The forge in the forest : being the narrative of the Acadian ranger, Jean de Mer, Seigneur de Briart, and how he crossed the Black Abbé, and of his adventures in a strange fellowship /

Mode of access: Internet.

Acadian ballads and De Soto's last dream,

Mode of access: Internet.

Acadian geology. The geological structure, organic remains, and mineral resources of Nova Scotia, New Brunswick, and Prince Edward Island.

"Geological bibliography of the Acadian provinces," p. 9-13.

A bioregional classification of the continental shelf of northeastern North America for conservation analysis and planning based on representation

Understanding how well National Marine Sanctuaries and other marine protected areas represent the diversity of species present within and among the biogeographic regions where they occur is essential for assessing their conservation value and identifying gaps in the protection of biological diversity. One of the first steps in any such assessment should be the development of clearly defined and scientifically justified planning boundaries representing distinct oceanographic conditions and faunal assemblages. Here, we propose a set of boundaries for the continental shelf of northeastern North America defined by subdivisions of the Eastern Temperate Province, based on a review and synthesis (i.e. meta-analysis) of the scientific literature. According to this review, the Eastern Temperate Province is generally divided into the Acadian and Virginian Subprovinces. Broad agreement places the Scotian Shelf, Gulf of Maine, and Bay of Fundy within the Acadian Subprovince. The proper association of Georges Bank is less clear; some investigators consider it part of the Acadian and others part of the Virginian. Disparate perspectives emerge from the analysis of different groups of organisms. Further, while some studies suggest a distinction between the Southern New England shelf and the rest of the Mid-Atlantic Bight, others describe the region as a broad transition zone with no unique characteristics of its own. We suggest there exists sufficient evidence to consider the Scotian Shelf, Gulf of Maine, Georges Bank, Southern New England, and Southern Mid-Atlantic Bight as distinct biogeographic regions from a conservation planning perspective, and present a set of proposed mapped boundaries. (PDF contains 23 pages.)

Geology of the Gander Group, Gander River Ultramafic Belt and Davidsville Group in the Jonathan's Pond - Weir's Pond Area, northeast Newfoundland /

The study area is situated in NE Newfoundland between Gander Lake and the north coast and on the boundary between the Gander and Botwood tectonostratigraphic zones (Williams et al., 1974). The area is underlain by three NE trending units; the Gander Group, the Gander River Ultramafic Belt (the GRUB) and the Davidsville Group. The easternmost Gander Group consists of a thick, psammitic unit composed predominantly of psammitic schist and a thinner, mixed unit of semipelitic and pelitic schist with minor psammite. The mixed unit may stratigraphically overlie the psammitic unit or be a lateral facies equivalent of the latter. No fossils have been recovered from the Gander Group. The GRUB is a terrain of mafic and ultramafic plutonic rocks with minor pillow lava and plagiogranite. It is interpreted to be a dismembered ophiolite in thrust contact with the Gander Group. The westernmost Davidsville Group consists of a basal conglomerate, believed deposited unconformably upon the GRUB from which it was derived, and an upper unit of greywacke and slate, mostly of turbidite origin, with minor limestone and calcareous sandstone. The limestone, which lies near the base of the unit, contains Upper Llanvirn to Lower Llandeilo fossils. The Gander and Davidsville Groups display distinctly different sedimentological , structural and metamorphic histories. The Gander Group consists of quartz-rich, relatively mature sediment. It has suffered three pre-Llanvirn deformations, of which the main deformation, Dp produced a major, NE-N-facing recumbent anticline in the southern part of the study area. Middle greenschist conditions existed from D^ to D- with growth of metamorphic minerals during each dynamic and static phase. In contrast, the mineralogically immature Davidsville Group sediment contains abundant mafic and ultramafic detritus which is absent from the Gander Group. The Davidsville Group displays the effects of a single penetrative deformation with localized D_ and D_ features, all of which can be shown to postdate D_ in the Gander Group. Rotation of the flat Gander S- into a subvertical orientation near the contact with the GRUB and the Davidsville Group is believed to be a Davidsville D^ feature. Regional metamorphism in the Davidsville Group is lower greenschist with a single growth phase, MS . These sedimentological, structural and metamorphic differences between the Gander and Davidsville Groups persist even where the GRUB is absent and the two units are in contact, indicating that the tectonic histories of the Gander and Davidsville Groups are distinctly different. Structural features in the GRUB, locally the result of multiple deformations, may be the result of Gander and/or Davidsville deformations. Metamorphism is in the greenschist facies. Geochemical analyses of the pillow lava suggest that these rocks were formed in a back-arc basin. Mafic intrusives in the Gander Group appear to be the result of magraatism separate from that producing the pillow lava. The Gander Group is interpreted to be a continental rise prism deposited on the eastern margin of the Late Precambrian-Lower Paleozoic lapetus Ocean. The GRUB, oceanic crust possibly formed in a marginal basin to the west, is believed to have been thrust eastward over the Gander Group, deforming the latter, during the pre-Llanvirnian, possibly Precambrian, Ganderian Orogeny. The Middle Ordovician and younger Davidsville Group was derived from, and deposited unconformably on, this deformed terrain. Deformation of the Davidsville Group occurred during the Middle Devonian Acadian Orogeny.

Structural, stratigraphic and geochemical studies of the Horwood Peninsula - Gander Bay Area, Northeast Newfoundland /

The Horwood Peninsula - Gander Bay area is located at NE Newfoundland in the Botwood Zone (Williams et a1., 1974) or in the Dunnage Zone (Williams, 1979) of the Central Mobile Belt of the Newfoundland Appalachians. The area is underlain by Middle Ordovician to possible Lower Silurian rocks of the Davidsville and Indian Islands Groups, respectively. Three conformable formations named informally : the Mafic Volcanic Formation, the Greywacke and Siltstone Formation and the Black Slate Formation, have been recognized in the Davidsville Group. The Greywacke and the Black Slate Formations pass locally into a Melange Formation. From consideration of regional structure and abundant locally-derived mafic volcanic olisto- 1iths in the melange, it is considered to have originated by gravity sliding rather than thrusting. Four formations have been recognized in the Indian Islands Group. They mainly contain silty slate and phyllite, grey cherty siltstone, green to red micaceous siltstone and limestone horizons. Repetition of lithological units by F1 folding are well-demonstrated in one of formations in this Group. The major structure in this Group on the Horwood Peninsula is interpreted to be a synclinal complex. The lithology of this Group is different from the Botwood Group to the west and is probably Late Ordovician and/or Early Silurian in age. The effects of soft-sediment deformation can be seen from the lower part of the Davidsville Group to the middle part of the Indian Islands Group indicating continuous and/or episodic slumping and sliding activities throughout the whole area. However, no siginificant depOSitional and tectonic break that could be assigned to the Taconian Orogeny has been recognized in this study. Three periods of tectonic deformation were produced by the Acadian Orogeny. Double boudinage in thin dikes indicates a southeast-northwest sub-horizontal compression and main northeast-southwest sub-horizontal extension during the D1 deformation. A penetrative, axial planar slaty cleavage (Sl) and tight to isocJ.ina1 F1 folds are products of this deformation. The D2 and D3 deformations formed S2 and S3 fabrics associated with crenulations and kink bands which are well-shown in the slates and phyllites of the Indian Islands Group. The D2 and D3 deformations are the products of vertical and northeast-southwest horizontal shortening respectively. The inferred fault between the Ordovician slates (Davidsville Group) and the siltstones (Indian Islands Group) suggested by Williams (1963, 1964b, 1972, 1978) is absent. Formations can be followed without displacement across this inferred fault. Chemically, the pillow lavas, mafic agglomerates, tuff beds and diabase dikes are subdivided into three rock suites : (a) basaltic komatiite (Beaver Cove Assemblage), (b) tholeiitic basalt (diabase dikes), (c) alkaline basalt (Shoal Bay Assemblage). The high Ti02 , MgO, Ni contents and bimodal characteristic of the basaltic komatiite in the area are comparable to the Svartenhuk Peninsula at Baffin Bay and are interpreted to be the result of an abortive volcano-tectonic rift-zone in a rear-arc basin. Modal and chemical analyses of greywackes and siltstones show the trend of maturity of these rocks increasing from poorly sorted Ordovician greywackes to fairly well-sorted Silurian siltstones. Rock fragments in greywackes indicate source areas consisting of plagiogranite, low grade metamorphic rocks and ultramafic rocks. Rare sedimentary structures in both Groups indicate a southeasterly provenance. Trace element analyses of greywackes also reveal a possible island-arc affinity.

Exclusion de liaison génétique au locus SPAX2 de cas canadiens-français d’ataxie spastique

Les ataxies héréditaires sont des désordres neuro-dégénératifs qui causent une ataxie comme symptôme primaire; soit une perte de coordination des mouvements volontaires, un sens de l’équilibre déficient et un trouble à la motricité. Elles forment un groupe cliniquement et génétiquement hétérogène. De ce fait, de nombreuses classifications existent basées sur différents critères. Cependant, le consensus actuel veut que le mode de transmission soit le critère premier de classement. On estime la prévalence mondiale des ataxies héréditaires à 6/100 000 bien que ce nombre diffère entre régions. C’est le cas du Québec où la structuration historique du bassin génétique canadien-français a menée à des effets fondateurs régionaux, ce qui a eu comme conséquence de hausser la prévalence régionale de certaines maladies. L’Acadie est également une région canadienne-française avec des effets fondateurs où le taux de prévalence de certaines ataxies héréditaires est plus élevé. Nous avons recruté huit familles canadiennes-françaises provenant de diverses régions du Québec, ayant un lien génétique plus ou moins rapproché avec l’Acadie, dans lesquelles nous avons observé dix cas d’une forme d’ataxie spastique autosomique récessive relativement légère qui a résistée à l’analyse des gènes d’ataxies connues. Nous avons émis l’hypothèse d’être en présence d’une nouvelle forme d’ataxie à effet fondateur pour la population canadienne-française. Afin d’identifier le gène muté responsable de cette ataxie, un criblage génomique des marqueurs SNP pour les individus recrutés fut effectué. Puis, par cartographie de l’homozygotie, une région de 2,5 Mb fut identifiée sur le chromosome 17p13 dans une famille. Une revue de la littérature nous a permis de constater, qu’en 2007, quatre familles nord-africaines atteintes d’une ataxie dénommée SPAX2 qui présentaient des manifestations cliniques semblables avaient déjà été liées au même locus sur le chromosome 17. Afin de supporter notre hypothèse que les malades étaient porteurs de deux copies de la même mutation fondatrice et de cartographier plus finement notre région d’intérêt, les haplotypes de tous les atteints de nos huit familles furent étudiés. Nous avons établie qu’un intervalle de 200 kb (70 SNP), soit du marqueur rs9900036 à rs7222052, était partagé par tous nos participants. Les deux gènes les plus prometteurs des 18 se trouvant dans la région furent séquencés. Aucune mutation ne fut trouvée dans les gènes SLC25A11 et KIF1C. Par la suite, une analyse de liaison génétique stricte avec calcul de LOD score nous a permis d’exclure ce locus de 200 kb comme étant celui porteur du gène muté causant l’ataxie dans la majorité de nos familles. Nous avons donc conclus que malgré qu’une famille soit homozygote pour une grande région du chromosome 17, l’absence d’Informativité des marqueurs SNP dans la région de 200 kb fut responsable de l’apparent partage d’haplotype homozygote. Le travail reste donc entier afin d’identifier les mutations géniques responsables de la présentation ataxique chez nos participants de souche acadienne.

Processus d’identification et stratégies identitaires des Acadiens du Nouveau-Brunswick

Les Acadiens du Nouveau-Brunswick ont un parcours identitaire collectif riche en rebondissements qui les a menés vers une identité singulière solide. Ils se trouvent désormais confrontés au contexte d’une nouvelle réalité qui est la mondialisation. Depuis les dernières décennies, les changements occasionnés par la mondialisation se répercutent dans la conception même que l’on se fait du parler acadien et des pratiques culturelles acadiennes. Le chiac par exemple, auparavant stigmatisé et dévalorisé, devient maintenant porteur de valeurs identitaires modernes rattachées au mélange des cultures et à l’ouverture à l’autre. Toutefois, les contours de l’identité acadienne demeurent flous et sujets aux débats épistémologiques. La situation particulière d’un groupe qui n’a plus de territoire officiellement reconnu a une forte incidence sur les critères d’appartenance que les acteurs peuvent mobiliser pour se définir. Comment expliquer les processus d’identifications et les stratégies identitaires qui définissent l’appartenance au groupe chez les Acadiens? Partagent-ils les mêmes processus identitaires présents dans la littérature sur le sujet? Une connaissance plus approfondie des processus généraux peut-elle aider à mieux saisir et expliquer la complexité d’un groupe sensiblement diasporique dont l’identité et ses contours sont incertains? L’anthropologie en milieu acadien est presque inexistante. D’autre part, l’identité culturelle est un sujet ayant été longuement étudié et débattu, mais qui demande toujours plus de précision. Cette recherche a permis de mieux cerner de quelle façon la représentation de l’acadianité évolue en milieu minoritaire.

Plutonism in three orogenic pulses, Eastern Blue Ridge Province, southern Appalachians

The Eastern Blue Ridge Province of the southern Appalachians contains, in part, remnants of an Ordovician accretionary wedge complex formed during subduction of an oceanic tract before mid-Ordovician accretion with Laurentia. The Eastern Blue Ridge Province consists of metapelite and amphibolite intruded by low-K plutons, high-temperature (T > 750 degrees C) Ordovician eclogite, and other high-pressure metamafic and meta-ultramatic rocks. Felsic plutons in the Eastern Blue Ridge Province are important time markers for regional-scale tectonics, deformation, and metamorphism. Plutons were thought to be related to either Taconian (Ordovician) or Acadian (Devonian-Silurian) tectonothermal events.We dated five plutonic or metaplutonic rocks to constrain pluton crystallization ages better and thus the timing of tectonism. The Persimmon Creek gneiss yielded a protolith crystallization age of 455.7 +/- 2.1 Ma, Chalk Mountain 377.7 +/- 2.5 Ma, Mt. Airy 334 +/- 3 Ma, Stone Mountain 335.6 +/- 1.0 Ma, and Rabun 335.1 +/- 2.8 Ma. The latter four plutons were thought to be part of the Acadian Spruce Pine Suite, but instead our new ages indicate that Alleghanian (Carboniferous-Permian) plutonism is widespread and voluminous in the Eastern Blue Ridge Province. The Chattahoochee fault, which was considered an Acadian structure, cuts the Rabun pluton and thus must have been active during the Alleghanian orogeny. The new ages indicate that Persimmon Creek crystallized less than 3 m.y. after zircon crystallization in Eastern Blue Ridge eclogite and is nearly synchronous with nearby high-grade metamorphism and migmatization. The three phases of plutonism in the Eastern Blue Ridge Province correspond with established metamorphic ages for each of the three major orogenic pulses along the western flank of the southern Appalachians.

Plutonismn in three orogenic pulses, Eastern Blue Ridge Province, southern Appalachians

The Eastern Blue Ridge Province of the southern Appalachians contains, in part, remnants of an Ordovician accretionary wedge complex formed during subduction of an oceanic tract before mid-Ordovician accretion with Laurentia. The Eastern Blue Ridge Province consists of metapelite and amphibolite intruded by low-K plutons, high-temperature (T >750 °C) Ordovician eclogite, and other high-pressure metamafic and meta-ultramafic rocks. Felsic plutons in the Eastern Blue Ridge Province are important time markers for regional-scale tectonics, deformation, and metamorphism. Plutons were thought to be related to either Taconian (Ordovician) or Acadian (Devonian-Silurian) tectonothermal events. We dated five plutonic or metaplutonic rocks to constrain pluton crystallization ages better and thus the timing of tectonism. The Persimmon Creek gneiss yielded a protolith crystallization age of 455.7 ± 2.1 Ma, Chalk Mountain 377.7 ± 2.5 Ma, Mt. Airy 334 ± 3Ma, Stone Mountain 335.6 ± 1.0 Ma, and Rabun 335.1 ± 2.8 Ma. The latter four plutons were thought to be part of the Acadian Spruce Pine Suite, but instead our new ages indicate that Alleghanian (Carboniferous-Permian) plutonism is widespread and voluminous in the Eastern Blue Ridge Province. The Chattahoochee fault, which was considered an Acadian structure, cuts the Rabun pluton and thus must have been active during the Alleghanian orogeny. The new ages indicate that Persimmon Creek crystallized less than 3 m.y. after zircon crystallization in Eastern Blue Ridge eclogite and is nearly synchronous with nearby high-grade metamorphism and migmatization. The three phases of plutonism in the Eastern Blue Ridge Province correspond with established metamorphic ages for each of the three major orogenic pulses along the western flank of the southern Appalachians. © 2006 Geological Society of America.

Réclamations à l'Assemblée-Nationale en faveur des anciens habitans de l'Acadie transportés en France lors de la prise de Louisbourg et particulierement en faveur de ceux débarqués à Cherbourg le 14 janvier 1760: Distribué au profit des acadiens 1790 : manuscript, 1790

Documents concern the landing of Acadian refugees at Cherbourg on 14 Jan. 1760.

(Table T1) Ages of white mica clasts in core samples of ODP Hole 210-1276A

Fifty-seven white mica clasts were separated from five samples taken from near the bases of turbidites ranging in age from early Albian to middle Eocene. Twenty two (39%) of the micas have ages between 260 and 340 Ma and five (9%) have older ages (~400-600 Ma). The former age range is characteristic of the North American Alleghenian orogeny and the Iberian Variscan orogeny. The latter range is characteristic of the North American Acadian orogeny and older basement rocks in the Grand Banks and Newfoundland areas. Both age ranges are present in the middle Eocene sample, but only the younger range occurs in the middle Albian sample. This difference could be a sampling artifact. If this is not the case, then the most likely explanation is that the Acadian-aged micas within the Meguma Zone underlying the Grand Banks were totally reset by Alleghenian reactivation of the zone, a feature which occurs extensively in Nova Scotia. The addition of Acadian-aged micas in the middle Eocene sample may reflect a change in sediment provenance as drainage systems unrelated to rift topography developed. With the exception of one clast dated at 186 Ma, the 12 other micas obtained from the upper Paleocene sample yielded ages between 55 and 74 Ma, with 7 falling within ±2 m.y. of the 57-Ma age of the sample indicated by the biostratigraphic age-depth plot for Site 1276. This, together with the volcaniclastic content of the sample, indicates an input from near-contemporaneous volcanism. The nearest known occurrences of near-contemporaneous late Paleocene volcanism that could have produced white micas are in Greenland and Portugal, some 2000 and 1500 km distant, respectively, from Site 1276 during the Paleocene. However, ages of volcanism in these areas indicate that they could probably not be sources of micas younger than 60 m.y., which suggests some as-yet unknown volcanic source in the North Atlantic area. Accumulation in the Grand Banks area of airborne-transported volcaniclastic material from eruptions of slightly different ages, followed by a single resedimentation event, could account for the spread of dates obtained from the sample. White micas from the lowermost Albian sample show a spread of ages between 37 and 284 Ma that is completely different from the age distribution pattern of the middle Albian and middle Eocene samples. The sample location is between, and at least 25 m above and below, two igneous sills dated at 98 and 105 Ma. The sills have narrow thermal aureoles and ages older than the youngest detrital micas in the sample. It is unlikely, therefore, that the spread of mica ages in the sample is due to partial resetting of ages caused by thermal effects associated with the intrusion of the sills. The resetting may have been associated with a longer lived thermal event.

De Pas pire à Pour sûr : faits et effets des langues chez France Daigle

La littérature de l’Acadie du Sud-Est émerge dans un contexte lui-même déjà hétérolingue (Grutman). Le chiac porte d’ailleurs les traces de cette cohabitation linguistique puisque son caractère hybride traduit la forte interaction entre les communautés de la région. Or, son usage suscite-t-il une réflexion inquiète sur la situation diglossique du français acadien ou est-il strictement créatif ? Le présent mémoire porte sur le rapport à la langue dans les romans récents de France Daigle, soit Pas pire (1998), Un fin passage (2001), Petites difficultés d’existence (2002) et Pour sûr (2011), en mettant au jour les particularités sociolinguistiques et la façon dont le texte « parle la langue » (Gauvin). Bien qu’il mette à distance les présupposés idéologiques, l’œuvre de Daigle demeure extrêmement sensible au contexte socioculturel d’où il émerge. Ainsi, si l’œuvre s’affranchit d’un réalisme sociolinguistique, c’est afin de créer une « fiction linguistique » (Baetens Beardsmore) qui reconfigure l’imaginaire social de Moncton tout en intégrant certaines inquiétudes bien « réelles ». Qui plus est, la prise en compte de la polyphonie structurelle de l’œuvre permet de s’affranchir de la lecture ethnographique. 

De Pas pire à Pour sûr : faits et effets des langues chez France Daigle

La littérature de l’Acadie du Sud-Est émerge dans un contexte lui-même déjà hétérolingue (Grutman). Le chiac porte d’ailleurs les traces de cette cohabitation linguistique puisque son caractère hybride traduit la forte interaction entre les communautés de la région. Or, son usage suscite-t-il une réflexion inquiète sur la situation diglossique du français acadien ou est-il strictement créatif ? Le présent mémoire porte sur le rapport à la langue dans les romans récents de France Daigle, soit Pas pire (1998), Un fin passage (2001), Petites difficultés d’existence (2002) et Pour sûr (2011), en mettant au jour les particularités sociolinguistiques et la façon dont le texte « parle la langue » (Gauvin). Bien qu’il mette à distance les présupposés idéologiques, l’œuvre de Daigle demeure extrêmement sensible au contexte socioculturel d’où il émerge. Ainsi, si l’œuvre s’affranchit d’un réalisme sociolinguistique, c’est afin de créer une « fiction linguistique » (Baetens Beardsmore) qui reconfigure l’imaginaire social de Moncton tout en intégrant certaines inquiétudes bien « réelles ». Qui plus est, la prise en compte de la polyphonie structurelle de l’œuvre permet de s’affranchir de la lecture ethnographique.