of eastern New York) record rapid foundering of this “failed arm.” Subsequent deposition (latest middle Cambrian–Early Ordovician) in the Ottawa aulacogen produced a vertical succession of lithofacies that are fully comparable with those of the shelf of the New York Promontory. One of the greatest challenges in summarizing the geological history of the Ottawa aulacogen is the presence of a duplicate stratigraphic nomenclature with lithostratigraphic names changing as state and provincial borders are crossed. RÉSUMÉ L’aulacogène/graben d’Ottawa, situé sur la frontière entre le NE des États-Unis et le Canada (SW du Québec et est de l’Ontario), est une longue structure d’orientation ENE formée au Néoprotérozoïque tardif durant le rifting initial du supercontinent Rodinia. Ce rifting a aussi mené à la formation de segments à expansion active (promontoire de New York et réentrant de Québec) le long de la marge NE (coordonnées actuelles) du nouveau paléo-continent Laurentia, avec l’aulacogène d’Ottawa qui est généralement considéré comme un segment de rift avorté. Toutefois, aucune accumulation de sediments n’est documentée au sein de l’aulacogène avant la fin du Cambrien précoce, période durant laquelle une ceinture d’orientation SE, representée par l’aulacogène et son prolongement dans le bassin de Franklin vers le NW du Vermont, a subi une subsidence. La sedimentation marine de la fin du Cambrien précoce (Formation d’Altona) a été suivie d’une subsidence rapide à la fin du Cambrien moyen et de la déposition d’arkoses fluviatiles (Formation de Covey Hill dans le SW du Québec et la Formation/Membre d’Ausable dans l’est de l’état de New York) qui ont enregistré un affaissement rapide de ce “bras avorté.” La sédimentation subséquente (Cambrien moyen tardif–Ordovicien inférieur) au sein de l’aulacogène d’Ottawa a produit une succession verticale de lithofaciès qui sont comparables à ceux de la plate-forme du promontoire de New York. Un des principaux défis dans la synthèse de l’histoire géologique de l’aulacogène d’Ottawa demeure la duplication des termes stratigraphiques de part et d’autre des frontières interprovinciales et entre les différents états.