New U-Pb (zircon) age and geochemistry of the Wedgeport pluton, Meguma terrane, Nova Scotia

MacLean, Natalie; Barr, Sandra; White, Chris; Ketchum, John

INTRODUCTION

The Wedgeport pluton in southernmost Nova Scotia differs in both age and composition from the abundant Devonian plu-tons that characterize the Meguma terrane (Fig. 1). Its specialized characteristics were recognized in the Nova Scotia "granite boom" of the late 1970s and early 1980s, when the poorly exposed pluton was extensively explored and drilled for Sn, W, and U (Cant et al. 1978; Wolfson 1983). Subsequently, the pluton was reported to be signiﬁcantly younger than the other plutons of the Meguma terrane, with a late Carboniferous UPb (zircon) and Rb-Sr whole rock age of 316 ± 5 and 323 ± 12 Ma, respectively (Cormier et al. 1988). This age is similar to some ⁴⁰Ar/³⁹Ar ages from mica in plutonic and metasedimentary units and shear zones in the area (e.g., Reynolds et al. 1981, 1987; Dallmeyer and Keppie 1987, 1988; Muecke et al. 1988; Keppie and Dallmeyer 1995; Culshaw and Reynolds 1997). The pluton also yielded younger ⁴⁰Ar/³⁹Ar biotite and Rb-Sr mineral ages of ca. 257 Ma (Reynolds et al. 1981; Cormier et al. 1988), which, together with the inferred crystallization age, were used to suggest that Permian-Carboniferous plutonism was a signiﬁcant factor for economic mineralization in the Meguma Terrane (Cormier et al. 1988). It was suggested more recently that emplacement of the Wedgeport pluton may have been linked to extension related to delamination (Keppie and Dallmeyer 1995) or transtension along shear zones as a result of relative motion of the Gondwanan and Laurentian plates (Pe-Piper and Jansa 1999).

The Southwest Nova Mapping Project (White 2003) provided an opportunity to revisit the Wedgeport pluton with detailed mapping and sampling, which was used as the basis for a BSc honours thesis project by the senior author. Furthermore, the previously reported U-Pb (zircon) age was based on a single bulk zircon fraction and thus is not reliable by current standards; hence, the opportunity was also taken to re-date the pluton. The purpose of this paper is to report the results of these studies, together with a compilation of some earlier work on the pluton. The results show that the pluton is older than was indicated by previous dating, but still younger than other granitoid rocks of the Meguma terrane.

GEOLOGICAL SETTING

The Wedgeport pluton (Taylor 1967) intrudes thickly bedded metasandstone, metasiltstone, and slate of the New Harbour Member, the lower part of the Goldenville Formation (White and King 2002; White 2003) (Figs. 1, 2). The Goldenville Formation is overlain by the mainly pelitic Halifax Formation. In the Yarmouth area west of the Wedgeport pluton (Fig. 1), metavolcanic and metasedimentary rocks of the late Ordovician to Silurian White Rock Formation disconformably overlie or are in faulted contact with the Halifax Formation (MacDonald et al. 2002; White et al. 2001). These units were deformed and metamorphosed during the Acadian orogeny at ca. 395– 380 Ma (Hicks et al. 1999), prior to emplacement of the South Mountain Batholith and related plutons at ca. 378– 372 Ma (see Clarke et al. 1997 for a summary). The Meguma terrane was juxtaposed with the Avalon terrane to the north by Devonian-Carboniferous dextral transcurrent motion along the Cobequid-Chedabucto fault system (e.g., Keppie 2000). Mantle-derived maﬁc igneous activity in the Middle Devonian to Carboniferous may have provided the heat source to generate these granitoid magmas by crustal melting (Tate and Clarke 1995). Ongoing localized deformation occurred along shear zones during the Carboniferous (Culshaw and Liesa 1997; Culshaw and Reynolds 1997).

FIELD RELATIONS

Although the Wedgeport pluton is poorly exposed and outcrop is sporadic, second derivative aeromagnetic data (King 1997a, b, and unpublished data) combined with several drill holes (Cant et al. 1978) clarify the position of the contact in areas of limited or no outcrop. The pluton intruded along the western limb of a north-south-trending, north-plunging anticline (Fig. 2). It produced a narrow (approximately 400 m wide) contact metamorphic aureole of spotted hornfels containing andalusite and cordierite superimposed on biotite zone assemblages (Cullen 1983). Abundant garnet also was noted during the present study in the more pelitic beds in the metasandstone. The contact metamorphic mineral assemblage is indicative of the albite-epidote to hornblende-hornfels facies, and indicates that the pluton was emplaced at relatively shallow crustal depth, about 3– 4 km below surface. The contact zone is well exposed on the western shore of Pinkneys Point (Fig. 2), where the metasedimentary rocks are intruded by granitic dykes from the pluton.

The mainly granitic pluton contains scattered ﬁne- to medium-grained, biotite-rich, round granodioritic enclaves that range in size from a few 10s of cm to 1– 2 m in longest dimension. None of the enclaves were included in the present study. Narrow (2– 5 cm wide, rarely > 1 m), pale grey veins and pods of aplite and pegmatite intrude the pluton. Near the margins of the pluton the granite is heterogeneous with textures that range from ﬁne-grained to porphyritic. In addition, igneous layering is present, deﬁned by alternating biotite-rich and feldspar-quartz-rich bands that are broadly parallel to the contact with the adjacent country rocks. Miarolitic cavities are present locally but are generally uncommon (Wolfson 1983). These textural variations suggest that a signiﬁcant amount of ﬂuid was present during crystallization of the pluton, especially near the margins.

The pluton and adjacent country rock are cut by several thin (1– 2 mm to several cm) quartz, quartz-tourmaline, quartz-carbonate, and greisen veins. Typically, the quartz-carbonate and greisen veins contain various sulphide minerals, ﬂuorite, scheelite, white mica, and cassiterite (Wolfson 1983). Northeast- to east-trending shear zones, reported to contain cassiterite, wolframite, molybdenite, and scheelite, cut the pluton, and appear rusty as the result of weathering of associated sulphide minerals, mainly pyrite and arsenopyrite (e.g., Wolfson, 1983). Mylonitic fabrics are common in the shear zones which display well-developed asymmetric quartz augen and C– S fabrics indicating dextral sense of motion (White 2003).

The pluton is cut by lamprophyre and alkaline olivine dia-base dykes of early Jurassic age (Cant et al. 1978; Chatterjee and Keppie 1981; Wolfson 1983; Pe-Piper and Reynolds 2000; White and King 2002; White 2003).

PETROGRAPHY

The Wedgeport pluton is composed mainly of medium- to coarse-grained biotite monzogranite which grades in composition to syenogranite (Fig. 3). Texture is typically hypidiomorphic equigranular and, locally, inequigranular to porphyritic, especially near the margins as described above. Microcline is the dominant feldspar, and simple Carlsbad twins are visible in some grains suggesting that orthoclase was the original form. Perthitic texture is typically present, and albitic lamellae have compositions similar to those of separate plagioclase grains in the rock. Granophyric texture occurs only in samples from the northwestern part of the intrusion; that area may represent the shallowest part at the time of emplacement. Subhedral plagioclase is slightly to extensively altered to saussurite and sericite. Microprobe analyses of plagioclase in 6 samples showed a range in composition from An1 to An17; zoned plagioclase grains do not greatly vary in composition from the core to the rim (MacLean 2003). Anhedral quartz grains commonly show undulatory extinction.

Biotite forms about 15% of the rock, and typically is partially or wholly altered to chlorite and muscovite. Microprobe analyses (MacLean 2003) revealed that the biotite has a high iron content (Fe/Fe+Mg = 0.73 to 0.83) and tetrahedral Al contents of 2 to 2.2, close to the annite end member. Common inclusions in biotite are titanite, zircon, apatite, ilmenite, epidote, and probably monazite (not easily identiﬁed because of small grain size). Titanite is the most abundant accessory mineral in the samples and mainly occurs in association with biotite and ilmenite; the latter mineral is partially or in some cases entirely altered to titanite. Many samples also contain minor amounts of garnet and ﬂuorite. Electron microprobe analyses revealed that the garnet is of almandine-grossular composition with high manganese content (MacLean 2003).

Chatterjee and Keppie (1981) and Chatterjee et al. (1985) divided the Wedgeport pluton into the Goose Bay and Pinkneys Point units, forming the eastern and western parts of the pluton, respectively, with the mutual contact not exposed. They described the Goose Bay granite as garnetiferous, and similar to parts of the South Mountain Batholith. In contrast, the Pinkneys Point granite was described as a more variable unit, containing topaz granite, greisenized granite, albitite, and greisen, and associated with mineralization, including cassiterite, wolframite, scheelite, and a variety of similar l ithophile-element minerals (Chatterjee et al. 1985). Chatterjee and Keppie (1981) suggested that the Pinkneys Point pluton may have been the source of ﬂuids that resulted in alteration and mineralized veins in the Wedgeport pluton and adjacent rocks. Observations made during the present study do not provide any evidence to support this subdivision; garnet was observed in samples distributed throughout the pluton, and features ascribed to the Pinkneys Point unit are more likely a reﬂection of the excellent exposure in the Pinkneys Point section and its position near the margin of the pluton.

GEOCHRONOLOGY

Previous Work

U-Pb and Rb-Sr data presented by Cormier et al. (1988) indicated that the Wedgeport pluton crystallized at 316 ± 5 Ma, but was reheated at 257 ± 8 Ma during a thermal event. However, the U-Pb data of Cormier et al. (1988) are difﬁcult to re-assess as no U isotopic information was provided and some aspects of the data are inconsistent between data table and text. Additionally, only one zircon fraction was analyzed, and presumably that fraction was large and multigrain. The zircon was reported to be of poor quality, and it is unlikely that it was air-abraded prior to analysis because at the time of the work, the abrasion technique (Krogh 1982) was not widely used.

An ⁴⁰Ar/³⁹Ar plateau age on biotite at 258 ± 8 Ma has also been reported from the Wedgeport pluton (Reynolds et al. 1981); however, this sample showed appreciable alteration of biotite to chlorite (Reynolds et al. 1981). The similarity between the Rb-Sr mineral isochron ages (Cormier et al. 1988) and the ⁴⁰Ar/³⁹Ar age from chloritized biotite suggests that both the Rb-Sr and ⁴⁰Ar/³⁹Ar systems may record the timing of pervasive alteration in the Wedgeport pluton as opposed to a re-heating event.

Even younger hornblende and biotite ⁴⁰Ar/³⁹Ar plateau ages (ca. 231 to 222 Ma and ca. 209 to 203 Ma) were reported for the lamprophyre and alkaline olivine diabase dykes that occur in the area (Reynolds et al. 1987; Pe-Piper and Reynolds 2000).

Analytical Methods

A 20 kg monzogranite sample was processed at the Royal Ontario Museum in Toronto using standard techniques, including heavy liquids and a Frantz magnetic separator for isolation of heavy mineral fractions. Zircon was selected from the least paramagnetic fraction by hand picking grains under a binocular microscope. All picked zircons were given an air abrasion treatment to eliminate cracked grains and remove exterior surfaces (Krogh 1982). Final selection of grains for analysis was then made. The weight of each fraction (consisting of one to four grains) was determined using an unpublished spreadsheet calculation that estimates fraction weights from photomicrograph measurements of individual zircons. Uncertainties on the estimated weights have not been calculated but are likely to be <30% in most cases. This uncertainty only affects the calculation of Pb and U concentrations and has no inﬂuence on age data.

The selected grains were washed in 4N and 7N HNO3 and then loaded into Teﬂon bombs with HF and a measured amount of ²⁰⁵Pb - ²³⁵U isotopic tracer solution (Krogh 1973). Dissolution occurred over four to ﬁve days at 195°C. No chemical isolation of U and Pb was carried out on the dissolved grains. Fractions were dried down with phosphoric acid and then loaded with silica gel onto out-gassed rhenium ﬁlaments. The isotopic compositions of Pb and U were measured using a single Daly collector with a pulse counting detector in a solid source VG354 mass spectrometer. A detector mass discrimination of 0.14% per atomic mass unit (AMU) and a dead time of 22.5 nsec were employed for Daly detector measurements. A thermal source mass discrimination correction of 0.1% per atomic mass unit for both Pb and U was also used.

Assigned laboratory blank for U is 0.2 pg. Total measured common Pb in each fraction was below 1 pg in all cases and was assigned the isotopic composition of lab blank (see footnotes to Table 1). Error estimates were calculated by propagating known sources of analytical uncertainty for each analysis including ratio variability (within run), uncertainty in the fractionation correction, and uncertainties in the isotopic composition of laboratory blank. Decay constants used are those of Jaffey et al. (1971). Uncertainties are given at the 95% conﬁdence level. Discordia lines and concordia intercept ages were calculated by the method of Davis (1982) using the in-house program ROMAGE. The average ²⁰⁶Pb/²³⁸U age reported below was also calculated using ROMAGE.

Table 1

**U-Pb isotopic data for Wedgeport pluton sample 016-W02-004A**

New Results

Zircon grains in the Wedgeport granite sample are dominated by euhedral, 4-sided, well-formed igneous prisms ranging from small to large (Fig. 4a, b). Most grains are cracked and/or contain inclusions but the selected grains are free of these features. Six fractions of small and large grains were abraded and analysed separately (Table 1). Fractions Z2, Z3, and Z5 are multigrain fractions of small prisms with inclusions. On the concordia diagram (Fig. 5), these analyses plot distinctly below and to the left of two concordant analyses (Z4, Z6) of larger single prisms. Fraction Z1, also a single large grain, is older than all other fractions. Although interpretation of these data is not straightforward, we consider the following scenario to be the most likely. Concordant fractions Z4 and Z6, with identical ²⁰⁶Pb/²³⁸U ages of 357 Ma, are interpreted to give the igneous crystallization age of the granite. The weighted mean ²⁰⁶Pb/²³⁸U age of these fractions is 357.3 ± 1.1 Ma. Fraction Z5 is interpreted to consist of ca. 357 Ma zircons that experienced some modern-day Pb loss, and fraction Z1 appears to contain an inherited component. The age of this component is modelled as 1340 +830/-500 Ma, the upper intercept age of a discordia line through fractions Z1, Z4, and Z6. The remaining fractions (Z2, Z3) have ²⁰⁷Pb/²⁰⁶Pb ages signiﬁcantly older than 357 Ma and therefore modern-day Pb loss alone cannot account for their discordance. We suggest that Pb loss combined with the presence of a minor inherited component best explains the discordance of these analyses.

We consider the weighted mean ²⁰⁶Pb/²³⁸U age of 357.3 ± 1.1 Ma to be the best estimate for the crystallization age of the Wedgeport pluton. The previously reported age of 316 ± 5 Ma (Cormier et al. 1988), which was based on a single analysis of highly fractured and metamict grains, may be erroneously young due to signiﬁcant Pb loss from these zircons.

GEOCHEMISTRY

Introduction

We acquired major and trace element data (Table 2) for 18 samples from surface outcrops of the Wedgeport pluton (Fig. 2). Rare-earth element data were obtained for 5 of these samples (Table 3), and Sm-Nd isotopic data for the dated sample (Table 4). Wolfson (1983) had reported whole-rock analyses of 8 samples from drill core in the Wedgeport pluton, but her data included only a limited suite of trace elements. Pe-Piper and Jansa (1999) also obtained chemical data from 7 samples from the pluton, in order to compare to offshore plutons sampled in drill core. Those data include a suite of trace elements and in two samples, also rare-earth elements, comparable to the present data set, although no petrographic descriptions were provided. Locations for these samples (G. Pe-Piper, written communication, 2004) are shown on Fig. 2. In addition, Chatterjee et al. (1985) presented a large amount of chemical data from the Wedgeport pluton in the form of variation diagrams; however, their focus was on mineralization processes, not petrogenesis and tectonic setting, and the actual chemical data for those samples were not published.

Table 2

**Table 2. Chemical data for samples from the Wedgeport pluton**

Table 3

**Table 3. Rare-earth element, Hf, and Ta data* for samples from the Wedgeport pluton**

Major and trace elements

All analyzed samples from the Wedgeport pluton have high silica content (Table 2) that averages about 75%. Although scattered, most major element oxides show a negative correlation with SiO2 (Fig. 6). Exceptions are Na2O and K2O (Fig. 6f, g) which show little or no correlation with SiO2. These variations mainly reﬂect variations in the amount of modal biotite and plagioclase in the analyzed samples. No consistent differences are apparent between samples that contain garnet compared to those that do not, or between the porphyritic sample and the other samples. The two aplite samples do not differ signiﬁcantly in major element composition from their host rocks. In terms of major element composition, the Wedgeport pluton does not show a clear afﬁnity with any of the average A-type and felsic I- and S-type granites of Whalen et al. (1987). For example, Na2O contents are similar to that in the average I-type but lower than in the average A-type and higher than in the average S-type (Fig. 6f), whereas MgO and CaO contents are most similar to the average A-type (Fig. 6d, e) and P2O5 content to the average S-type (Fig. 6h).

Trace elements show more diagnostic features (Fig. 7). Both Ba and Sr show negative correlation with SiO2, and concentrations below those typical of average felsic I- and S-type granite and most similar to average A-type (Figs. 7a, b). On the other hand, Rb values show no correlation with SiO2 and are elevated compared to all three granite types (Fig. 7c). This feature is also shown on the Ba-Rb-Sr ternary diagram (Fig. 8a), in which the samples plot in the area of enriched granite according to El Bouseily and El Sokkary (1975).

The trace elements Y, Nb, and Ga show scatter and no consistent correlation with SiO2 (Figs. 7d, e, f), whereas Zr shows a weak negative correlation (Fig. 7g). The abundances of all of these elements are below those of the average A-type granite, although they tend to be higher than those in the average felsic I- and S-type granites. V show strong negative correlation with SiO2, and higher values than I-, S-, and especially A-type granites (Fig. 7h). Values in the Pe-Piper and Jansa (1999) samples are uniformly lower than those obtained during the present study, most likely due to a systematic analytical problem in one of the data sets. Both Pb and Zn show negative correlation with SiO2 (Fig. 7i, j). Pb tends to be higher in samples that contain garnet, and Zn values are low compared to the average A-type granite. Concentrations of Ni, Cu, and Cr are low and commonly below the detection limit of the analytical method (Table 2), and hence are not displayed graphically.

Th and U values are scattered, but overall higher than those in the average felsic I-, S-, or A-type granites (Fig. 9a, b). A plot of Th against U shows a positive correlation (Fig.9c), and two trends are suggested that correspond to the "unaltered" (lower U) and "altered" (higher U) sample trends identiﬁed by Chatterjee et al. (1985). The majority of samples analyzed during the present study, as well as those of Pe-Piper and Jansa (1999), follow the "unaltered" trend.

Table 4

**Table 4. New Sm-Nd isotopic data for sample 016-WO2-04A from the Wedgeport pluton**

The Wedgeport pluton is not easily assigned to I-, S-, or A-type on the basis of major or trace element compositions compared to the averages from Whalen et al. (1987). Whalen et al. (1987) used the Ga/Al ratio as a distinguishing feature of these granite types, and plots of Na2O+K2O and Nb against Ga/Al suggest a composition intermediate between A-type and felsic I- and S-type granites (Fig. 8b, c). However, the presence of iron-rich biotite and abundant titanite and ﬂuorite are more consistent with A-type character. A plot of Al2O3 / Na2O + K2O against Al2O3 / CaO + Na2O + K2O shows that the Wedgeport pluton is peraluminous (Fig. 8d). Other peraluminous characteristics of the Wedgeport pluton include the presence of garnet in many samples.

The samples plot at the junction of the within-plate, syncollisional, and volcanic-arc granitoid ﬁelds on the Rb against Y+Nb discrimination diagram (Fig. 8e) but more deﬁnitively in the A-type ﬁeld on the Nb-Y diagram (Fig. 8f).

Rare-Earth Element Data

Rare-earth element (REE) data were obtained for 5 samples (four granite and one aplite) during the present study (Table 3), and an additional two samples are available from Pe-Piper and Jansa (1999). The patterns for all of the granite samples are similar, and show moderate enrichment in the light REE, a large negative Eu anomaly, and a ﬂat heavy REE at 20 to 40 times chondritic values (Fig. 10). The aplite sample shows a strongly contrasting pattern, with no enrichment in the light REE and increasing enrichment in the heavy REE. No obvious mineralogical differences such as high garnet content are evident in the aplite to explain the REE pattern.

Isotopic Data

The Sm-Nd data for the dated sample 016-WO2-004A (Table 4) are similar to those reported for two samples by Pe-Piper and Jansa (1999). The εNd value at 357 Ma is 2.1, whereas the two samples from Pe-Piper and Jansa (1999) have values (at 357 Ma) of 2.1 and 3.1. These relatively high positive values contrast markedly with reported εNd values for other granitic plutons in the Meguma terrane, which have negative values ranging from -1.4 to -5.2 at 372 Ma (Clarke et al. 1988). The positive values in the Wedgeport pluton samples suggest a relatively primitive source and allow for little contamination from the metasedimentary host rocks of the Meguma Group, which have very negative εNd values of ca. -10 (Clarke et al. 1988). Instead, they are similar to values from minor maﬁc plutons of the Meguma terrane, for which mainly positive values have been reported (Tate and Clarke 1995). They are also similar to values reported by MacDonald et al. (2002) for ca. 440 Ma rhyolite in the White Rock Formation in the Yarmouth area (εNd = 1.37), although the ca. 440 Ma Brenton pluton has a lower value (εNd = -0.42).

DISCUSSION AND CONCLUSIONS

The revised age reported here for the Wedgeport pluton shows that it is 40 million years older than previously assumed, that is earliest Carboniferous (Okulitch 2002) as opposed to late Carboniferous. Hence the pluton cannot be associated with the late thermal events at ca. 320– 315 Ma in the Meguma terrane, nor with the shear zones of late Carboniferous age, as suggested by previous workers (Dallmeyer and Keppie 1987; Keppie and Dallmeyer 1995; Culshaw and Reynolds 1997; see compilation in White 2003).

The 357 ±1 Ma age is signiﬁcantly younger than the ages from the South Mountain Batholith and its satellite plutons, Shelburne and Barrington Passage (Fig. 1), all of which have yielded ca. 372 Ma ages. It is also much younger than the nearby Brenton Pluton (Fig. 1), which is Silurian (MacDonald et al. 2002). No other igneous activity of ca. 357 Ma is known in the Meguma terrane, although abundant plutons of similar age occur north of the Cobequid - Chedabucto fault system in northern mainland Nova Scotia (Dunning et al. 2002). However, the latter plutons differ from the Wedgeport pluton in that they are part of bimodal gabbro-granite suites with clear A-type features, and occur in association with voluminous bimodal volcanic rocks. Pe-Piper and Jansa (1999) compared offshore plutons with onshore plutons, including the Wedgeport pluton, and showed that none of the offshore plutons has petrochemical characteristics that match those of the Wedgeport pluton.

A possible link may exist between the Wedgeport pluton and mineralization in spodumene-bearing pegmatite bodies in the Brazil Lake area north of the Wedgeport pluton (Fig. 1). Pegmatite in this area occurs as elongate lenses in deformed metavolcanic and metasedimentary rocks of the Silurian White Rock Formation. Although U-Pb dating of tantalite indicated that the pegmatite crystallized at 378 ± 1 Ma, molybdenite from an adjacent quartz vein yielded a Re/Os age of 354 ± 3 Ma (Kontak et al. 2003). This result indicates that mineralization in the Brazil Lake area is of similar age to the crystallization age of the Wedgeport pluton. Although it does not prove a genetic link between the two areas, the similar ages, younger than ages of other plutons known in the Meguma terrane, may be signiﬁcant.

In addition to its anomalous age, the Wedgeport pluton also has anomalous petrochemical characteristics. It cannot be classiﬁed as any of the commonly accepted granite end-members, and its tectonic setting is not evident from its petrochemical features using commonly applied discrimination diagrams. However, a within-plate tectonic setting is most likely, both from the petrochemical features and the inferred tectonic situation of the Meguma terrane in the earliest Carboniferous. At that time, the Meguma terrane was being uplifted and unroofed, and shedding sedimentary material into Carboniferous basins. The northwestern part of the South Mountain Batholith was exposed by 357 Ma when the Wedgeport pluton was being emplaced, as conglomerate in the overlying units contains debris derived from the batholith. However, it is clear that the area around the Wedgeport pluton was still buried. The depth of emplacement of the Wedgeport pluton was likely epizonal, based on the presence of a well-developed contact metamorphic aureole containing cordierite and andalusite, and localized development of porphyritic, granophyric, and inequigranular textures near the margins.

The Wedgeport pluton appears to be a unique intrusion in the Meguma terrane, both in terms of its age and its composition, and remains an enigma in terms of its origin.

New U-Pb (zircon) age and geochemistry of the Wedgeport pluton, Meguma terrane, Nova Scotia

ABSTRACT

RÉSUMÉ

INTRODUCTION

GEOLOGICAL SETTING

FIELD RELATIONS

PETROGRAPHY