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Similar to many freshwater ecosystems, the Laurentian Great Lakes of North America have undergone numerous anthropogenic stressors resulting in considerable loss of biodiversity and habitat. Among Great Lakes fishes, the coregonine sub-family has endured the most extensive declines, including extinction of several species (Coregonus johannae, C. alpenae, and C. kiyi orientalis) and at least 10 instances of local extirpations of other species (C. nigripinnis, C. reighardi, C. zenithicus, C. hoyi, and C. artedi) across all 5 lakes, much of which occurred prior to the 1960s owing to overfishing, interactions with non-indigenous species, and habitat loss. Despite these declines, no federal-, provincial-, or state-mandated actions were ever implemented to conserve coregonine diversity, potentially because so much of the coregonine declines occurred prior to the enactment of federal conservation legislation. Possible explanations for inaction since enactment of that legislation include insufficient data on biological vulnerability or threats, unresolved taxonomy, and limited support from the fishery management agencies and their stakeholders prior to the 2000s. In recent decades, however, several fishery management agencies have undertaken efforts to re-introduce coregonine diversity. These efforts helped lead to development of a science-based framework to restore coregonines that was universally endorsed by fishery managers representing eight U.S. states, four U.S. tribal organizations, and the province of ON, Canada, in May 2018. The basin-wide framework is based on principles of conservation biology and adaptive management. We describe details of its key steps, including planning, restoring, and evaluating, while also describing recent implementation efforts to develop methods, improve available resources, and enhance coordination across the basin. Although our paper describes a regional effort to restore native coregonines, our adaptive-management approach could be used by other multi-agency stakeholders seeking to conserve or restore native fishes. [ABSTRACT FROM AUTHOR]

Three Orosirian basins and associated foreland thrust-fold belts are preserved on the margins of the Slave craton. All three are related to orogenic belts where oceans opened and later closed, uniting new crustal partners. The Great Slave basin differs from the Kilhigok and Coronation basins in ways that have defied explanation. It lacks a passive margin sequence and hosts two discrete igneous suites, separated by large-scale thrusting, that occurred well after the adjacent paleocean had closed. Here we report U–Pb zircon geochronology by chemical abrasion isotope dilution thermal ionization mass spectrometry for a member of each suite to constrain the age and origin of postcollisional thrusting. A widespread pulse of mainly phreatic alkaline volcanism, coeval with renewed foredeep flexure, occurred at 1889.0 ± 0.7 Ma (2σ internal error). A quartz-monzodiorite body, one of a belt-parallel chain of laccoliths that postdate thrusting, was emplaced at 1866.9 ± 0.9 Ma. These ages bracket renewed foredeep sedimentation and thrusting that telescoped major facies zones and was rooted within the basin. The older age is 70 and 30−60 Myr younger than collision in the Thelon and Taltson orogens, respectively. We attribute postcollisional thrusting and foredeep subsidence to "eduction"—the upward and outward ejection of partly subducted crust—and postulate that the top of the ejected wedge was a normal-sense detachment fault projecting beneath the Nonacho basin. We infer that eduction was triggered by slab failure, producing alkaline volcanism, and ended with delamination and laccolith emplacement. Eduction was facilitated by tradewind-driven erosion. Delamination was enabled by crustal transfer to the educted wedge, reducing footwall buoyancy. Slab failure and/or delamination removed the passive margin. [ABSTRACT FROM AUTHOR]

New bedrock mapping completed as part of the Nechako NATMAP Project indicates that the area between Babine and Takla lakes in central British Columbia is underlain by rocks of the Early Permian Asitka, Late Triassic Takla, and Early to Middle Jurassic Hazelton volcanic-arc assemblages of the Stikine Terrane. These are cut by large composite stocks of quartz diorite, granodiorite, and quartz monzonite previously mapped as the Late Triassic to Early Jurassic Topley intrusions. New U/Pb (n = 6) and laser [sup 40] Ar/[sup 39] Ar (n = 10) isotopic age dates reported in this paper suggest there are two distinct ages of plutons: the Topley intrusive suite with isotopic ages between 218 and 193 Ma; and, east of Babine Lake, the new Spike Peak intrusive suite with isotopic ages ranging from 179 to 166 Ma. West of the main plutonic belt is a thick volcanic succession of subaerial, porphyritic andesite flows, volcanic breccias, and rhyolitic ash-flow tuffs that have isotopic ages between 185 and 174 Ma. These rocks are assigned to the Saddle Hill Formation of the Hazelton Group. The plutonic roots of this proximal arc assemblage are most likely the coeval and compositionally similar plutons of the Spike Peak intrusive suite that have been unroofed in the area east of the Takla Fault. Major oxide and trace element data support the interpretation that the Topley and Spike Peak granitic rocks formed in a juvenile volcanic-arc environment and that magmatism is related to melts generated above a long-lived subduction zone of unknown orientation.Une nouvelle cartographie effectuée dans le cadre du projet NATMAP Nechako indique que la région entre les lacs Babine et Takla au centre de la Colombie-Britannique est recouverte de roches des assemblages d'arcs volcaniques du terrane de Stikine, soit Asitka du Permien précoce, Takla du Trias tardif et Hazelton du Jurassique précoce à moyen. Ces assemblages sont recoupés par des petits massifs intrusifs composites de diorite quartzique, de granodiorite et de monzonite quartzique qui avaient auparavant été cartographiés en tant que les intrusions Topley, du Trias tardif au Jurassique précoce. De nouvelles datations U-Pb (n = 6) et isotopes laser [sup 40] Ar/[sup 39] Ar (n = 10) présentées dans cet article suggèrent deux âges distincts de plutons, soit la suite intrusive de Topley avec des âges isotopiques entre 218 et 193 Ma et, à l'est du lac Babine, la nouvelle suite intrusive de Spike Peak dont les âges isotopiques varient de 179 à 166 Ma. À l'ouest de la ceinture plutonique principale se trouve une séquence volcanique épaisse d'écoulements subaériens d'andésite porphyrique, des brèches volcanique et des tufs d'écoulement de cendre rhyolitique dont les âges isotopiques varient entre 185 et 174 Ma. Ces roches sont assignées à la Formation de Saddle Hill du Groupe Hazelton. Les racines plutoniques de cet assemblage d'arc proximal sont fort probablement les plutons contemporains et à composition similaire de la suite intrusive de Spike Peak qui ont été décapés dans la région à l'est de la faille de Takla. Les données sur les principaux oxydes et les éléments traces corroborent l'interprétation que les roches granitiques de Topley et de Spike Peak se sont formées dans un environnement d'arc volcanique juvénile et que le magmatisme est relié aux fusions qui se sont produites au-dessus d'une ligne de subduction de longue durée mais dont l'orientation est inconnue.[Traduit par la Rédaction] [ABSTRACT FROM AUTHOR]

Over the past decade, plastic pollution has been documented throughout the Laurentian Great Lakes basin. Here, we demonstrate the application of a published ecological risk assessment and management framework for microplastics in aquatic environments by comparing proposed thresholds for risk to monitoring data from the Great Lakes region. Our results suggest that there may be measurable risks from microplastics to aquatic communities in parts of the Great Lakes where current concentrations are relatively high. For example, 89% of surface water samples collected across the region exceed the proposed risk thresholds for food dilution toxicity. However, all sediment samples remain below the proposed risk thresholds. Accordingly, we suggest that an appropriate and necessary next step for management may include convening a working group of local experts to develop an ecological risk assessment and management framework for the region comprising thresholds of concern for microplastics in surface water and sediment. Ultimately, microplastic pollution should be addressed in the Great Lakes Water Quality Agreement to ensure coordinated and sustained efforts are taken by the governments of Canada and the United States to reduce their release and impact. [ABSTRACT FROM AUTHOR]

Microplastics are a global contaminant of concern, but we have little information on the characteristics and bioavailability of these pollutants in western Canadian lakes. Here, we quantify and characterize microplastics in subsurface water and zooplankton from eight lakes in BC, Canada. By sampling water and zooplankton, we provide insight into the fraction of microplastics entering the food web. We found 0.607 ± 0.153 microplastics per litre in subsurface water, 0.01 ± 0.011 microplastics per copepod, and 0.02 ± 0.014 microplastics per Daphnia. Microplastic pollution was similar in all lakes sampled and showed no relationship with local population density. Fibers were the dominant morphology observed in all lakes, and Raman spectroscopy identified polyester as the dominant polymer found both in lakes and within zooplankton. Zooplankton generally ingested microplastics that were shorter than their body length and that fell on the smaller end of the range of available microplastics. The prominence of polyester fibers and PET films and fragments suggests that the likely sources of microplastics to these lakes are recreational activities and atmospheric deposition. [ABSTRACT FROM AUTHOR]

Copyright of Canadian Journal of Fisheries & Aquatic Sciences is the property of Canadian Science Publishing and its content may not be copied or emailed to multiple sites or posted to a listserv without the copyright holder's express written permission. However, users may print, download, or email articles for individual use. This abstract may be abridged. No warranty is given about the accuracy of the copy. Users should refer to the original published version of the material for the full abstract. (Copyright applies to all Abstracts.)

Copyright of Canadian Journal of Earth Sciences is the property of Canadian Science Publishing and its content may not be copied or emailed to multiple sites or posted to a listserv without the copyright holder's express written permission. However, users may print, download, or email articles for individual use. This abstract may be abridged. No warranty is given about the accuracy of the copy. Users should refer to the original published version of the material for the full abstract. (Copyright applies to all Abstracts.)

The Quaternary stratigraphy of the Nechako River – Cheslatta Lake area of central British Columbia is described and interpreted to reconstruct the late Quaternary history of the region. Exposures of glacial and nonglacial sediments deposited prior to the last glaciation (Fraser) are limited to three sites. Pollen assemblages from pre-Fraser nonglacial sediments at two of these sites reveal forested conditions around 39 000 BP. During the advance phase of the Fraser Glaciation, glacial lakes were ponded when trunk glaciers blocked some tributary valleys. Early in the glaciation, the drainage was free in easterly draining valleys. Subsequently, the easterly drainage was blocked either locally by sediments and ice or as a result of impoundment of the Fraser River and its tributaries east of the study area. Ice generally moved east and northeast from accumulation zones in the Coast Mountains. Ice flow was influenced by topography. Major late-glacial lakes developed in the Nechako River valley and the Knewstubb Lake region because potential drainage routes were blocked by ice.La stratigraphie du Quaternaire de la région de la rivière Nechako et du lac Cheslatta sise au centre de la Colombie Britannique est décrite et interprétée dans le but de reconstruire l'histoire du Quaternaire tardif de cette région. Seul trois coupes stratigraphiques mettent en évidence des sédiments glaciaires et non-glaciaires mis en place avant la dernière glaciation (Fraser). À deux sites, l'assemblage pollinique des sédiments non-glaciaires prédatant la Glaciation de Fraser reflète un environnement forestier aux environs de 39 000 BP. Lors de l'avancée des glaciers au début de la Glaciation de Fraser, des lacs glaciaires furent retenus dans les vallées secondaires par les glaciers qui occupaient les vallées primaires. Au début de cette glaciation, le drainage vers l'est fut tout d'abord ouvert mais subséquemment, il fut bloqué soit localement par des sédiments et de la glace ou en raison du blocage du fleuve Fraser et ses tributaires à l'est de la région d'étude. Les glaciers se sont écoulés vers l'est et le nord-est à partir de zones d'accumulation centrées sur la Chaîne Côtière. Les écoulements glaciaires furent influencés par la topographie. Des lacs post-glaciaires se sont formés dans la vallée de la rivière Nechako et dans la région du lac Knewstubb suite au blocage du drainage potentiel par la glace.[Traduit par la Rédaction] [ABSTRACT FROM AUTHOR]

Copyright of Canadian Geotechnical Journal is the property of Canadian Science Publishing and its content may not be copied or emailed to multiple sites or posted to a listserv without the copyright holder's express written permission. However, users may print, download, or email articles for individual use. This abstract may be abridged. No warranty is given about the accuracy of the copy. Users should refer to the original published version of the material for the full abstract. (Copyright applies to all Abstracts.)

Copyright of Canadian Journal of Fisheries & Aquatic Sciences is the property of Canadian Science Publishing and its content may not be copied or emailed to multiple sites or posted to a listserv without the copyright holder's express written permission. However, users may print, download, or email articles for individual use. This abstract may be abridged. No warranty is given about the accuracy of the copy. Users should refer to the original published version of the material for the full abstract. (Copyright applies to all Abstracts.)

In this article, the author discusses the landscape-scale patterns of the cyanobacterial toxin microcystin in Canadian lakes discovered by researchers through a regression tree model using the TREES module in the software SYSTAT 13. He mentions that the model helps to determine the relationship between microcystin concentrations, the concentration of total nitrogen (TN) to total phosphorus (TP) and the TN:TP ratio.

Copyright of Canadian Journal of Fisheries & Aquatic Sciences is the property of Canadian Science Publishing and its content may not be copied or emailed to multiple sites or posted to a listserv without the copyright holder's express written permission. However, users may print, download, or email articles for individual use. This abstract may be abridged. No warranty is given about the accuracy of the copy. Users should refer to the original published version of the material for the full abstract. (Copyright applies to all Abstracts.)

Copyright of Canadian Journal of Fisheries & Aquatic Sciences is the property of Canadian Science Publishing and its content may not be copied or emailed to multiple sites or posted to a listserv without the copyright holder's express written permission. However, users may print, download, or email articles for individual use. This abstract may be abridged. No warranty is given about the accuracy of the copy. Users should refer to the original published version of the material for the full abstract. (Copyright applies to all Abstracts.)

Copyright of Canadian Journal of Fisheries & Aquatic Sciences is the property of Canadian Science Publishing and its content may not be copied or emailed to multiple sites or posted to a listserv without the copyright holder's express written permission. However, users may print, download, or email articles for individual use. This abstract may be abridged. No warranty is given about the accuracy of the copy. Users should refer to the original published version of the material for the full abstract. (Copyright applies to all Abstracts.)

Copyright of Canadian Journal of Fisheries & Aquatic Sciences is the property of Canadian Science Publishing and its content may not be copied or emailed to multiple sites or posted to a listserv without the copyright holder's express written permission. However, users may print, download, or email articles for individual use. This abstract may be abridged. No warranty is given about the accuracy of the copy. Users should refer to the original published version of the material for the full abstract. (Copyright applies to all Abstracts.)

Copyright of Canadian Journal of Fisheries & Aquatic Sciences is the property of Canadian Science Publishing and its content may not be copied or emailed to multiple sites or posted to a listserv without the copyright holder's express written permission. However, users may print, download, or email articles for individual use. This abstract may be abridged. No warranty is given about the accuracy of the copy. Users should refer to the original published version of the material for the full abstract. (Copyright applies to all Abstracts.)

Copyright of Canadian Journal of Fisheries & Aquatic Sciences is the property of Canadian Science Publishing and its content may not be copied or emailed to multiple sites or posted to a listserv without the copyright holder's express written permission. However, users may print, download, or email articles for individual use. This abstract may be abridged. No warranty is given about the accuracy of the copy. Users should refer to the original published version of the material for the full abstract. (Copyright applies to all Abstracts.)

Copyright of Canadian Journal of Earth Sciences is the property of Canadian Science Publishing and its content may not be copied or emailed to multiple sites or posted to a listserv without the copyright holder's express written permission. However, users may print, download, or email articles for individual use. This abstract may be abridged. No warranty is given about the accuracy of the copy. Users should refer to the original published version of the material for the full abstract. (Copyright applies to all Abstracts.)

Copyright of Canadian Journal of Fisheries & Aquatic Sciences is the property of Canadian Science Publishing and its content may not be copied or emailed to multiple sites or posted to a listserv without the copyright holder's express written permission. However, users may print, download, or email articles for individual use. This abstract may be abridged. No warranty is given about the accuracy of the copy. Users should refer to the original published version of the material for the full abstract. (Copyright applies to all Abstracts.)

Copyright of Canadian Journal of Fisheries & Aquatic Sciences is the property of Canadian Science Publishing and its content may not be copied or emailed to multiple sites or posted to a listserv without the copyright holder's express written permission. However, users may print, download, or email articles for individual use. This abstract may be abridged. No warranty is given about the accuracy of the copy. Users should refer to the original published version of the material for the full abstract. (Copyright applies to all Abstracts.)

Copyright of Canadian Journal of Fisheries & Aquatic Sciences is the property of Canadian Science Publishing and its content may not be copied or emailed to multiple sites or posted to a listserv without the copyright holder's express written permission. However, users may print, download, or email articles for individual use. This abstract may be abridged. No warranty is given about the accuracy of the copy. Users should refer to the original published version of the material for the full abstract. (Copyright applies to all Abstracts.)

Copyright of Canadian Journal of Fisheries & Aquatic Sciences is the property of Canadian Science Publishing and its content may not be copied or emailed to multiple sites or posted to a listserv without the copyright holder's express written permission. However, users may print, download, or email articles for individual use. This abstract may be abridged. No warranty is given about the accuracy of the copy. Users should refer to the original published version of the material for the full abstract. (Copyright applies to all Abstracts.)

Copyright of Canadian Journal of Fisheries & Aquatic Sciences is the property of Canadian Science Publishing and its content may not be copied or emailed to multiple sites or posted to a listserv without the copyright holder's express written permission. However, users may print, download, or email articles for individual use. This abstract may be abridged. No warranty is given about the accuracy of the copy. Users should refer to the original published version of the material for the full abstract. (Copyright applies to all Abstracts.)

Copyright of Canadian Journal of Earth Sciences is the property of Canadian Science Publishing and its content may not be copied or emailed to multiple sites or posted to a listserv without the copyright holder's express written permission. However, users may print, download, or email articles for individual use. This abstract may be abridged. No warranty is given about the accuracy of the copy. Users should refer to the original published version of the material for the full abstract. (Copyright applies to all Abstracts.)

Copyright of Botany is the property of Canadian Science Publishing and its content may not be copied or emailed to multiple sites or posted to a listserv without the copyright holder's express written permission. However, users may print, download, or email articles for individual use. This abstract may be abridged. No warranty is given about the accuracy of the copy. Users should refer to the original published version of the material for the full abstract. (Copyright applies to all Abstracts.)

Copyright of Botany is the property of Canadian Science Publishing and its content may not be copied or emailed to multiple sites or posted to a listserv without the copyright holder's express written permission. However, users may print, download, or email articles for individual use. This abstract may be abridged. No warranty is given about the accuracy of the copy. Users should refer to the original published version of the material for the full abstract. (Copyright applies to all Abstracts.)

Copyright of Canadian Journal of Earth Sciences is the property of Canadian Science Publishing and its content may not be copied or emailed to multiple sites or posted to a listserv without the copyright holder's express written permission. However, users may print, download, or email articles for individual use. This abstract may be abridged. No warranty is given about the accuracy of the copy. Users should refer to the original published version of the material for the full abstract. (Copyright applies to all Abstracts.)

Copyright of Canadian Journal of Fisheries & Aquatic Sciences is the property of Canadian Science Publishing and its content may not be copied or emailed to multiple sites or posted to a listserv without the copyright holder's express written permission. However, users may print, download, or email articles for individual use. This abstract may be abridged. No warranty is given about the accuracy of the copy. Users should refer to the original published version of the material for the full abstract. (Copyright applies to all Abstracts.)

Copyright of Canadian Journal of Earth Sciences is the property of Canadian Science Publishing and its content may not be copied or emailed to multiple sites or posted to a listserv without the copyright holder's express written permission. However, users may print, download, or email articles for individual use. This abstract may be abridged. No warranty is given about the accuracy of the copy. Users should refer to the original published version of the material for the full abstract. (Copyright applies to all Abstracts.)

Copyright of Canadian Journal of Earth Sciences is the property of Canadian Science Publishing and its content may not be copied or emailed to multiple sites or posted to a listserv without the copyright holder's express written permission. However, users may print, download, or email articles for individual use. This abstract may be abridged. No warranty is given about the accuracy of the copy. Users should refer to the original published version of the material for the full abstract. (Copyright applies to all Abstracts.)

Copyright of Canadian Journal of Earth Sciences is the property of Canadian Science Publishing and its content may not be copied or emailed to multiple sites or posted to a listserv without the copyright holder's express written permission. However, users may print, download, or email articles for individual use. This abstract may be abridged. No warranty is given about the accuracy of the copy. Users should refer to the original published version of the material for the full abstract. (Copyright applies to all Abstracts.)

Copyright of Canadian Journal of Earth Sciences is the property of Canadian Science Publishing and its content may not be copied or emailed to multiple sites or posted to a listserv without the copyright holder's express written permission. However, users may print, download, or email articles for individual use. This abstract may be abridged. No warranty is given about the accuracy of the copy. Users should refer to the original published version of the material for the full abstract. (Copyright applies to all Abstracts.)

Copyright of Canadian Journal of Earth Sciences is the property of Canadian Science Publishing and its content may not be copied or emailed to multiple sites or posted to a listserv without the copyright holder's express written permission. However, users may print, download, or email articles for individual use. This abstract may be abridged. No warranty is given about the accuracy of the copy. Users should refer to the original published version of the material for the full abstract. (Copyright applies to all Abstracts.)

Copyright of Canadian Journal of Earth Sciences is the property of Canadian Science Publishing and its content may not be copied or emailed to multiple sites or posted to a listserv without the copyright holder's express written permission. However, users may print, download, or email articles for individual use. This abstract may be abridged. No warranty is given about the accuracy of the copy. Users should refer to the original published version of the material for the full abstract. (Copyright applies to all Abstracts.)

Focuses on changes in phytoplankton abundance, biodiversity and community structure in three small Precambrian Shield boreal forest lakes in northwestern Ontario for several years before and after experimental watershed and shoreline clearcut logging operations and associated forest regeneration practices. Possible effects of forest harvesting within drainage basins; Data analysis; Total phytoplankton biovolumes in the three lakes.

Lakes, of average size 33 ha, occupy a quarter of the surface area of Richards Island, Northwest Territories. Most of the lakes have a central pool deeper than the thickness of winter ice, and many have prominent, shallow, littoral terraces. The relatively warm lake bottoms cause considerable disturbance to the surrounding continuous permafrost. Water and lake-bottom temperatures, the configuration of permafrost, and active-layer thickness were measured at a tundra lake between 1992 and 1997. The lake is oval, 1.6 km long, 800 m wide, and as deep as 13 m. Sandy terraces, covered by less than 1 m of water, extend over 100 m from the shore. The terraces are underlain by permafrost, which terminates almost vertically at their edge. The annual mean temperature measured at lake bottom in the central pool ranged between 1.5°C and 4.8°C, depending on depth, and between –0.2°C and –5°C on the terraces, due to differences in snow cover and proximity to the central pool. In consequence, the temperature of permafrost at 7 m depth in the terraces also varied, from –2°C near shore to –5°C in mid-terrace. The active layer in the terraces was uniformly 1.4 m deep. Geothermal modelling of talik configuration indicates that there is no permafrost beneath the central pool of the lake. The modelling indicates that, under equilibrium conditions, about one quarter of the lakes on Richards Island have taliks that penetrate permafrost, and at least 10–15% of the island is underlain by talik. Short-term climatic changes predicted for the region imply a small increase in summer lake-water temperature and an extension of the open-water season, accompanied by thicker snow cover in winter. Following such changes, with longer freeze-up and warmer terrace temperatures in winter, permafrost may not be sustainable in the lake terraces.Le quart de la superficie de l'île Richards, dans les Territoires du Nord-Ouest, est occupé par des lacs, dont la superficie moyenne est de 33 ha. La plupart des lacs ont un bassin central plus profond que l'épaisseur de la glace en hiver et plusieurs ont des terrasses littorales, proéminentes et peu profondes. Le fond relativement chaud des lacs perturbe considérablement le pergélisol avoisinant. Les températures de l'eau et du fond du lac, la configuration du pergélisol et l'épaisseur de la couche active ont été mesurées dans un lac de toundra entre 1992 et 1997. Le lac est de forme ovale, il a une longueur de 1,6 km, une largeur de 800 m et sa profondeur atteint 13 m. Des terrasses de sable, recouvertes de moins d'un mètre d'eau s'étendent à plus de 100 m de la berge. Le pergélisol se retrouve sous les terrasses et il se termine presque verticalement au bord de ces terrasses. La température moyenne annuelle mesurée au fond du lac dans le bassin central varie entre 1,5 et 4,8 ºC et elle varie entre –0,2 et –5,0 ºC sur les terrasses; ces différences sont fonction du couvert de neige et de la proximité au bassin central. En conséquence, la température du pergélisol, à une profondeur de 7 m, varie également, de –2 près de la berge à –5 ºC au milieu de la terrasse. La couche active des terrasses a une profondeur uniforme de 1,4 m. Une modélisation géothermique de la configuration du talik indique qu'il n'y a pas de pergélisol sous le bassin central du lac. La modélisation indique aussi que, sous des conditions d'équilibre, environ le quart des lacs sur l'île Richards ont des taliks qui pénètrent le pergélisol et qu'il y a des taliks sous environ 10 à 15 % de l'île. Les changements climatiques à court terme prévus pour la région impliquent une faible augmentation de la température des eaux des lacs en été et une extension de la saison des eaux libres, accompagné d'un couvert de neige plus épais en hiver. Après de tels changements, accompagnés, en hiver, de périodes de gel plus longues et de températures plus chaudes pour les terrasses, il se pourrait que le pergélisol ne subsiste pas dans les terrasses des lacs.[Traduit par la Rédaction] [ABSTRACT FROM AUTHOR]

The Long Range Mountains of Newfoundland expose the northeastern most basement inlier of the Appalachian Orogen. U–Pb results for two samples of basement gneiss reveal crustal formation ages of 1466 ± 10 Ma (Western Brook Pond charnockite) and 1530 ± 8 Ma (Cat Arm Road gneiss), indicating an affinity with Pinwarian magmatism (1510–1450 Ma) in Labrador. A third sample of basement gneiss from the Cat Arm Road dam site yielded a minimum formation age of 1631 Ma. These basement gneisses were intruded by granite plutons during two periods of Grenvillian magmatism; Group I at 1032–1022 Ma and Group II at 993–985 Ma. Group I intrusions include the 1032.0 ± 1.5 Ma Lomond River granite and the 1022.0 ± 2.0 Ma Lake Michel igneous suite; Group II intrusions include the 999 ± 4 Ma Potato Hill charnockite, 993 ± 7 Ma Horse Chops granite, 984.9 ± 1.6 Ma Cloud River granite, and may include the Apsy granite. The metamorphic history of the Long Range Inlier is complex and three discrete Proterozoic metamorphic events can be delineated on the basis of field relationships and U–Pb dates for metamorphic minerals. M[sub 1] metamorphism is a regional high-grade event that occurred prior to 1032 Ma, the emplacement age for the unmetamorphosed Lomond River granite. M[sub 2] and M[sub 3] occurred at 1022 and 989 Ma, respectively; coinciding with the two main periods of Grenvillian magmatism. The Precambrian crustal evolution of the Long Range Inlier is very similar to the Pinware terrane of Labrador, consistent with a single contiguous terrane presently separated by the Gulf of St. Lawrence. A surprising discovery from this study is identification of the first known occurrence of Silurian mafic magmatism in the Long Range Inlier, the 430.5 ± 2.5 Ma Taylor Brook gabbro.L'enclave du socle le plus au nord-est de l'orogène des Appalaches affleure dans les montagnes du Long Range à Terre-Neuve. Des résultats U–Pb de deux échantillons de gneiss du socle révèlent des âges de formation crustale de 1466 ± 10 Ma (la charnokite de Western Brook Pond) et de 1530 ± 8 Ma (le gneiss de Cat Arm Road) indiquant une affinité avec le magnétisme pinwarien (1510–1450 Ma) au Labrador. Un troisième échantillon de gneiss du socle, au site du barrage de Cat Arm Road, a donné un âge minimum de 1631 Ma pour sa formation. Ces gneiss du socle ont été pénétrés par des plutons granitiques au cours de deux périodes de magmatisme grenvillien; le Groupe I à 1032–1022 Ma et le Groupe II à 993–985 Ma. Les intrusions du Groupe I comprennent le granite de Lomond River, 1032,0 ± 1,5 Ma et la suite ignée de Lake Michel 1022,0 ± 2,0; les intrusions du Groupe II comprennent la charnokite de Potato Hill, 999 ± 4 Ma, le granite de Horse Chops, 993 ± 7 Ma, le granite de Cloud River, 984,9 ± 1,6 Ma, et peut aussi comprendre le granite d'Apsy. L'histoire métamorphique de l'enclave de Long Range est complexe et il est possible de délimiter trois événements métamorphiques distincts au Protérozoïque selon les relations de terrain et les datations U–Pb des minéraux métamorphiques. Le métamorphisme M[sub 1] représente un événement régional de niveau élevé qui a eu lieu avant 1032 Ma, soit l'âge de la mise en place du granite non métamorphosé de Lomond River. M[sub 2] et M[sub 3] ont eu lieu respectivement à 1022 et 989 Ma, coïncidant avec les deux périodes principales de magmatisme grenvillien. L'évolution crustale au Précambrien de l'enclave de Long Range est très similaire à celle du terrane de Pinware au Labrador, concordant avec un terrane contigu unique présentement séparé par le golfe du Saint-Laurent. Une découverte surprenante de cette étude est l'identification de la première occurrence connue de magmatisme mafique silurien dans l'enclave de Long Range, soit le gabbro de Taylor Brook, à 430,5 ± 2,5 Ma.[Traduit par la Rédaction] [ABSTRACT FROM AUTHOR]

Studies the distribution of modern diatom assemblages in surficial sediments of Labrador lakes across broad vegetational biomass in Canada. Relationships between species and environment; Development of transfer functions for paleoenvironmental reconstruction; Six catchment vegetation types.

In August 1978, a large tundra lake was drained to study the aggradation of permafrost into newly exposed lake-bottom sediments. Ice-wedge growth, which started in the first winter following drainage, had ceased in most of the lake bottom within about twelve years. The gradual cessation of thermal contraction cracking can be attributed to rapid vegetation growth, snow entrapment, an increase in winter ground temperatures, and a decrease in the linear coefficient of thermal contraction associated with freeze–thaw consolidation of the initially saturated lake-bottom sediments. The tilt and separation of markers in the active layer revealed gradual convergence towards the troughs even after ice-wedge growth had ceased. For the first few years the ice-wedge growth rate was up to 3 cm/a as determined by excavation, drilling, separation of the bottoms of benchmarks installed into permafrost, and divergence of free-floating inductance coils placed on the sides of ice wedges well below the bottom of the active layer. The vertical extent of most ice wedges was probably about 2 m, as deduced from the depths of ice-wedge cracks and the geometries of the wedge tops. Many thermal contraction cracks propagated upward to the ground surface from the tops of the ice wedges rather than downward from the ground surface. Small, upward facing, horizontal steps and vertical slickensided surfaces in permafrost on both sides of an excavated ice wedge near its top indicated that the adjacent permafrost had moved upward, relative to the wedge, from thermal expansion during the warming period.En août 1978, un grand lac de toundra a été drainé afin d'étudier l'extension du pergélisol dans des sédiments de fond de lac nouvellement exposés. La croissance des coins de glace, qui a débuté le premier hiver suivant le drainage, avait cessé dans presque tout le fond du lac après une douzaine d'années. La cessation graduelle de la fissuration par contraction thermique peut être attribuée à la croissance rapide de la végétation, la retenue de la neige, une augmentation de la température du sol en hiver et une décroissance du coefficient linéaire de contraction thermique associée à la consolidation par le gel–dégel des sédiments de fond de lac, initialement saturés. Le basculement et la séparation des marqueurs dans la couche active révèlent une convergence graduelle vers les fosses même après l'arrêt de croissance des coins de glace. Pour les quelques premières années, le taux de croissance des coins de glace était de 3 cm/a tel que déterminé par excavation, forage, séparation des fonds des repères installés dans le pergélisol et la divergence des bobines d'induction flottantes placées sur les côtés des coins de glace bien en dessous du fond de la couche active. L'étendue verticale de la plupart des coins de glace était probablement d'environ 2 m, tel que déduit à partir des profondeurs des fentes de glace et de la géométrie du haut des coins. Plusieurs fissures de contraction thermique se sont propagées vers le haut à la surface du sol, à partir du sommet des coins de glace, plutôt que vers le bas, à partir de la surface du sol. De petites marches horizontales à face vers le haut et des surfaces verticales de friction dans le pergélisol des deux côtés d'un coin de glace excavé à proximité de son sommet indiquent que, par rapport au coin, le pergélisol adjacent s'était déplacé vers le haut en raison de l'expansion thermique durant la période de réchauffement.[Traduit par la Rédaction] [ABSTRACT FROM AUTHOR]

Stable isotope analysis of the potential prey and predator can be combined with gut content analysis to quantify the diet. This dietary knowledge allows the quantitative assessment of the role of key species in energy and contaminant transfer, their impact on prey communities, and their susceptibility to perturbation. The diet of Mysis relicta was examined in Lake Ontario in spring, summer, and autumn using both techniques. Mysids fed on the bottom during the day and in the pelagia and on the bottom at night. A trophic fractionation of 2.2‰ N between mysids and their prey provided the best correspondence between the observed stable isotope signature of mysids and that estimated from their diet. Tissue turnover rate of δ[sup 13] C was slow compared with that of δ[sup 15] N. Diatoms formed 50% of the assimilated diet in May. In September, 25% of large mysids feeding on the bottom contained amphipod parts and 20% contained phytoplankton. The remainder of the diet consisted of zooplankton and rotifers. The contribution of amphipods and phytoplankton could not be quantified. Revised daily consumption estimates, based on this new diet information and clearance rate estimates of consumption, gave daily consumption estimates similar to those estimated from previous bioenergetic modelling.L'analyse des isotopes stables chez les proies et les prédateurs potentiels combinée à l'examen des contenus du tube digestif permet de quantifier le régime alimentaire. Cette information rend possible l'évaluation quantitative du rôle des espèces-clés dans le transfert de l'énergie et des contaminants, de leur impact sur les communautés de proies et de leur vulnérabilité aux perturbations. Le régime alimentaire de Mysis relicta au lac Ontario au printemps, à l'été et en automne a été analysé à l'aide de ces deux techniques. Le jour, les Mysis se nourrissent sur le fond, mais la nuit ils s'alimentent à la fois dans les zones pélagique et profonde. Un fractionnement trophique de 2,2‰ de l'azote entre les Mysis et leurs proies donne la correspondance optimale entre la signature d'isotopes stables observée chez les Mysis et celle estimée à partir de leur régime alimentaire. Le taux de renouvellement tissulaire du δ[sup 13] C est faible par comparaison à celui du δ[sup 15] C. Les diatomées constituent 50% de la nourriture assimilée en mai. En septembre, 25% des Mysis de grande taille à alimentation benthique ont des restes d'amphipodes dans leur tube digestif et 20% ont du phytoplancton. Le reste du régime alimentaire est composé de zooplancton et de rotifères. L'apport des amphipodes et du phytoplancton n'a pu être quantifié. Les taux révisés de consommation journalière, basés sur ces informations nouvelles et sur des estimations du taux de clearance de la consommation, donnent des estimations de consommation journalière semblables à celles obtenues à l'aide des modèles bioénergétiques antérieurs.[Traduit par la Rédaction] [ABSTRACT FROM AUTHOR]

Thousands of lakes in northeastern Ontario, Canada, have been acidified by sulphur deposition associated with emissions from the Sudbury area metal smelters. However, water quality improvements including increased pH and reduced sulphate concentrations have followed large reductions in Sudbury emissions that were implemented, beginning in the 1970s. Substantial decreases in Ca concentrations accompanied these other changes in lakewater chemistry. Monitoring of 38 lakes 20–128 km from Sudbury showed declines in Ca concentrations, averaging 2.7 µeq·L[sup –1] ·year[sup –1] , over the period 1981–1999. Declines were particularly apparent during the 1990s, averaging 3.8 µeq·L[sup –1] ·year[sup –1] . Paleolimnological reconstructions of the long-term Ca patterns in six lakes suggest that general lakewater Ca declines occurred through much of the 20th century. Comparison of recent measured Ca concentrations in 16 lakes with diatom-inferred pre-industrial Ca concentrations indicates that overall decreases in Ca have been large, averaging 74.6 µeq·L[sup –1] or 46%. Long-term Ca patterns may reflect a combination of factors including climatic changes, forest harvesting activities, and leaching by acid deposition, the effects of which we can not separate. Calcium declines have biological implications that will need to be considered in the development of appropriate targets as these lakes continue to recover from acidification.Des milliers de lacs du nord-est de l'Ontario, Canada, ont été acidifiés par les dépôts de soufre provenant des émissions des fonderies de la région de Sudbury. Cependant, les réductions importantes des émissions depuis les années 1970 ont entraîné une amélioration de la qualité de l'eau et, en particulier, un accroissement du pH et une diminution des concentrations de sulfates. Des réductions importantes des concentrations de Ca ont accompagné ces changements dans la chimie des eaux des lacs. Le suivi de 28 lacs situés à des distances de 20 à 128 km de Sudbury indique des déclins dans les concentrations de Ca d'en moyenne 2,7 µeq·L[sup –1] ·année[sup –1] de 1981 à 1999, particulièrement durant les années 1990 où les taux étaient en moyenne de 3,8 µeq·L[sup –1] ·année[sup –1] . Des reconstitutions paléolimnologiques de l'évolution à long terme du Ca dans six des lacs laissent croire que le déclin général du Ca dans l'eau des lacs s'est poursuivi pendant presque tout le vingtième siècle. Une comparaison des concentrations récentes de Ca dans 16 lacs avec les concentrations estimées d'après les peuplements de diatomées avant l'ère industrielle montre que le déclin de Ca a été important, en moyenne de l'ordre de 74,6 µeq·L[sup –1] ou de 46%. Cette évolution à long terme du Ca peut être le reflet d'une combinaison de facteurs, dont les effets ne peuvent être séparés, en particulier les changements climatiques, les activités de coupe des forêts et le lessivage dû aux précipitations acides. Les déclins du Ca ont des implications biologiques qu'il sera nécessaire de considérer dans la définition d'objectifs appropriés, à mesure que ces lacs se rétablissent de l'acidification.[Traduit par la Rédaction] [ABSTRACT FROM AUTHOR]

Three classic sections of Middle and Late Triassic fossiliferous limestones cropping out around Williston Lake in British Columbia, Canada, were sampled for paleomagnetic study. The objective was to test the suitability of these units for detailed magnetobiostratigraphic study with the aim of improving the reference Triassic geomagnetic polarity time scale. The Williston Lake characteristic magnetizations differ, however, from any Triassic North America cratonic reference directions. A satisfactory agreement is found instead with Cretaceous – early Cenozoic North America cratonic reference directions. The exclusive occurrence of normal polarity suggests that remagnetization likely occurred during the Cretaceous long normal superchron. Remagnetizations may have been triggered by connate brines, which moved along aquifers of porous sandstones and carbonates in the early stages of Laramide folding.Trois sections fossilifères classiques de calcaires (Trias moyen et tardif), affleurant autour du lac Williston en Colombie Britannique, ont été échantillonnées pour une étude paléomagnétique. L'objectif était de s'assurer de la pertinence de ces unités pour une étude magnéto-bio-stratigraphique détaillée visant à améliorer l'échelle référentielle de temps de la polarité géomagnétique au Trias. Les magnétisations caractéristiques du lac Williston diffèrent toutefois de toute direction cratonique référentielle au Trias en Amérique du Nord. Toutefois, une corrélation satisfaisante est établie avec les directions cratoniques référentielles du Crétacé–Cénozoïque précoce en Amérique du Nord. L'occurrence exclusive d'une polarité normale suggère qu'il y eut probablement une remagnétisation au cours du long superchron normal du Crétacé. Les remagnétisations peuvent avoir été déclenchées par des saumures connées qui se sont déplacées le long d'aquifères de grès et de carbonates poreux dans les premières phases du plissement Laramide.[Traduit par la Rédaction] [ABSTRACT FROM AUTHOR]

New mapping, mineralogical, and geochemical studies help characterize late Tertiary primitive, alkaline, sodic basanite, alkali olivine basalt, transitional basalt, and diabase in the Nechako River, Whitesail Lake, and McLeod Lake map areas of central British Columbia and distinguish the Miocene Cheslatta Lake suite. The suite encompasses scattered erosional remnants of topographically distinct, columnar-jointed, olivine-phyric basalt and diabase volcanic necks, dykes, and associated lava flows north of the Anahim volcanic belt and west of the Pinchi Fault. Volcanic centres at Alasla Mountain and at Cutoff Creek, near Cheslatta Lake, are proposed as type areas. Olivine, plagioclase, and pyroxene phenocrysts, megacrysts, and (or) xenocrysts; common ultramafic xenoliths; and rare but significant plutonic and metamorphic xenoliths are characteristic. Basanite, transitional basalt, and alkali olivine basalt groundmass contain plagioclase, clinopyroxene, Fe-Ti oxides, feldspathoid, olivine, and apatite. The Cheslatta Lake suite is characterized by its alkaline character, olivine-rich (>10 wt.%) normative mineralogy, and silica-undersaturated nature (>1 wt.% normative nepheline; hypersthene-normative rocks are uncommon). Mg numbers vary between 72–42. Some samples encompass near-primitive mantle melt compositions. Cheslatta Lake suite rocks in the Nechako River area are distinguished from the underlying Eocene Endako and stratigraphically higher Neogene Chilcotin groups basaltic andesite lavas within the study area, and from the Chilcotin Group basalt in the type area south of the Anahim volcanic belt, by form, preserved thickness, phenocryst–xenocryst mineralogy, amygdule abundance, included xenoliths, isotopic age, and major and incompatible, high field strength, and rare-earth trace element contents.Une nouvelle cartographie et de nouvelles études minéralogiques et géochimiques aident à caractériser la basanite sodique, alcaline et primitive du Tertiaire tardif, le basalte alcalin à olivine, le basalte de transition et la diabase dans les régions cartographiques de la rivière Nechako et des lacs Whitesail et McLeod du centre de la Colombie-Britannique et aident à distinguer la suite de Cheslatta Lake, datant du Miocène. La suite comprend des lambeaux épars de l'érosion de roches topographiquement distinctes et à structure prismée; ces roches comprennent des basaltes à olivine porphyrique, des « necks » de diabase volcanique, des dykes et des coulées de lave associées, au nord de la ceinture volcanique Anahim et à l'ouest de la faille Pinchi. Nous proposons les centres volcaniques du mont Alasla et du ruisseau Cutoff, près du lac Cheslatta, comme régions types. Les roches suivantes sont caractéristiques des phénocristaux, des mégacristaux et (ou) des xénocristaux d'olivine, de plagioclase et de pyroxène; des xénolites ultramafiques communs et de rares mais significatifs xénolites plutoniques et métamorphiques. La matrice rocheuse de basanite, de basalte de transition et de basalte alcalin à olivine comprend du plagioclase, du clinopyroxène, des oxydes de Fe–Ti, des feldspathoïdes, de l'olivine et de l'apatite. La suite de Cheslatta Lake est caractérisée par son caractère alcalin, sa minéralogie normative riche en olivine (>10 % en poids) et sa sous-saturation en silice (les roches à > 1 % en poids de néphéline normative, hypersthène normatif sont peu communes). Les nombres pour le Mg varient entre 72 et 42. Quelques échantillons présentent des compositions du manteau quasi-primitif en fusion. Dans la région de la rivière Nechako, les roches de la suite de Cheslatta Lake se distinguent des roches sous-jacentes Endako, datant de l'Éocène, et des laves basaltiques à andésite des groupes Chilcotin, datant du Néogène, stratigraphiquement plus hautes ainsi que du basalte du Groupe Chilcotin dans la région type au sud de la ceinture volcanique Anahim par les points suivants la forme, la conservation de l'épaisseur, la minéralogie des phénocristaux–xénocristaux, l'abondance d'éléments amygdaloïdes, les xénolites inclus, l'âge isotopique ainsi que, significatif et incompatible, une grande intensité du champ et des contenus trace en éléments des terres rares.[Traduit par la Rédaction] [ABSTRACT FROM AUTHOR]

Erosion along the Nechako Reservoir and Cheslatta River Spillway has resulted in unusually well-exposed late Quaternary and Holocene stratigraphy. Surficial sediments in the study area are mostly products of Late Wisconsinan glaciation. However, evidence for pre-Late Wisconsinan sedimentation has been found along the shores of the Nechako Reservoir, including till of an older glaciation and organic-bearing, blue-grey, lacustrine sediments of probable Middle Wisconsinan age. Stratigraphic correlation of the lake sediments suggests that an extensive lake system occurred in the region during the Olympia Nonglacial Interval. Late Wisconsinan ice initially moved along major valleys, with glaciofluvial outwash deposited in front of the advancing ice. Advance-phase glaciolacustrine sediments are rare but significant, as slope failures are spatially associated with areas where they are preserved. The distribution of these sediments and associated deltaic deposits indicates that advance-phase glacial lakes occurred up to approximately 855 m asl, at least several metres above the modern reservoir level. Sediments deposited in front of the ice margin were overridden during ice advance and are best preserved in large valleys. At the glacial maximum, ice flowed northeasterly throughout the study region. Crag and tails, flutings, and drumlinoid ridges with a generally consistent northeast trend are the dominant landforms. Till is the most common Pleistocene surficial sediment, covering approximately 80% of the area; large areas of exposed bedrock are rare. Late-glacial glaciofluvial and Holocene fluvial deposits are uncommon and occur mainly along the Cheslatta River valley. De l'érosion le long du réservoir Nechako et du déversoir de la rivière Cheslatta a produit de très beaux affleurements de la stratigraphie du Quaternaire tardif et de l'Holocène. Les sédiments de surface dans la région à l'étude sont surtout des produits de la glaciation du Wisconsinien tardif. Toutefois, des preuves de sédimentation au pré-Wisconsinien tardif ont été retrouvées le long des berges du réservoir Nechako; elles comprennent un till d'une glaciation plus ancienne et des sédiments lacustres gris-bleu contenant de la matière organique, datant probablement du Wisconsinien moyen. La corrélation stratigraphique des sédiments lacustres suggère qu'un système extensif de lacs était en place dans la région durant l'intervalle non glaciaire Olympia. La glace du Wisconsinien tardif a tout d'abord avancé le long des vallées majeures alors que du matériel stratifié fluvio-glaciaire était déposé en avant de la glace qui avançait. Des sédiments glacio-lacustres de phase avancée sont rares mais importants car les ruptures de pentes sont associées aux régions où ils sont préservés. La distribution de ces sédiments et des dépôts deltaïques associés indique que des lacs glaciaires de phase avancée se sont retrouvés à environ 855 m au-dessus du niveau de la mer, au moins plusieurs mètres au-dessus du niveau moderne du réservoir. Lors d'une avancée glaciaire, la glace passe par-dessus les sédiments déposés en avant du front glaciaire et ils sont ainsi mieux conservés dans les grandes vallées. Au maximum glaciaire, la glace coulait vers le nord-est dans toute la région à l'étude. Les formes de terrain dominantes, à direction généralement nord-est, sont les « crag and tail », les rainures glaciaires et les drumlinoïdes. Le till est le sédiment de surface le plus commun du Pléistocène, couvrant environ 80 % de la région; les grandes aires d'affleurements rocheux sont rares. Les dépôts fluvio-glaciaires tardi-glaciaires et les dépôts fluviaux de l'Holocène sont peu communs et se retrouvent surtout le long de la vallée de la rivière Cheslatta.[Traduit par la Rédaction] [ABSTRACT FROM AUTHOR]