Precise age and petrology of Silurian-Devonian plutons in the Benjamin River--Charlo area, northern New Brunswick.
The Late Silurian Landry Brook and Dickie Brook plutons and Charlo plutonic suite underlie a combined area of approximately 80 [km.sup.2] in the northeastern part of the Ganderian Tobique-Chaleur tectonostratigraphic belt in northern New Brunswick. The Landry Brook pluton is divided into three units: gabbro to quartz diorite, quartz monzodiorite to monzogranite, and monzogranite. A sample from the quartz monzodiorite unit yielded a U-Pb (zircon) crystallization age of 419.63 [+ or -] 0.23 Ma. A granodioritic stock located near the Landry Brook pluton has yielded an age of 400.7 [+ or -] 0.4 Ma, indicating that it is a younger unrelated body, herein referred to as the Blue Mountain Granodiorite (new name). The Dickie Brook pluton also consists of three units: leucogabbro to quartz gabbro, diorite to quartz diorite and quartz monzodiorite to monzogranite. Two samples from the monzogranite unit yielded U-Pb (zircon) crystallization ages of 418 [+ or -] 1 Ma and 418.1 [+ or -] 1.3 Ma. The Charlo plutonic suite is a group of small plutons and dykes, located west of the Dickie Brook and Landry Brook plutons and consists mainly of diabase, quartz monzonite to monzogranite, rhyolite porphyry, and dacite porphyry. Chemical trends indicate that the quartz monzodiorite to monzogranite unit of the Landry Brook pluton, all of the units of the Dickie Brook pluton, and the quartz monzodiorite to monzogranite unit of the Charlo plutonic suite, as well as the volcanic host rocks of the Bryant Point and Benjamin formations, are co-magmatic They formed following slab break-off and extension in the waning stages of the Salinic orogeny, which resulted from the collision of Ganderia and Laurentia. In contrast, the dacite porphyry of the Charlo plutonic suite may be cogenetic with the younger Blue Mountain Granodiorite and related to the collision of Avalonia with Laurentia.
Les plutons des ruisseaux Landry et Dickie et le corrige plutonique de Charlo, du Silurien tardif, recouvrent une superficie totale d'environ 80 [km.sup.2] dans la partie nord-est du domaine tectonostratigraphique ganderien Tobique-Chaleur, dans le nord du Nouveau-Brunswick. Le pluton du ruisseau Landry se compose de trois unites : du gabbro a de la diorite quartzique, de la monzodiorite quartzique au monzogranite, et du monzogranite. Un echantillon de l'unite de monzodiorite quartzique a produit un age de cristallisation de 419,63 [+ or -] 0,23 Ma par la methode de datation U-Pb (sur zircon). Un bloc de granodiorite a proximite du pluton du ruisseau Landry a produit un age de 400,7 [+ or -] 0,4 Ma, ce qui indiquerait qu'il s'agit d'un corps de formation plus recente et non relie, designe ici comme la granodiorite de Blue Mountain (nouveau nom). Le pluton du ruisseau Dickie comprend lui aussi trois unites : du leucogabbro a du gabbro quartzique, de la diorite a de la diorite quartzique, et de la monzodiorite quartzique a du monzogranite. Deux echantillons de monzogranite ont produit des ages de cristallisation de 418 [+ or -] 1 Ma et de 418,1 [+ or -] 1,3 Ma, selon la methode de datation U-Pb (sur zircon). Le cortege plutonique de Charlo est un groupe de plutons et de dykes de petite taille, situe a l'ouest des plutons du ruisseau Dickie et du ruisseau Landry, et il se compose de diabase, de monzonite quartzique a du monzogranite, de porphyre rhyolitique, et de porphyre dacitique. Les tendances chimiques indiquent une nature comagmatique en ce qui concerne l'unite de monzodiorite quartzique au monzogranite du pluton du ruisseau Landry, la totalite des unites du pluton du ruisseau Dickie, ainsi que l'unite monzodiorite quartzique au monzogranite du corthge plutonique de Charlo, tout comme pour les roches volcaniques encaissantes des Formations Bryant Point et Benjamin. Ces structures sont apparues apres la rupture de la plaque et son extension aux derniers stades de l'orogenese salinique, provoquee par la collision des anciens continents de Ganderie et de Laurentie. Par contraste, le porphyre dacitique du corthge plutonique de Charlo peut s'&re forme sous les m4mes conditions que celles ayant preside h l'apparition de la granodiorite plus recente de Blue Mountain et etre associe a la collision des anciens continents d'Avalon et de Laurentie.
[Traduit par la redaction]
Central and northern New Brunswick contains voluminous Silurian-Devonian plutonic and volcanic rocks displaying a continuous spectrum from mafic to felsic compositions (e.g., Whalen 1993; Wilson et al. 2008). The focus of this study, the Landry Brook and Dickie Brook plutons anda group of smaller plutons, dykes, and sills referred to here as the Charlo plutonic suite, are part of this widespread mid-Paleozoic magmatism, but are spatially isolated from other plutonic manifestations of the magmatic event. These plutonic rocks range in composition from gabbro to monzogranite and, collectively, cover an area of approximately 80 [km.sup.2] (Fig. 1). Although generally assumed to be consanguineous and Devonian, the ages of these plutons were in fact uncertain prior to the present study. Stewart (1979) reported an imprecise age of 370 [+ or -] 30 Ma (whole-rock Rb-Sr) for the Landry Brook pluton, and later an unpublished U-Pb (zircon) age of 400 [+ or -] 1 Ma was obtained (V. McNicoll; reported in Wilson et al. 2004) from a separate granodiorite stock southwest of the Landry Brook pluton; however, its relationship to that pluton was uncertain. Data from this latter stock are included in this study, and geochemical comparisons are made with adjacent intrusive rocks. The Landry Brook and Dickie Brook plutons and Charlo plutonic suite are excellent targets for petrological and geochronological study, to add new information to models for northern Appalachian magmatic and tectonic evolution.
The purpose of this paper is to describe the field relationships and petrology of these plutons, to present new and older (but previously unpublished) U-Pb (zircon) data that closely constrain the age of the Landry Brook and Dickie Brook plutons and spatially associated stocks, and to interpret their petrogenesis and tectonic setting at the time of emplacement. Based on geochemical and age similarities, we further suggest that the host volcanic rocks of the Benjamin and Bryant Point formations are likely genetically related to (i.e., the extrusive equivalents of) the plutons.
The Landry Brook pluton, Dickie Brook pluton, and Charlo plutonic suite intruded rocks that are part of the mid-Paleozoic Appalachian realm of Ganderia and its cover sequence (Fig. 2). At regional scale, Ordovician rocks in this area are part of the Popelogan-Victoria arc subzone (Hibbard et al. 2006; van Staal 2007; van Staal et al. 2009) and are covered by the Silurian-Devonian Chaleur Bay Synclinorium (part of the Gaspe Belt; Wilson et al. 2004), which includes rocks of the Quinn Point, Dickie Cove, Petit Rocher, and Dalhousie groups (Wilson and Kamo 2012). The Silurian rocks in the study area include the Upsalquitch Formation (Quinn Point Group), and the Bryant Point, New Mills, and Benjamin formations (Dickie Cove Group; Fig. 1).
The Llandoverian Upsalquitch Formation (Fig. 1) is generally composed of calcareous, micaceous siltstone and fine-grained sandstone (McCutcheon and Bevier 1990). It is disconformably overlain by the Ludlovian Bryant Point Formation, which is composed of greyish-green to maroon, locally highly porphyritic and amygdaloidal basaltic flows with plagioclase phenocrysts up to 3 cm in length. It is estimated to be about 650 m thick at the type locality (Walker and McCutcheon 1995). The New Mills Formation overlies the Bryant Point Formation, and is composed of red pebble-cobble conglomerate, sandstone and siltstone, and minor mafic and felsic volcanic flows. Cobbles and pebbles in the conglomerate are composed of mafic and felsic volcanic rocks, derived from underlying and coeval formations. The large size of many of the boulders, their lack of orientation, and poor stratification suggest deposition as subaerial debris flows (Greiner 1970; Irrinki 1990; Walker et al. 1993; Walker and McCutcheon 1995). The formation is approximately 120 m thick, and is overlain by and interfingers with felsic volcanic rocks of the Benjamin Formation. The latter formation is composed of pale red, flow-banded, sparsely porphyritic rhyolite, and also includes feldspar crystal tuff, pumaceous lapilli tuff and, at the top of the formation, basalt (McCutcheon and Bevier 1990). The Benjamin Formation is late Ludfordian to early Pridolian in age, and yielded U-Pb (zircon) ages of 420.8 [+ or -] 0.4 Ma (Wilson and Kamo 2008) and 419.7 [+ or -] 7 Ma (Wilson and Kamo 2012) at different localities. The former dated sample was collected 3.5 km north of the northern tip of the Dickie Brook pluton (Fig. 1), and the latter 14 km south of the southern part of the Landry Brook pluton (not shown on Fig. 1).
FIELD RELATIONS AND PETROGRAPHY
The Landry Brook pluton was previously termed the "Benjamin River intrusive complex" by Stewart (1979), and the Landry Brook, Dickie Brook and Charlo intrusions were later collectively referred to as the "Charlo stocks" (Fyffe et al. 1981). Whalen (1993) considered the Landry Brook and Dickie Brook plutons as two separate plutons forming the "Benjamin River complex". However, to avoid any terminology conflict with some of the host rocks (i.e., the Benjamin Formation), the names Landry Brook and Dickie Brook were introduced; both names derive from brooks that are tributaries of the Benjamin River, which transects both plutons. The formal names of these plutons in the New Brunswick bedrock lexicon are the Landry Brook Quartz Monzonite and Dickie Brook Quartz Monzonite; however, to avoid exclusivity in the various rock types forming them, they are referred herein simply as plutons. The term Charlo plutonic suite is used here only for small plutons, dykes, and sills that occur over a large area west of the Landry Brook and Dickie Brook plutons (Fig. 1). These small bodies were referred to as the "Charlo stocks" by Whalen (1993); the formal name in the New Brunswick bedrock lexicon is the Charlo Granite. As discussed later in the text, the name Blue Mountain Granodiorite is introduced for two granodioritic stocks south and southwest of the Landry Brook pluton. The name is derived from Blue Mountain, a topographic feature in the area (Fig. 1). However, gabbroic bodies in the same area are interpreted to be part of the Landry Brook pluton, based on petrological features described below.
Landry Brook pluton and Blue Mountain Granodiorite
The Landry Brook pluton consists of one main composite intrusion and a few small gabbroic bodies located southwest of the main intrusion (Fig. 1). The latter area is also the location of the Blue Mountain Granodiorite stocks, which were originally considered to be genetically related to the Landry Brook pluton, but are discussed separately here.
The most abundant rock type in the Landry Brook pluton is quartz monzodiorite to monzogranite, which makes up most of the pluton. Other lithotypes include gabbro/quartz diorite and late monzogranite. Throughout the area, exposure is poor; hence, cross-cutting and other contact relations are difficult to observe. In addition to field observations, 16 drill holes were re-logged in order to reassess the relationships with the smaller plutons to the southwest of the main body. Based on these observations and prior to geochronological work, the sequence of emplacement was inferred to be gabbro/quartz diorite, followed by medium-grained granodiorite, porphyritic granodiorite and quartz monzodiorite to monzogranite (QMM), and lastly the monzogranite. All these plutonic rocks intruded mafic flows and felsic flows and pyroclastic rocks of the Bryant Point and Benjamin formations, respectively. The gabbro to diorite (of leucogabbro) occurs also as xenoliths in the QMM (Figs. 3a, b); the xenoliths are angular to irregular (e.g., ovoid) in shape and range widely in size (cm to m scale). Contacts between the gabbro and the QMM are gradational to sharp and the late monzogranite clearly cross-cuts both the QMM and gabbro (Fig. 3b), as xenoliths are present in a monzogranite dyke in the northeastern part of the pluton.
Porphyritic granodiorite (Fig. 3c) and medium-grained granodiorite (Fig. 3d) of the Blue Mountain Granodiorite have clear intrusive relationships relative to both the early gabbro and the late monzogranite of the Landry Brook pluton. In both cases contacts are sharp and well define& chilled margins and marginal alteration of feldspar grains were observed in places. The relationship of the Blue Mountain Granodiorite to the QMM of the Landry Brook pluton is uncertain, as no contacts were observed. Geochronological and geochemical analyses of the Blue Mountain Granodiorite (see below) demonstrate that it is unrelated to the Landry Brook pluton, and the product of a much younger magmatic event.
Dickie Brook pluton
Like the Landry Brook pluton, the Dickie Brook pluton and associated dykes intruded mafic flows and felsic flows and pyroclastic rocks of the Bryant Point and Benjamin formations, respectively. Most of the northeastern and southern parts of the Dickie Brook pluton consist of medium-grained gabbro to quartz gabbro and quartz diorite (Fig. 1). These areas are also cut by diabasic dykes trending northwest-southeast. The contact between the light-coloured quartz diorite and somewhat darker gabbro is subtle but visible in some places (Fig. 3e). The contact is typically sharp, suggesting that the gabbro had cooled prior to subsequent intrusion of the quartz diorite. Dykes of granodiorite composition (slightly higher in quartz and K-feldspar) cut the gabbro and quartz diorite and may be related to the quartz monzodiorite/monzogranite unit that forms more than half of the pluton (Fig. 1). Near the eastern margin, the contact between quartz diorite and gabbro is irregular (e.g., cuspatelobate margins) but towards the west, the contact is sharp and angular. Xenoliths of leucogabbro or quartz diorite were also observed in the quartz monzodiorite/monzogranite (Fig. 3f), indicating that the latter is the youngest unit in the pluton. Flow during emplacement/cooling is suggested by the presence of schlieren or flow layering in the leucogabbro. Hence, small aphanitic diabasic dykes appear to have been boudinaged, possibly by host magma movement during their emplacement. Close to its contact with the host rocks of the Bryant Point and Benjamin formations, the quartz monzodiorite/monzogranite contains centimetre- to metre-scale xenoliths of basalt (probably from the Bryant Point Formation). A melanocratic monzogranite dyke in the Bryant Point Formation north of the pluton is interpreted to be related to the quartz monzodiorite/monzogranite unit based on texture and mineralogy. Diabasic and aphanitic felsic dykes, probably late phases of the pluton, cut the quartz monzodiorite/monzogranite, and are especially visible along the South Branch Benjamin River.
Charlo plutonic suite
The plutons, dykes, and sills of the Charlo plutonic suite consist of varied intermediate to felsic rock including quartz monzonite to monzogranite, quartz-plagioclase rhyolite porphyry, hornblende dacite porphyry, and felsite. They intruded calcareous sedimentary rocks of the Upsalquitch Formation (Fig. 1) and are typically oriented southwest-northeast, parallel to regional strike of bedding and cleavage. Diabase dykes, also oriented southwest-northeast, are abundant in the area, and are assumed to be mainly younger than the felsic rocks, based on cross-cutting relationships observed in several places. Some of the diabase bodies are concordant with bedding and hence sill-like; vugs at the tops of these sills indicate way-up.
Small areas of skarn were observed in the calcareous rocks throughout the area adjacent to the intrusions. A drilling project in 1996-97 by Noranda Inc. evaluated the potential for skarn mineralization; however, no further work has been carried out since then. The drill cores, stored at Madran, New Brunswick, were examined and the lithotypes intersected in drill core correspond to those seen in surface outcrops.
The quartz monzonite to monzogranite occurs in three plutonic bodies; it is cut by later felsite dykes (Fig. 3g) and has sharp contacts with the host rocks. It is possible that the felsite and quartz-plagioclase rhyolite porphyry dykes are somewhat younger than the quartz monzonite, assuming they are all comagmatic. This hypothesis is supported by cross-cutting relationships with the quartz monzonite, but also by their similarity to the late felsite dykes in the Landry Brook and Dickie Brook plutons. Alteration in the rhyolite porphyry is pervasive, indicated by abundant chlorite and calcite veins. The abundance of aligned miarolitic cavities parallel to primary flow fabric suggests that these bodies were emplaced at high levels. No cross-cutting relationships were observed between the hornblende dacite porphyry (Fig. 3h) and the other units.
Blue Mountain Granodiorite
Porphyritic (hiatal to seriate) granodiorite has plagioclase (~[An.sub.25]) phenocrysts varying from 3 to 5 mm in size, with ah altered fine-grained groundmass composed of K-feldspar and quartz (Fig. 4a). In contrast, the medium-grained granodiorite consists of quartz, plagioclase ([An.sub.36-41]), biotite, and minor hornblende (Fig. 4b). It is also less altered than the porphyritic granodiorite. Hence they are texturally and mineralogically distinct, although both host disseminated sulphide minerals (e.g. pyrite, chalcopyrite). A summary of plutonic units and petrographic features are presented in Appendix 1.
Landry Brook pluton
The main body of the Landry Brook pluton varies from quartz monzodiorite to quartz monzonite and monzogranite, depending mainly on the relative abundance of K-feldspar. Colour varies from light grey to dark brick red with increasing degree of alteration. Most of these rocks are medium-grained and in some areas they are porphyritic with zoned plagioclase phenocrysts (Fig. 4c). They contain abundant xenoliths of gabbro/diorite and basalt, the latter likely from the host Bryant Point Formation. The youngest component of the pluton is fine- to medium-grained monzogranite, which in places contains plagioclase phenocrysts in a fine-grained groundmass (Fig. 4d).
Gabbro is generally medium to dark grey and the grain size varies from fine to medium; quartz diorite is texturally similar to the gabbro but lighter in colour. Both the gabbro and quartz diorite consist of plagioclase ([An.sub.44-63]), diopside and/or calcic hornblende, magnetite and minor quartz (less than 5%).
Dickie Brook pluton
Mafic rocks of the Dickie Brook pluton vary in composition, and include gabbro, leucogabbro to quartz gabbro, and diorite to quartz diorite. Gabbro and quartz gabbro contain a higher proportion ofmafic minerals, mainly clinopyroxene, than the leucogabbro. The diorite/quartz diorite (Fig. 4e) is lighter in colour that the gabbroic rocks but with similar medium to coarse grain size. The quartz content is higher than in the gabbroic rocks and the main mafic mineral is hornblende rather than clinopyroxene.
Quartz monzodiorite/monzogranite (Fig. 4f) is typically light pink to dark red, medium-grained and equigranular, but in some places it is porphyritic with phenocrysts of plagioclase (~[An.sub.45]). This unit is fairly homogeneous throughout in terms of texture and composition. Mafic minerals include biotite and hornblende, and titanite as a prominent accessory phase.
Charlo plutonic suite
The main rock types in the Charlo plutonic suite are diabase to gabbro, quartz monzonite to monzogranite, quartz rhyolite porphyry, and hornblende dacite porphyry. The gabbro and diabase occur both as small plutons and as dykes; they are dark grey, fine- to medium-grained, and contain augite-diopside, plagioclase, and magnetite. The quartz monzonite to monzogranite (Fig. 4g) is fine-to medium-grained, and consists of zoned phenocrysts of plagioclase (ranging [An.sub.17-57] from rim to core) in a fine-grained groundmass consisting of granophyric quartz and K-feldspar. It is similar in mineralogy and texture to the quartz monzodiorite/monzogranite units in the Landry Brook and Dickie Brook plutons, and is likely related to them (see Discussion). Miarolitic cavities are abundant, consistent with high-level emplacement. The quartz rhyolite porphyry occurs as dykes that vary from light grey to dark pink depending on the degree of alteration. Quartz phenocrysts are abundant, as are miarolitic cavities. At some locations, sulphide concentration is relatively high. Hornblende dacite porphyry (Fig. 4h) is medium grey, and has hornblende phenocrysts ranging from 3 to 5 mm in size in an aphanitic groundmass. The phenocrysts have a more or less parallel arrangement.
Samples MLNB-733 (Dickie Brook quartz monzodiorite) and 97-DL-04 (Blue Mountain Granodiorite) were collected and analyzed by M.L. Bevier in 1988 and V. McNicoll in 1997, respectively, at the Geological Survey of Canada, Ottawa. Heavy mineral concentrates were prepared by standard crushing, grinding, Wilfley table, and heavy liquid techniques. Mineral separates were sorted by magnetic susceptibility using a Frantz isodynamic separator. Multigrain zircon fractions analyzed were very strongly air abraded following the method of Krogh (1982). U-Pb analytical methods were those outlined in Parrish et al. (1987). Treatment of analytical errors follows Roddick et al. (1987), with regression analysis modified after York (1969). Analytical results are presented in Table 1, where errors on the ages are reported at the 2o level, and displayed in the concordia plot (Figs. 5a, c).
Samples LB00-1 (Landry Brook quartz monzonite) and 09SHM-BR-50 (Dickie Brook quartz monzodiorite) were collected in the summer of 2009 by R.A. Wilson and S. McClaneghan, respectively, and analyzed by S. Kamo at the Jack Satterly Geochronology Laboratory of the University of Toronto. The samples were crushed, pulverized and passed over a Wilfley table. The resulting heavy mineral concentrates were re-processed on
the Wilfley table until a significantly reduced sample size of ~5-10 g was achieved (from rock samples weighing ~8-12 kg). The smaller heavy mineral concentrates were more rapidly processed through mineral separation procedures (i.e., magnetic separation and reduced volumes of methylene iodide of ~2-8 ml) and no longer required the use of the heavy liquid "bromoform". U-Pb analysis was by isotope dilution thermal ionization mass spectrometry methods (ID-TIMS) at the Jack Satterly Geochronology Laboratory of the University of Toronto. Prior to analysis, zircon crystals were thermally annealed and partially dissolved in HF (chemical abrasion), which has the advantage of penetratively removing alteration zones where Pb loss has occurred (Mattinson 2005). Grains were placed in a muffle furnace at ~1000[degrees]C for 60 hours, followed by leaching in a 50:50 solution of HF and 6N HCl in Teflon dissolution vessels at 195[degrees]C for 16 hours. After selecting the zircons, their dimensions were measured, and the weights of each grain were calculated. The grains were washed in 8N HN[O.sub.3] acid and ultra-clean acetone prior to dissolution. A [sup.205]Pb-[sup.233]U-[sup.235]U spike (ET535) was added to the Teflon dissolution capsules during sample loading. Zircon was dissolved using ~0.10 mL of concentrated HF and ~0.02 mL of 7N HN[O.sub.3] in teflon bombs at 195[degrees]C (Krogh, 1973) for five days, and re-dissolved in ~0.15 mL of 3N HCI. Uranium and Pb were isolated from the zircon solutions using 50 microlitre anion exchange columns, dried in dilute H3PO4 acid, and deposited onto outgassed rhenium filaments with silica gel (Gerstenberger and Haase 1997). Uranium and Pb were analyzed with a VG354 mass spectrometer using a Daly pulse-counting system. The dead time of the measuring system for Pb and U was 21.5 nsec. The mass discrimination correction for the Daly detector is constant at 0.05%/atomic mass unit. Amplifier gains and Daly characteristics were monitored using the SRM982 Pb standard. Thermal mass discrimination corrections are 0.10%/atomic mass unit. The total amount of common Pb for each analysis (Table 1) was attributed to laboratory Pb, thus no correction for initial common Pb from geological sources was made.
In geologically young zircons, the [sup.238]U/[sup.206]Pb dating system is the most reliable and precise because of the much greater abundance of [sup.238]U. Therefore, the results (Table 1 and Fig. 5) presented herein refer exclusively to the [sup.206]Pb/[sup.238]U ages.
Four multigrain zircon fractions were analyzed in sample 97-DL-04, representing the various zircon morphologies in the sample, including equant multifaceted crystals (fraction A), prismatic crystals with aspect ratios of about 2:1 (fractions B1 and B2), and elongate, needle-like grains (fraction C). Most of the zircon grains analyzed contain minor fluid inclusions. Three of the analyses overlap and are near-concordant (Fig. 5a). Analysis B2 contains an inherited component and is not included in the age calculation. A weighted average of the [sup.206]Pb/[sup.238]U ages of fractions A, B1, and C is calculated to be 400.7 [+ or -] 0.4 Ma (Fig. 5a), which is interpreted to be the crystallization age of the Blue Mountain Granodiorite.
In sample LB00-1 from the Landry Brook pluton, abundant zircons are euhedral, sharply-facetted, pink, multi-facetted to 2:1 prismatic, fresh and gem-like, and contain abundant bubble-like melt inclusions. The U-Pb data for four, single, chemically-abraded zircon crystals give concordant, highly reproducible data. The weighted mean [sup.206]Pb/[sup.238]U age is 419.63 [+ or -] 0.23 Ma (Fig. 5b) and this is interpreted as the best age estimate for the Landry Brook pluton, which is significantly older that the previously reported age of 370 [+ or -] 30 Ma (whole-rock Rb-Sr; Stewart 1979). It is also older than the spatially related Blue Mountain Granodiorite (401.7 [+ or -] 0.4 Ma).
Two independent age analyses were done at the same location (Fig. 2a) on the Dickie Brook pluton. A comparison of sample MLNB-733 with the recently collected sample 09SHM-BR50 enabled us to verify the accuracy of the original age determination. The zircons analyzed in sample MLNB-733 were pale yellow, clear, stubby to elongate square prisms with simple terminations. Both samples show three-data-point clusters with weighted mean [sup.206]Pb/[sup.238]U ages of 418.1 [+ or -] 1.3 Ma (Fig. 5c) and 418 [+ or -] 1 Ma (Fig. 5d), respectively. In sample 09SHM-BR50, the fourth data point is older and plots outside the error range of the cluster, having a [sup.206]Pb/[sup.238]U age of 420.7 [+ or -] 0.8 Ma. This grain is interpreted as having crystallized 2-3 my prior to the granite, and was incorporated into the granite magma source or during emplacement of the granite body. Therefore, the age of the granite is interpreted to be 418 [+ or -] 1 Ma, making it, within error, coeval with the Landry Brook pluton.
Forty samples from the Landry Brook and Dickie Brook plutons, the Charlo plutonic suite, and Blue Mountain Granodiorite were analysed for major and trace elements, including rare-earth elements (Appendix 2 and 3) at ACME Analytical Laboratories Ltd., Vancouver, Canada. Lithologically homogeneous samples (i.e., barren of enclaves) were collected with an effort to ensure that the freshest, least altered samples were taken. However, the spatial distribution of collected samples is, in general, dependant on the available exposed bedrock.
The purpose of this section is to describe the chemical characteristics of the plutons based on these data. In order to compare the chemical characteristics of the Landry Brook and Dickie Brook plutons and the Charlo plutonic suite, all of the samples are plotted together on Harker variation diagrams. The geochemical data of Whalen (1993) also are included on these diagrams to increase the amount of data, and include 6 samples from the Landry Brook pluton, 4 samples from the Dickie Brook pluton, and 4 samples from the Charlo plutonic suite.
Major Element Compositions
In the Landry Brook pluton and Charlo plutonic suite, gabbro/quartz diorite and diabase have Si[O.sub.2] concentrations of 47-50 wt. % (Fig. 6), anda gap in Si[O.sub.2] separates those rocks from intermediate to felsic rocks, which vary from 58 to 78 wt. % Si[O.sub.2], Samples from the Dickie Brook pluton have a continuous silica spectrum ranging from 50% to 72%. Overall, Ti[O.sub.2], [Al.sub.2][O.sub.3], [Fe.sub.2][O.sub.3.sup.t], MgO, and CaO show similar negative correlation with Si[O.sub.2] in all three plutons (Fig. 6), consistent with decreasing abundances of ferromagnesian minerals, plagioclase, titanite, and magnetite. Amounts of Ti[O.sub.2], [Fe.sub.2][O.sub.3.sup.t], MgO, and CaO (Figs. 6a, c-e) are higher in gabbro/quartz diorite samples than in samples from the intermediate-felsic units, reflecting their greater abundance of ferromagnesian minerals and calcic plagioclase. Although they vary little in Si[O.sub.2], the gabbro/quartz diorite samples show a wide range in most other major oxides including Ti[O.sub.2], [Al.sub.2][O.sub.3], [Fe.sub.2][O.sub.3.sup.t], MgO, and CaO (Figs. 6a-e), consistent with the varying abundances of clinopyroxene, amphibole, plagioclase, opaque minerals, and titanite observed in these samples.
Both [K.sub.2]O and [Na.sub.2]O (Figs. 6f, g) show positive correlation with Si[O.sub.2], consistent with the absence of K-bearing minerals (e.g., K-feldspar and biotite) in the mafic rocks. [Na.sub.2]O shows an increase and then a decrease after about 65 % Si[O.sub.2], which could be linked to fractionation of increasingly Na-rich plagioclase as the magma evolved.
In samples from the Landry Brook pluton and Charlo plutonic suite, a gap in MgO of about 2-3 wt. % separates mafic samples and intermediate-felsic samples (Fig. 6d). For example, the abundance of Mg-rich clinopyroxene in the gabbro compared to its minor presence in the quartz monzodiorite in samples from the Charlo plutonic suite is consistent with this gap, which does not exist in the [Fe.sub.2][O.sub.3.sup.t] data (Fig. 6c). Samples from the hornblende dacite porphyry dyke in the Charlo plutonic suite and porphyritic granodiorite in the Blue Mountain Granodiorite tend to diverge from the trends defined by samples from the other units, with slightly higher [Al.sub.2][O.sub.3], CaO, and MgO and lower Ti[O.sub.2], [Fe.sub.2][O.sub.3.sup.t], and [K.sub.2]O. The quartz rhyolite porphyry in the Charlo plutonic suite is the most felsic unit in the study area, and has very low abundances of all of these components. Overall, [P.sub.2][O.sub.5] shows a wide spread in the more mafic samples, linked to modal variations in apatite content, and then decreases in the felsic samples, likely as a result of apatite fractionation, perhaps as inclusions in the fractionating ferromagnesian minerals
Collectively, samples from the four intermediate-felsic units show negative correlation of [Al.sub.2][O.sub.3], Ti[O.sub.2], [Fe.sub.2][O.sub.3.sup.t], MgO, MnO, and CaO with Si[O.sub.2], consistent with fractionation of ferromagnesian minerals and calcic plagioclase. The mafic units in the Landry Brook pluton and Charlo plutonic suite are similar, except that the gabbro in the Charlo plutonic suite contains much lower CaO (Fig. 6e) and higher [Na.sub.2]O and P2Os (Figs. 6f, h). Overall, the samples from all units are similar, although diorite/quartz diorite from the Dickie Brook pluton shows the greatest deviation from the norm.
Trace and Rare-Earth Element Compositions
Ratios of Zr/Ti[O.sub.2] show a stronger variation than Nb/Y (Fig. Ta) with lower Zr/Ti[O.sub.2] values for the mafic units, consistent with the negative correlation of Ti[O.sub.2] and Si[O.sub.2] (Fig. 6a). These ratios plotted on a volcanic rock-equivalent discrimination diagram (Fig. Ta) are more or less consistent with the names determined using modal mineralogy. High Zr/Y and Th/Yb ratios (Fig. 7b) associate the rocks with calc-alkaline affinity, consistent with the range rock types present. The rhyolite porphyry plots outside the main data cluster due to high values of Y relative to Zr. This feature is also shown using Zr/Hf against Zr (Fig. 7c) with high Hf values relative to Zr. Although most of the units are shown in the Chondrite and Cumulate residue fields, the rhyolite porphyry from the Charlo plutonic suite is more likely to result from the melting of continental crust. La/Yb ratios (Fig. 7d) for all units are similar (<14), whereas the Blue Mountain Granodiorite and Charlo dacite porphyry have La/Yb ranging from 22 to 48, suggesting that they were generated from a genetically unrelated source that probably contained garnet (Thirlwall et al. 1994).
Comparing the chondrite-normalized REE diagrams from pluton to pluton (Figs. 8a-c), the Blue Mountain Granodiorite (Fig. 8a) and dacite porphyry of the Charlo plutonic suite (Fig. 8c) are strikingly similar, with significantly lower values in heavy REE and higher La/Yb ratios (Fig. 7c). The gabbro/quartz diorite samples from the Landry Brook pluton tend to have lower total REE than the other units (Fig. 8a), including lower LREE and higher heavy REE, probably linked to the abundance of apatite and other accessory minerals. The REE pattern for the rhyolite porphyry from the Charlo plutonic suite also shows elevated heavy REE (Fig. 8c), as do the two samples from the monzogranite unit in the Landry Brook pluton (Fig. 8a).
Similar sloping profiles of decreasing light to heavy REE's for the quartz monzodiorite/monzogranite of the Landry Brook pluton, all of the units of the Dickie Brook pluton, and the quartz monzodiorite/monzogranite of the Charlo plutonic suite suggest that all of these units are co-magmatic, which is supported by the similarities on variation and ratio diagrams (Figs. 6-8).
CHEMICAL AFFINITY AND TECTONIC SETTING
Petrographic and chemical characteristics described in previous sections suggest that most of the units in the Landry Brook and Dickie Brook plutons and Charlo plutonic suite are comagmatic and potentially linked by fractional crystallization, predominantly of plagioclase and amphibole. All three plutons show calc-alkaline trends, although some samples show moderate iron enrichment and plot on or slightly above the tholeiitic/calc-alkaline dividing line on an AFM diagram (Fig. 9a). This diagram illustrates the bimodality of the Landry Brook pluton compared to the more continuous trends in the other two plutons; the Landry Brook gabbros may therefore represent part of an unrelated but coeval suite that appears to be tholeiitic based on the AFM diagram (Fig. 9a). The Blue Mountain Granodiorite and the dacite porphyry from the Charlo plutonic suite are also calc-alkaline, but have relatively higher MgO and hence forma cluster distinct from the trends of the other plutons (Fig. 9a). Given the much younger age obtained for the Blue Mountain Granodiorite, its close geochemical similarity with the dacite porphyry suggests that the latter is probably also Devonian.
AII samples with more than 60% Si[O.sub.2] are metaluminous to peraluminous based on the Si[O.sub.2] vs. A/CNK classification diagram for granitoid rocks (Fig. 9b). The Landry Brook pluton and Charlo plutonic suite straddle the metaluminous-peraluminous fields, although none of these rocks have mineralogical characteristics of peraluminous granite (such as primary muscovite or other Al-rich minerals) and the apparently peraluminous character is probably related to alkali mobility. Hornblende fractionation could be another factor contributing to the peraluminous character (Cawthorn and Brown 1976). All samples of altered rhyolite porphyry from the Charlo plutonic suite are peraluminous, whereas the Dickie Brook pluton, in contrast, is entirely metaluminous. The Blue Mountain Granodiorite is somewhat more peraluminous than all other units, with higher alumina relative to soda and potash; however, the Charlo dacite porphyry is metaluminous (Fig. 9b).
On Rb vs. Y + Nb and Hf-Rb-Nb tectonic discrimination diagrams for granitoid rocks (Figs. 9c, d), intermediate and felsic rocks straddle the volcanic-arc and within-plate fields, with most points falling within the circular field for post-collisional granitoids (Pearce 1996a). The Dickie Brook quartz monzodiorites and monzogranites display the most prominent within-plate character on both diagrams, whereas the Blue Mountain Granodiorite and Charlo dacite porphyry have lower Y and Nb and plot in the field of volcanic-arc granites (Figs. 9c, d). On average, all samples are more typical of I-type granitoid rocks than A-type granitoids (Fig. 10). Looking at just the mafic rocks from all three plutons, most samples from the Dickie Brook pluton plot in the calk-alkaline field on a Th-Hf-Ta diagram (Fig. 9e), whereas samples from the Landry Brook pluton plot in the alkalic field. Quartz monzodiorite in the Charlo plutonic suite plots in the calc-alkalic basah field, although related gabbros overlap two or more fields (Fig. 9e). On a La-Y-Nb plot (Fig. 9f) most mafic rocks from all plutons plot in the continental tholeiite field.
Oxygen and Sm-Nd isotope data for these plutons were reported by Whalen (1993). The [[delta].sup.18][O.sub.WR] values are 6.6 in a sample from the Dickie Brook pluton, 6.5 in a sample from the Landry Brook pluton, and 7.4 in a sample from the Charlo plutonic suite (Whalen 1993). Al1 are within the range expected of granitoid rocks derived from mantle-like
sources (Taylor 1988). The [[epsilon].sub.Nd] isotopic signatures of these rocks are relatively high (+1.2, +2.0, and +4.5) which suggests mainly a mantle source but with some crustal interaction (Whalen 1993). Overall, the values are higher than [[epsilon].sub.Nd] signatures reported from Ganderia in Newfoundland, which tend to be negative (e.g., Kerr et al. 1995; Whalen et al. 1994).
Overall, the tectonic setting for these plutons is most likely within-plate but the data such as high Zr/Y and Th/Yb ratios indicate a subduction influence, such as in a back-arc setting. Their chemical characteristics are explored in more detail below, together with data from the associated and more voluminous volcanic rocks of the Dickie Cove Group.
RELATIONSHIPS WITH THE HOST ROCKS
The host rocks of the Landry Brook and Dickie Brook plutons, and part of the Charlo plutonic suite, are the Bryant Point Formation and overlying Benjamin Formation of the Dickie Cove Group (Fig. 1), consisting mainly of subaerial mafic and felsic volcanic rocks, respectively (Walker and McCutcheon 1995; Wilson and Kamo 2012). A rhyolite flow from near the base of the Bryant Point Formation has yielded a U-Pb (zircon) age of 422.3 [+ or -] 0.3 Ma, whereas a U-Pb (zircon) age of 419.7 [+ or -] 0.3 Ma was obtained for rhyolite at the top of the Benjamin Formation (Wilson and Kamo 2012). Emplacement of the Landry Brook quartz monzodiorite at 419.63 [+ or -] 0.23 Ma (Fig. 5) was therefore essentially coeval with cessation of felsic volcanism. Emplacement of the Dickie Brook quartz monzodiorite/monzogranite occurred shortly thereafter, at 418 [+ or -] 1 Ma (Fig. 5).
Mafic volcanic rocks of the Bryant Point Formation show chemical similarities to gabbro and leucogabbro (<52 % Si[O.sub.2]) from the Landry Brook and Dickie Brook plutons and Charlo plutonic suite. Like the plutons, the Bryant Point Formation is mainly calk-alkaline but straddles the boundary with the tholeiite field (Fig. 11a). On a multielement spidergram (Fig. l lb), the mafic samples show similar patterns, with negative anomalies in Cs, Rb, K, anda positive anomaly in Sr. REE patterns of volcanic and plutonic rocks are similar, with most showing parallel patterns and continuous depletion from LREE to HREE, with the exception of slight positive Eu anomalies in a few samples (Fig. 11c). On a Hf-Th-Ta diagram (Fig. 11d), most samples span the calc-alkalic basalt to within-plate tholeiite/ E-MORB fields; only gabbros from the Landry Brook pluton plot in the alkaline basalt field. However, most volcanic and plutonic rocks plot in the within-plate field on a Ti-Zr-Y diagram (Fig. 11e), and in a cluster that overlaps the within-plate and volcanic-arc fields on a Zr-Y-Nb diagram (Fig. 11f). In general, these strong similarities are consistent with the volcanic and mafic plutonic rocks being co-magmatic and formed in a continental within-plate setting as suggested previously by Dostal et al. (1989).
Late Silurian felsic volcanic rocks of the Benjamin Formation also have chemical similarities to felsic intrusive rocks of all three plutons. Plotted together on a multi-element variation diagram normalized to primitive mantle, the volcanic and plutonic rocks show similar patterns, including pronounced negative Ba, Nb, Sr, Eu, and Ti anomalies (Fig. 12a). The REE profiles are also similar, with strong negative Eu anomalies, although the volcanic rocks tend to have higher REE overall (Fig. 12b). In terms of tectonic setting, both volcanic and plutonic rocks plot in the within-plate/post-collisional/volcanic-arc granite fields (Figs. 12c, d), consistent with a co-magmatic relationship. Dostal et al. (1989) suggested a within-plate setting based on their study of the volcanic rocks.
The complex history of the Appalachian orogen can be summarized in terms of processes related to the Palaeozoic closure of the Iapetus and Rheic oceans, which led to the accretion of arcs, back arcs, and microcontinents to Laurentia (e.g., van Staal et al. 2009). Temporally, the emplacement of the Landry Brook and Dickie Brook plutons and Charlo plutonic suite was associated with the accretion of Ganderia to Laurentia. However, Ganderia itselfhas a complex tectonic history both prior to and after accretion to Laurentia (van Staal et al. 2009). Remnants of the Popelogan-Victoria arc and rocks deposited in the associated Tetagouche-Exploits back-arc basin (e.g., van Staal et al. 2003) were accreted to Laurentia (forming the Bathurst Subduction Complex) during the Early Silurian, prior to the arrival of the main part of Ganderia (i.e., during the early phase of the Salinic orogeny; Fig. 13a). This was followed by the Devonian Acadian orogeny, which was associated with the collision of Avalonia and Laurentia (Fig. 13b).
Based on geological and chemical characteristics of the sedimentary and volcanic rocks in the region, including Quebec, Wilson et al. (2008) suggested that subduction of the Tetagouche-Exploits back-arc crust ceased by the Early Wenlockian (ca. 428 Ma, coincident with the arrival of the leading edge of Ganderia), and was followed by uplift and extension during the Wenlockian to Pridolian (ca. 428-416 Ma; Fig. 13a). Wilson et al. (2008) suggested that slab-break-off occurred after the last "gasp" of subduction-related calc-alkaline rocks represented by ash tuff dated at ca. 429 Ma (i.e., Pointe Rochette ash; Fig. 14) in the lower part of the Quinn Point Group. Wilson et al. (2008) further suggested that extensional magmatism associated with slab break-off is manifested in the bimodal within-plate volcanic rocks of the Bryant Point and Benjamin formations (Dickie Cove Group). These rocks generally post-dated structures formed during the Salinic orogeny but predated development of Acadian structures in the area; that is, they were emplaced to the northwest of the migrating Acadian deformation front (Bradley and Tucker 2002). The results of this study have shown that the Landry Brook and Dickie Brook plutons and Charlo plutonic suite are the intrusive equivalents of these volcanic units.
This sequence of events is consistent with those interpreted to have occurred along strike in Newfoundland with slab breakoff and uplift following Salinic collision (Whalen et al. 2006). Based on extensive geochronological, geochemical and isotopic data, Whalen et al. (2006) demonstrated the compositional and spatial variations within the magmatic belt, involving rapid progression from exclusively arc-type to non-arc-like mafic magmatism, with a short episode of "A-type" granite generation, followed by contemporaneous emplacement of granitoids with both within-plate and volcanic-arc characteristics.
Many mantle melts can be influenced by contamination from the crust and hence may display some chemical characteristics of volcanic-arc rocks without being associated temporally with the partial melting of a subducted slab; however, it is most likely that arc-type chemical signatures observed in volcanic and plutonic rocks in the study area arise from contamination of the asthenospheric source by previous subduction events. This likely explains the I-type granitoid characteristics of the three studied plutons.
The Blue Mountain Granodiorite and dacite porphyry of the Charlo plutonic suite are temporally related to the collision of Avalonia with composite Laurentia (Fig. 13b). Widespread magmatism associated with this event is attributed to 'flat-slab' subduction (Murphy et al. 1999), somewhat analogous to the Laramide in the western USA and the present-day Andes in central Chile and Argentina (Kay and Abruzzi 1996; van Staal et al. 2009). Their chemical volcanic-arc affinities are consistent with this model, but it is difficult to envisage why such plutonism would be so sparsely distributed over such a wide area.
This work has demonstrated that the Landry Brook and Dickie Brook plutons and the Charlo plutonic suite are approximately contemporaneous and Late Silurian in age. The close petrochemical similarity between quartz monzodiorite/monzogranite unit of the Landry Brook pluton, all units of the Dickie Brook pluton, and the quartz monzodiorite/monzogranite of the Charlo plutonic suite suggest that they share a common, or at least similar, mantle source, and a similar petrogenetic history. The mafic and felsic phases of the plutons show chemical affinities with mafic and felsic volcanic rocks, respectively, of the Benjamin and Bryant Point formations, suggesting that they are cogenetic. The geological and chemical characteristics are consistent with emplacement in a post-collisional extensional regime. The magma was probably generated as a result of slab break-off and resultant high heat flow associated with upwelling asthenosphere under the extinct Popelogan-Victoria arc following closure of the Tetagouche-Exploits back-arc basin (Salinic collision). Another pulse of magmatic activity occurred ca. 400 Ma, as indicated by Blue Mountain Granodiorite (and probably dacite porphyry of the Charlo plutonic suite); however, the causes of the later magmatic pulse (ca. 400-415 Ma) are not addressed in this study, and are probably associated with a somewhat different tectonic setting and different petrogenetic processes.
Appendix 1. Summary of plutonic units and petrographic features *. Plutonic Unit Grain Size Plagioclase (composition) Blue Mountain Granodiorile granodiorite f.g-m.g. sub-to anhedral ([An.sub.36] to [An.sub.40,7]) Landry Brook pluton gabbro/quartz diorite f-g--c.fr subhedral, zoned ([An.sub.36] to [An.sub.40,7]) quartz monzodiorite/ m.g subhedral, zoned monzogranite ([An.sub.30,6] to [An.sub.49,3]) monzogranite f.g.-m.g subhedral, zoned ([An.sub.18,6] to [An.sub.33,3]) Dickie Brook pluton leucogabbro/quartz gabbro m.g.-c.g. subhedral, zoned ([An.sub.50] to [An.sub.60]) diorite/quartz diorite m.g.-c.g. subhedral, zoned ([An.sub.25,3] to [An.sub.45,3]) quartz monzodiorite/ in.fr subhedral, zoned monzogranite (albite to [An.sub.45,3]) Charlo plutonic suite gabbro/diabase fg-m.g. lath-shaped (labradorite) quartz monzonite/ f.g.-m,g. an- to subhedral, monzogranite zoned ([An.sub.17,3] to [An.sub.57,3]) quartz rhyolite porphyry v.f.fr-m.g. anhedral (oligoclase) hornblende-plagioclase v-f-g-f-g- an- to subhedral, dacite porphyry zoned, (nd) Plutonic Unit K-feldspar Quartz Blue Mountain Granodiorile granodiorite subhedral to interstitial anhedral; orthoclase Landry Brook pluton gabbro/quartz diorite none trace, interstitial quartz monzodiorite/ an- to subhedral; interstitial monzogranite orthoclase monzogranite anhedral; nd interstitial Dickie Brook pluton leucogabbro/quartz gabbro none minor, interstitial diorite/quartz diorite none interstitial quartz monzodiorite/ anhedral; nd interstitial monzogranite Charlo plutonic suite gabbro/diabase trace, interstitial quartz monzonite/ anhedral; nd interstitial monzogranite quartz rhyolite porphyry anhedral; nd interstitial hornblende-plagioclase anhedral; nd interstitial dacite porphyry Plutonic Unit Clinopyroxene Blue Mountain Granodiorile granodiorite none Landry Brook pluton gabbro/quartz diorite 20-30%; diopside quartz monzodiorite/ none monzogranite monzogranite none Dickie Brook pluton leucogabbro/quartz gabbro 15-25%; augite? diorite/quartz diorite 10-15%; diopside quartz monzodiorite/ 5%; augite-diopside monzogranite and hedenbergite Charlo plutonic suite gabbro/diabase 15-30%; augite- diopside quartz monzonite/ none monzogranite quartz rhyolite porphyry none hornblende-plagioclase none dacite porphyry Plutonic Unit Amphibole Blue Mountain Granodiorile granodiorite <3%; nd Landry Brook pluton gabbro/quartz diorite 5%; calcic to ferro-hornblende quartz monzodiorite/ 5-15%; calcic to monzogranite ferro-hornblende monzogranite 7%; nd Dickie Brook pluton leucogabbro/quartz gabbro 10%; nd diorite/quartz diorite 15-25%; edenite quartz monzodiorite/ 10-15%; ferro-edenite monzogranite with low Mg Charlo plutonic suite gabbro/diabase quartz monzonite/ 15%; nd monzogranite quartz rhyolite porphyry none hornblende-plagioclase 5%; hornblende dacite porphyry Plutonic Unit Biotite Opaque Blue Mountain Granodiorile granodiorite 5-10%; phlogopite cpy, py, mag to annite Landry Brook pluton gabbro/quartz diorite none mag, ilm quartz monzodiorite/ 5-7%; phlogopite ml, secondary? monzogranite to annite monzogranite 7-8%; phlogopite mag to annite Dickie Brook pluton leucogabbro/quartz gabbro none mag, ilm diorite/quartz diorite none nd quartz monzodiorite/ none mag, py monzogranite Charlo plutonic suite gabbro/diabase mag quartz monzonite/ 15%; high aluminum nd monzogranite phlogopite -annite quartz rhyolite porphyry none none hornblende-plagioclase secondary minor dacite porphyry Plutonic Unit Accessory Blue Mountain Granodiorile granodiorite apatite, zircon, titanite Landry Brook pluton gabbro/quartz diorite apatite, titanite quartz monzodiorite/ apatite, zircon, monzogranite titanite monzogranite apatite, zircon Dickie Brook pluton leucogabbro/quartz gabbro apatite, titanite diorite/quartz diorite apatite, titanite quartz monzodiorite/ titanite, minor monzogranite apatite Charlo plutonic suite gabbro/diabase quartz monzonite/ apatite, zircon, monzogranite titanite quartz rhyolite porphyry nd hornblende-plagioclase nd dacite porphyry Plutonic Unit Other information Blue Mountain Granodiorile granodiorite equigranular to porphyritic, hosts Cu-mineralization Landry Brook pluton gabbro/quartz diorite Intergranular to ophitic cpx-plag quartz monzodiorite/ Granophyric orthoclase monzogranite monzogranite interstial granophyric texture; perthitic K- Dickie Brook pluton feldspar leucogabbro/quartz gabbro Intergranular to ophitic cpx-plag diorite/quartz diorite abundant inclusions of apatite in amphibole quartz monzodiorite/ perthitic K-feldspar monzogranite Charlo plutonic suite gabbro/diabase pervasive carbonate alteration quartz monzonite/ granophyric and monzogranite perthitic K- feldspar quartz rhyolite porphyry highly altered, hiatal porphyritic hornblende-plagioclase skeletal hornblende, dacite porphyry hiatal plagioclase- phyric Abbreviations: v.f., f, m, and e.g., very fine-, fine-, medium-, and coarse-grained; cpy, chalcopyrite; cpx, clinopyrox enc; ilm, ilmcnite; mag, magnetite; plag, plagioclase; py, pyrite; nd, not determined. Appendix 2. Chemical data for samples from the Blue Mountain Granodiorite, Landry Brook and Dickie Brook plutons, and Charlo plutonic suite. Sample Lithology Si[O.sub.2] Blue Mountain Granodiorite JL-09-024 granodiorite 66.40 JL-09-057 granodiorite 70.40 JL-10-139 granodiorite 66.40 7020-101 tonalite 67.90 7012-130 granodiorite 67.30 7003-295 granodiorite 66.40 Landry Brook pluton JL-09-020 monzogranite 71.30 JL-09-030 monzogranite 70.10 JL-09-037 quartz monzonitc 64.50 JL-09-072 quartz monzonitc 64.80 JL-10-077 rhyolite/syenogranite 66.10 porphyry JL-10-081 monzogranite 64.40 JL-09-086 gabbro 47.00 Dickie Brook pluton IL-09-202 monzogranite 67.50 JL-09-207 quartz gabbro 59.50 JL-09-209 monzogranite 66.00 JL-09-214 monzogranite 70.90 JL-09-220 monzogranite/granodiorite 70.80 JL-09-228 dioritc/gabbro 53.80 JL-09-229 hornblende quartz diorite 50.80 JL-09 235 quartz monzodiorite 55.70 JL-10-304 quartz gabbro 52.40 JL-10-311 quartz, monzodiorite 64.10 JL-10-322 tonalite 63.60 JL-10-373 granodiorite 57.00 JL-10-383 quartz monzodiorite 59.60 JL-10-386 monzogranite 71.50 Charlo Plutonic suite JL-10-006 quartz monzonite 57.90 JL-10-007 quartz monzodiorite 62.60 JL-10-019 microgranite 65.30 JL-10-039 dacite porphyry 67.50 JL-10-058 rhyolite/syenogranite 73.70 JL-10-060 rhyolite porphyry 77.20 JL-10-092 rhyolite porphyry 73.70 JL-10-093 rhyolite porphyry 76.70 JL-10-094 alkali rhyolite porphyry 77.00 JL-10-104 diabase 46.30 JL-10-108 diabase 47.40 JL-10-113 monzogranite 66.50 JL-10-119 gabbro/quartz gabbro 50.60 Sample [Al.sub.2][0.sub.2] [Fe.sub.2][0.sub.3] CaO MgO Blue Mountain Granodiorite JL-09-024 17.02 2.95 2.82 1.44 JL-09-057 15.33 1.88 2 14 0.83 JL-10-139 16.78 2.98 2.93 1.84 7020-101 16.35 2.14 3.37 1.18 7012-130 15.97 2.68 2.76 1.07 7003-295 15.53 2.48 3.45 1.12 Landry Brook pluton JL-09-020 14.52 2.57 0 15 0.21 JL-09-030 14.66 2.61 0.79 0.24 JL-09-037 15.49 4.82 2.11 1.19 JL-09-072 15.57 4.95 2.91 1.21 JL-10-077 15.39 4.36 2.57 1.15 JL-10-081 15.43 4.57 1.93 1.12 JL-09-086 18.80 7.04 12.46 9.27 Dickie Brook pluton IL-09-202 14.69 5.63 1 23 0.21 JL-09-207 18.27 5.23 5.14 1.45 JL-09-209 15.42 5.68 1.26 0.48 JL-09-214 14.40 2.22 1 25 0.33 JL-09-220 14.05 2 93 0.52 0.23 JL-09-228 21.94 4.25 7.30 1.73 JL-09-229 20.21 7.99 9.66 2.78 JL-09 235 16.96 9.02 5.35 2.28 JL-10-304 15.70 11.16 8.43 3.61 JL-10-311 16.52 2.50 3.31 2.36 JL-10-322 16.11 5.46 2.00 0 95 JL-10-373 14.71 8.27 6.19 2.87 JL-10-383 16.49 3.46 6.68 2.00 JL-10-386 14.15 2.39 0.69 0.13 Charlo Plutonic suite JL-10-006 11.37 8.87 2.56 2.40 JL-10-007 15.19 6.53 2.33 1.35 JL-10-019 14.38 6.12 1.21 1.11 JL-10-039 15.58 2.32 2.78 1.01 JL-10-058 13.52 1.84 0.38 0.16 JL-10-060 13.33 0.70 0.02 0.15 JL-10-092 13.36 2.12 0.18 0.11 JL-10-093 12 16 1.20 0.25 0.12 JL-10-094 11.83 1.11 0.01 0.05 JL-10-104 16.91 11.53 2.21 6.58 JL-10-108 16.47 11.96 5.45 6.07 JL-10-113 14.94 5.18 1.29 0.81 JL-10-119 16.68 9.54 4.91 5.54 Sample [Na.sub.2]O [K.sub.2]O MnO Ti[O.sub.2] Blue Mountain Granodiorite JL-09-024 4.97 1.76 0.07 0.43 JL-09-057 4.50 2.70 0.02 0.30 JL-10-139 1.71 1.42 0.05 0.44 7020-101 4.53 2.09 0.03 0.40 7012-130 5.11 1.93 0.07 0 37 7003-295 3.72 2.31 0.05 0.37 Landry Brook pluton JL-09-020 4.91 4.58 0.03 0.30 JL-09-030 5.07 4.43 0.04 0.30 JL-09-037 4.35 3.71 0.07 0.77 JL-09-072 4 60 3.57 0.07 0.75 JL-10-077 4.45 3.77 0.08 0.66 JL-10-081 4.28 4.24 0.11 0.74 JL-09-0S6 1.72 0.54 0.12 0.69 Dickie Brook pluton IL-09-202 6.18 2.66 0.12 0.44 JL-09-207 7.57 0.59 0.09 0.99 JL-09-209 7.30 1.58 0.16 0.49 JL-09-214 5.76 3.62 0.03 0.30 JL-09-220 5.56 3.78 0.05 0.30 JL-09-228 6.17 0.83 0.13 1.03 JL-09-229 4.42 0.56 0.11 2.16 JL-09 235 5.41 1.65 0.14 1.60 JL-10-304 4.27 0.40 0.18 2.40 JL-10-311 7.00 0.75 0.04 0.69 JL-10-322 6.44 2 49 0.07 0.68 JL-10-373 5.29 1.24 0.15 2.06 JL-10-383 7.89 1.35 0.08 1.51 JL-10-386 5.38 3.72 0.03 0.31 Charlo Plutonic suite JL-10-006 4.68 3.18 0.17 1.47 JL-10-007 4.86 3.57 0.14 1.04 JL-10-019 3.32 4.10 0.08 0.92 JL-10-039 5.55 1.39 0.03 0.42 JL-10-058 4.16 4.68 0.03 0.23 JL-10-060 4.24 3.04 0.01 0.07 JL-10-092 3 34 5.04 0.05 0 20 JL-10-093 4.56 3.54 0.02 0.12 JL-10-094 2.86 5.19 0.01 0.15 JL-10-104 4.38 1.55 0.16 2.07 JL-10-108 4.75 0.68 0.15 2.45 JL-10-113 5.19 2.57 0.10 0.73 JL-10-119 4.19 1.26 0.19 1.70 Sample [P.sub.2][O.sub.5] LOI Total Rb Sr Ba Blue Mountain Granodiorite JL-09-024 0.15 1.62 99.63 39 707 413 JL-09-057 0.07 1.40 99.57 47 388 443 JL-10-139 0.09 1.84 99.16 36 523 365 7020-101 0.08 0.91 99.03 40 581 526 7012-130 0.10 2.35 99.75 31 614 442 7003-295 0.10 4.59 100.22 53 271 485 Landry Brook pluton JL-09-020 0.04 1.21 99.86 139 68 540 JL-09-030 0 0! 0.96 99.27 142 121 526 JL-09-037 0 19 2.19 99.43 111 230 488 JL-09-072 0.20 O.20 99.63 135 224 461 JL-10-077 0 1S 1.34 100.15 127 204 460 JL-10-081 0.18 2.39 99.49 131 236 495 JL-09-086 0.04 2 52 100.26 18 463 88 Dickie Brook pluton IL-09-202 0.06 0.54 99.62 42 124 583 JL-09-207 0.30 0.55 100.01 6 461 400 JL-09-209 0.09 1.29 99.56 25 149 634 JL-09-214 0.04 0.69 99.67 51 179 709 JL-09-220 0.03 0.86 99.19 91 116 497 JL-09-228 0.25 2.00 99.49 15 700 391 JL-09-229 0.09 0.69 99.52 9 593 214 JL-09 235 0.45 1.14 99.77 38 428 430 JL-10-304 0.34 0.90 99.86 7 380 214 JL-10-311 o.os 1.65 99.00 18 368 129 JL-10-322 0.23 1.51 99.90 60 296 473 JL-10-373 0.44 0 34 99.08 24 329 295 JL-10-383 0.55 1.15 99.78 7 478 141 JL-10-386 0.03 0.87 99.28 59 111 733 Charlo Plutonic suite JL-10-006 0.41 2.55 98.68 104 437 567 JL-10-007 0.28 1.67 99.60 111 217 643 JL-10-019 0.23 2.91 99.75 136 83 413 JL-10-039 0.09 2.96 99.69 26 601 263 JL-10-058 0.03 1.06 99.83 162 62 4116 JL-10-060 0.01 1.27 100.06 91 68 163 JL-10-092 0.01 1.51 99.65 157 62 411 JL-10-093 0.01 0.79 99.47 96 61 266 JL-10-094 0.02 1.18 99.42 205 25 193 JL-10-104 0.28 6.34 98.73 44 1747 941 JL-10-108 0.41 4.03 99.93 15 915 913 JL-10-113 0.21 1.84 99.74 77 220 566 JL-10-119 0.30 4.78 99.76 30 690 1027 Sample Zr Nb Y V Ni Cu Co Pb Zn Th U Blue Mountain Granodiorite JL-09-024 136 7 7 32 10 17 39 2 90 5 1 JL-09-057 118 7 8 22 4 108 53 2 13 7 2 JL-10-139 122 5 7 38 6 394 46 1 32 4 1 7020-101 126 5 7 28 5 506 57 1 20 5 1 7012-130 148 5 6 24 7 30 40 3 63 4 1 7003-295 146 5 6 25 7 9 23 1 27 4 1 Landry Brook pluton JL-09-020 293 15 11 8 1 3 54 3 21 16 3 JL-09-030 314 15 24 8 1 9 60 15 34 19 4 JL-09-037 346 21 33 55 3 3 44 6 34 17 5 JL-09-072 395 23 36 53 2 2 58 7 23 19 4 JL-10-077 336 20 30 44 4 4 60 15 42 15 6 JL-10-081 319 19 33 58 3 2 59 16 78 16 4 JL-09-086 31 3 8 109 50 11 53 1 19 1 0 Dickie Brook pluton IL-09-202 453 27 55 8 0 4 57 6 56 10 5 JL-09-207 579 11 42 58 1 3 59 2 14 6 1 JL-09-209 657 28 49 8 0 4 50 4 61 10 3 JL-09-214 462 25 51 8 1 1 73 4 11 19 4 JL-09-220 413 27 52 8 0 2 72 7 28 17 5 JL-09-228 614 10 25 167 11 18 44 45 93 5 1 JL-09-229 125 9 16 311 4 27 55 5 23 2 1 JL-09 235 231 26 51 93 1 6 55 3 16 7 2 JL-10-304 289 23 40 310 6 43 51 2 18 5 1 JL-10-311 197 9 21 83 2 0 33 1 5 10 3 JL-10-322 561 28 41 24 2 7 44 2 31 14 5 JL-10-373 371 22 53 192 3 10 48 6 38 8 3 JL-10-383 553 33 73 54 1 2 49 2 10 10 5 JL-10-386 399 25 51 8 2 1 70 4 17 16 4 Charlo Plutonic suite JL-10-006 286 25 49 122 2 8 33 4 97 10 3 JL-10-007 467 26 50 60 3 9 55 15 77 12 3 JL-10-019 496 26 47 51 4 9 35 8 61 15 4 JL-10-039 121 4 7 38 4 2 41 4 23 4 1 JL-10-058 231 17 31 8 1 2 95 12 26 23 6 JL-10-060 130 73 73 8 1 1 45 5 51 15 7 JL-10-092 225 15 38 8 1 2 48 3 29 21 8 JL-10-093 110 20 42 8 0 2 55 38 170 26 7 JL-10-094 105 21 45 8 0 0 65 1 15 20 8 JL-10-104 176 13 26 275 52 34 51 2 77 2 1 JL-10-108 276 15 32 172 34 23 48 2 72 2 1 JL-10-113 350 16 47 32 1 9 42 8 61 12 3 JL-10-119 247 23 27 144 20 22 37 5 61 5 2 Notes: Analyses were done by X-ray Fluorescence for major oxides and ICP-MS for trace elements at the ACME Laboratory in Vancouver, British Columbia, Canada. Anaiytical error is generally less than 5% for major element and 2-10% for trace elements. [Fe.sub.2][0.sub.3] is total Fe as [Fe.sub.2][O.sub.3]. LOI is loss on ignition at 1000[degrees]C. Appendix 3. Rare earth element, Hi, and Ta data * from the Blue Mountain Granodiorite, Landry Brook and Dickie Brook plutons, and Charlo plutonic suite. Sample La Ce Pr Nd Sm Eu Gd Blue Mountain Granodiorite JL-09-024 20.4 38.9 4.22 16.1 2.33 0.73 1.75 JL-09-057 21.8 41.9 4.35 16.2 2.44 0.59 1.72 JL-10-139 13.4 25.2 2.80 10.6 1.87 0.65 1.49 7020-101 23.2 45.0 4.66 16.4 2.48 0.66 1.66 7012-130 23.6 46.8 4.75 17.3 2.39 0.70 1.59 7003-295 21.1 41.3 4.22 15.3 2.28 0.69 1.48 Landry Brook pluton JL-09-020 11.8 42.1 2.83 10.9 1.94 0.33 1.42 JL-09-030 28.1 59.0 5.94 21.6 3.86 0.68 3.34 JL-09-037 36.4 76.4 8.47 32.5 5.94 1.28 5.37 JL-09-072 42.4 91.0 9.67 37.0 6.57 1.28 5.91 JL-10-077 36.0 74.5 8.17 31.5 5.71 1.23 4.90 IL-10-081 40.5 78.3 9.10 35.1 6.37 1.34 5.63 JL-09-086 5.0 10.8 1.43 6.6 1.43 0.75 1.64 Dickie Brook pluton JL-09-202 39.8 93.2 11.00 47.1 9.25 2.33 9.40 JL-09-207 21.4 52.1 7.11 33.7 7.41 2.96 7.89 JL-09-209 35.4 79.5 9.59 41.3 8.20 2.54 7.82 JL 09-214 16.6 52.1 7.83 34.7 7.69 1.33 7.74 JL-09-220-1 44.8 96.4 11.08 45.0 8.54 1.20 8.01 JL-09-228 14.8 32.9 4.19 18.3 4.12 1.40 4.31 JL-09-229 10.6 23.3 2.82 12.3 2.74 1.29 2.94 IL-09-235 37.1 79.9 9.97 42.4 8.79 2.67 9.20 JL-10-304 22.6 51.3 6.63 29.9 6.78 1.97 7.45 JL-10-311 14.9 34.1 3.78 14.8 3.27 0.84 3.35 JL-10-322 53.3 110.2 11.95 46.1 7.86 1.91 6.95 JL-10-373 34.1 81.6 10.02 44.2 9.33 2.47 9.71 JL-10-383 49.1 137.6 16.91 70.7 14.12 3.91 13.72 JL-10-386 25.6 66.0 9.15 40.3 8.12 1.36 7.95 Charlo Plutonlc suite JL-10-006 37.6 85.3 10.48 46.0 9.00 2.41 9.10 JL-10-007 43.6 97.4 11.57 47.8 9.17 2.12 8.91 IL-10-019 46.0 100.7 11.86 49.0 9.09 1.71 8.45 JL-10-039 15.2 28.4 3.30 13.0 2.15 0.63 1.56 JL-10-058 45.0 79.1 9.13 33.7 6.31 0.64 5.68 JL-10-060 1.0 20.8 0.64 3.4 2.78 0.23 5.79 IL-10-092 24.5 50.3 5.61 21.9 4.02 0.45 4.43 JL-10-093 34.0 66.5 7.84 30.6 7.14 0.27 7.29 JL-10-094 4.4 31.0 1.12 4.3 1.64 0.10 3.19 JL-10-104 14.3 35.0 4.54 22.2 4.52 1.50 4.86 JL-10-108 22.0 54.1 7.02 31.1 6.37 2.13 6.46 JL-10-113 36.8 80.7 9.44 39.2 7.61 1.84 7.58 JL-10-119 23.1 52.9 6.38 27.9 5.46 1.61 5.32 Sample Tb Dy Ho Er Tm Yb Lu Hf Blue Mountain Granodiorite JL-09-024 0.27 1.37 0.23 0.62 0.10 0.61 0.08 3.6 JL-09-057 0.27 1.38 0.25 0.70 0.11 0.72 0.10 3.3 JL-10-139 0.23 1.18 0.22 0.59 0.09 0.58 0.09 3.1 7020-101 0.23 1.13 0.21 0.58 0.08 0.56 0.09 3.2 7012-130 0.23 1.12 0.19 0.54 0.08 0.51 0.07 3.5 7003-295 0.22 1.14 0.21 0.51 0.07 0.50 0.07 3.4 Landry Brook pluton JL-09-020 0.30 1.92 0.43 1.49 0.26 1.82 0.29 7.0 JL-09-030 0.61 3.71 0.78 2.43 0.40 2.51 0.40 8.3 JL-09-037 0.95 5.49 1.11 3.37 0.54 3.52 0.54 9.1 JL-09-072 1.04 6.04 1.25 3.71 0.61 3.81 0.57 10.1 JL-10-077 0.87 5.06 1.04 3.06 0.49 3.20 0.48 8.6 IL-10-081 0.98 5.60 1.12 3.28 0.52 3.32 0.48 8.2 JL-09-086 0.27 1.51 0.29 0.77 0.13 0.73 0.10 0.9 Dickie Brook pluton JL-09-202 1.63 9.65 1.97 5.75 0.91 5.70 0.87 10.7 JL-09-207 1.30 7.37 1.49 4.23 0.64 3.95 0.58 11.5 JL-09-209 1.38 8.29 1.72 5.14 0.82 5.34 0.85 14.7 JL 09-214 1.37 8.55 1.69 5.12 0.82 5.46 0.85 11.8 JL-09-220-1 1.44 8.38 1.76 5.30 0.84 5.52 0.83 11.1 JL-09-228 0.71 4.15 0.86 2.61 0.38 2.65 0.41 13.3 JL-09-229 0.50 2.94 0.57 1.67 0.23 1.60 0.22 3.2 IL-09-235 1.50 8.86 1.75 5.01 0.75 4.83 0.71 5.9 JL-10-304 1.24 7.33 1.48 4.00 0.56 3.90 0.55 6.8 JL-10-311 0.59 3.67 0.73 2.15 0.34 2.30 0.35 5.1 JL-10-322 1.20 7.17 1.39 4.20 0.65 4.53 0.70 12.5 JL-10-373 1.60 9.64 1.92 5.52 81 5.34 0.79 9.7 JL-10-383 2.32 13.84 2.74 7.81 1.12 7.50 1.05 12.7 JL-10-386 1.40 8.57 1.78 5.32 0.79 5.37 0.78 10.1 Charlo Plutonlc suite JL-10-006 1.50 8.83 1.74 5.06 0.76 4.68 0.69 8.0 JL-10-007 1.50 8.73 1.74 5.14 0.80 4.85 0.75 11.8 IL-10-019 1.43 8.33 1.66 4.93 0.77 4.92 0.74 12.4 JL-10-039 0.24 1.23 0.23 0.64 0.09 0.58 0.08 3.4 JL-10-058 0.97 533 1.04 3.01 0.49 3.23 0.47 7.3 JL-10-060 1.50 10.61 2.35 7.72 1.32 8.48 1.23 7.7 IL-10-092 0.92 5.82 1.27 4.03 0.64 4.12 0.62 7.4 JL-10-093 1.28 7.50 1.52 4.55 0.71 4.58 0.67 4.9 JL-10-094 0.94 7.01 1.56 4.91 0.78 5.01 0.72 4.9 JL-10-104 0.81 4.93 0.94 2.71 0.42 2.63 0.38 4.4 JL-10-108 1.03 5.94 1.14 3.18 0.48 2.94 0.43 6.0 JL-10-113 1.31 7.95 1.62 4.91 0.79 5.02 0.74 9.6 JL-10-119 0.86 4.90 0.94 2.76 0.40 2.53 0.37 5.7 Sample Ta Blue Mountain Granodiorite JL-09-024 0.8 JL-09-057 1.2 JL-10-139 0.9 7020-101 0.9 7012-130 0.8 7003-295 0.6 Landry Brook pluton JL-09-020 1.9 JL-09-030 2.1 JL-09-037 2.1 JL-09-072 2.4 JL-10-077 2.1 IL-10-081 1.8 JL-09-086 0.4 Dickie Brook pluton JL-09-202 2.1 JL-09-207 1.1 JL-09-209 2.2 JL 09-214 2.4 JL-09-220-1 2.5 JL-09-228 1.0 JL-09-229 0.9 IL-09-235 1.8 JL-10-304 1.6 JL-10-311 0.9 JL-10-322 2.3 JL-10-373 1.8 JL-10-383 2.3 JL-10-386 2.1 Charlo Plutonlc suite JL-10-006 1.8 JL-10-007 1.9 IL-10-019 2.1 JL-10-039 0.7 JL-10-058 2.5 JL-10-060 7.8 IL-10-092 1.9 JL-10-093 2.7 JL-10-094 2.4 JL-10-104 0.9 JL-10-108 1.0 JL-10-113 1.5 JL-10-119 1.6 * Analyses at ACME Laboratory in Vancouver, British Columbia, Canada, using ICP-MS.
This paper results from a M.Sc. thesis by J-L. Pilote at Acadia University. We thank journal reviewers J. B. Whalen and L.R. Fyffe for their helpful comments and suggestions. Funding and logistical support were provided by the New Brunswick Department of Natural Resources, a Research Grant to J-L. Pilote from the Geological Society of America, and Discovery Grant to S.M. Barr from the Natural Sciences and Engineering Research Council of Canada.
Date received: 19 April 2012 [paragraph] Date accepted: 02 July 2012
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Editorial responsibility: David P. West
JEAN-LUC PILOTE (1) *, SANDRA M. BARR (1), REGINALD A. WILSON (2), SEAN MCCLENAGHAN (2), SANDRA KAMO (3), VICKI J. MCNICOLE (4), AND MARY LOU BEVIER (5)
(1.) Department of Earth and Environmental Science, Acadia University, Wolfville, Nova Scotia, B4P 2R6 Canada
(2.) Geological Surveys Branch, New Brunswick Department of Natural Resources, Bathurst, New Brunswick, E2A 3Z1 Canada
(3.) Jack Satterly Geochronology Laboratory, Department of Geology, University of Toronto, Toronto, Ontario, M5S 3B1 Canada
(4.) Geological Survey of Canada, Ottawa, Ontario, K1A 0E4 Canada
(5.) Department of Earth and Ocean Sciences, The University of British Columbia, Vancouver, British Columbia, V6T 1Z4 Canada
* Corresponding author: <email@example.com>
Table 1. U-Pb isotopic data for chemically abraded single zircon grains from samples 97-DL-04, LB00-1, MLNB-733, and 09SHM BR-50. Pb Sample Weight U Pbtol (a) Pb Th/U (b) (c) ([micro]g) (ppm) (pg) (ppm) (pg) 97 DL-04 A 61 127 -- 8 -- 3 BI 70 140 -- 9 -- 5 B2 40 138 -- 9 -- 4 C 64 155 -- 10 -- 8 LBO0-1 1 55 100 -- 6.9 0.46 0.4 2 5.0 177 -- 12.5 0.54 0.4 3 2.7 164 -- 115 0.51 0.6 4 4.7 92 -- 6.4 0.50 0.3 MLNB-733 A 25 272 -- 19 -- 18 B 13 406 -- 29 -- 43 C 16 279 -- 19 -- 17 09SHM-BR-50 1 6.3 108 47 -- 0.52 0.5 2 2.6 16i 29 -- 0.47 0.9 3 2.1 157 22 -- 0.41 1.4 4 3.1 104 22 -- 0.42 0.7 Sample [sup.206] Pb/ [sup.206]Pb/ 2[sigma] [sup.204] Pb (d) [sup.238]U (e) measured 97 DL-04 A 9982 0.06415 0.00006 BI 8468 0.06409 0.00005 B2 5498 0.06521 0.00006 C 4949 0.06417 0.00005 LBO0-1 1 5661 0.067307 0.000068 2 10119 0.067262 0.000072 3 3401 0.067222 0.000062 4 5780 0.067134 0.000421 MLNB-733 A 1525 0.06693 0.00007 B 527 0.06708 0.00008 C 1112 0.06706 0.00007 09SHM-BR-50 1 6007 0.06693 0.00007 2 2099 0.06707 0.00013 3 1053 0.06706 0.00014 4 2097 0.06744 0.00014 Sample [sup.207]Pb/[sup.235]U 2[sigma] (e) 97 DL-04 A 0.4833 0.0005 BI 0.4838 0.0005 B2 0.4976 0.0005 C 0.4818 0.0005 LBO0-1 1 0.5134 0.0015 2 0.5121 0.0013 3 0.5135 0.0022 4 0.5112 0.0035 MLNB-733 A 0.50876 0.00094 B 0.51027 0.00174 C 0.51246 0.00115 09SHM-BR-50 1 0.5103 0.0018 2 0.5111 0.0037 3 0.5i01 0.0058 4 0.5131 0.0034 Sample [sup.206]Pb/[sup.238]U 2[sigma] Age (Ma) 97 DL-04 A 400.8 0.7 BI 400.5 0.6 B2 407.3 0.7 C 4110.9 0.6 LBO0-1 1 419.91 0.41 2 419.64 0.43 3 419.40 0.38 4 418.87 2.54 MLNB-733 A 417.6 0.8 B 418.6 1.0 C 418.4 0.8 09SHM-BR-50 1 417.61 0.78 2 418.45 0.81 3 418.45 0.83 4 420.73 0.83 Sample [sup.207]Pb/[sup.235]U 2[sigma] Age (Ma) 97 DL-04 A 400.3 0.7 BI 400.6 0.7 B2 410.1 0.7 C 401.3 0.7 LBO0-1 1 420.7 1.0 2 419.9 0.9 3 420.8 1.4 4 419.3 2.3 MLNB-733 A 417.6 1.3 B 418.6 2.3 C 420.1 1.5 09SHM-BR-50 1 418.6 1.2 2 419.2 2.5 3 418.5 3.9 4 420.6 2.3 Sample [sup.207]Pb/[sup.206]Pb 2[sigma] %Disc Error Age (Ma) (f) Corr (g) 97 DL-04 A 397.8 2.0 -0.8 0.900 BI 401.7 1.8 0.3 0.924 B2 426.1 2.3 4.6 0.879 C 403.9 1.9 0.8 0.914 LBO0-1 1 425.2 5.4 1.3 0.669 2 421.3 4.3 0.4 0.714 3 428.5 8.3 2.2 0.608 4 421.6 5.0 0.7 0.944 MLNB-733 A 417.5 5.8 0.0 0.732 B 419.1 12.1 0.1 0.684 C 429.3 7.9 2.6 0.655 09SHM-BR-50 1 424 1 1.6 11692 2 423 14 1.1 0.519 3 419 23 0.1 0.510 4 420 13 -0.3 0.526 Notes (a) Pblot is total amount of Pb exclding blank. (b) Th-U calculated from radiogenic [sup.208]Pb-[sup.206] Pb ratin and [sup.207]Pb-[sup.206]Pb age assuming concordance. Correction for [sup.230]. Th disequilibrium in 206/238 and 207/206 assuming Th-U of 4,2 in the magma, (c) PbC is total common Pb (assuming isotopic composition of laboratory blank for zircon and for titamite using Stacey and Kramers (1975) for intial Pb in excess of blank): laboratory Pb isotopic composition 206/204: 18.221; 207/204: 15.612; 208/204 39.360; 2[sigma] errors of 1% (d) Measured ratio for spike and fractionation only. (e) Pb-U ratio are corrected for fractionation, common Pb in the spike, and blank, (f) Disc is percent discordance for the given [sup.207] Pb-[sup.206]Pb age. (g) Error Corr is correlation coefficients of X-Y errors on the concardia plot. Decay constants are those of Jaffey et al. (1971).
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|Author:||Pilote, Jean-Luc; Barr, Sandra M.; Wilson, Reginald A.; McClenaghan, Sean; Kamo, Sandra; McNicoll, V|
|Date:||Jan 1, 2012|
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