Hard Rock Spodumene Lithium Deposit

Report of Activities 2003 41

Geology of the Southern Lobe of the Brazil Lake
LCT-type Pegmatite (NTS 21A/04), Yarmouth
County, Nova Scotia
D. J. Kontak

Introduction initiated during the summer of 2003. This report
presents the preliminary findings of this work. In
addition, initial results of an integrated
Rare-element pegmatites are important resources
geochronological study are presented and, for the
for their economic concentrations of rare elements
first time, an absolute age constraint on the time of
(e.g. Sn, Li, Ta, Rb, Cs, etc.), presence of high-
emplacement of the pegmatite is provided. This age
quality industrial minerals (e.g. muscovite,
has important implications, not only for the
spodumene, feldspar, mica), and occurrence of gem
petrogenesis of the Bazil Lake pegmatite, but also
minerals (e.g. tourmaline, beryl). LCT-type
for exploration in this part of the Meguma Terrane.
pegmatites are rare-element pegmatites enriched in
Li, Cs and Ta, and are often related petro-
genetically to fertile, progenitor granites (see Summary of Previous Work
Černý, 1991a, for classification of pegmatites).
Examples of LCT pegmatites that are currently Two separate lobes of pegmatite are currently
mined include the Tanco pegmatite (Li, Ta, Cs, Be, exposed in the Brazil Lake pegmatite. These lobes
Rb) of Manitoba, the Bikita (Li) and Kamativi (Li, are referred to informally as the northern and
Sn) pegmatites of Zimbabwe, the giant southern pegmatites, with reference to their
Greenbushes pegmatite (Sn, Ta, Nb, Li) of western location to the Holly Road (Fig. 2a). The Brazil
Australia, and the spodumene pegmatites of North Lake pegmatite was discovered in 1960 when a
Carolina. Although spodumene-bearing pegmatites spodumene-bearing pegmatite boulder was found
occur elsewhere in the Appalachians (e.g. Kings beside the Brazil Lake - Pleasant Valley Road (i.e.
Mountain, North Carolina, and Peg Claims, the Holly Road). Subsequent stripping of outcrops
Maine), the Brazil Lake pegmatite (BLP) is at in the area revealed the presence of pegmatite north
present the only known occurrence in Nova Scotia. and south of the road. The first map of the area,
indicating the distribution of pegmatite bodies, was
The occurrence of spodumene and associated produced by Taylor (1967), who also provided a
columbite-tantalite in the Brazil Lake area of modal analysis from an exposure of the southern
southwestern Nova Scotia (Fig. 1a, b) has been outcrop (52% feldspar (K-feldspar and albite), 34%
known since 1960 (Taylor, 1967), but the quartz, 11% spodumene, 3% muscovite, minor to
occurrence has attracted only limited and sporadic trace beryl, apatite, and tourmaline). Metallurgical
work (see below) until recently. A more extensive work done on a 272 kg sample of spodumene-rich
program of drilling and stripping in 2002 by (34.4% modally) pegmatite indicated 0.18-
Champlain Resources Inc. exposed a large amount 0.3 wt. % Fe2O3 in the spodumene. Shell Canada
of pegmatite that was previously unknown. Work Ltd. evaluated the site with mapping, geophysics
to date indicates that this pegmatite has the and geochemical sampling, and found variable, but
potential to produce high-quality feldspar, quartz, elevated levels of Li (<275 ppm), Rb (<190 ppm),
mica and spodumene with appreciable grades of Cs (<100 ppm), Sn (<177 ppm) and Ta (<95 ppm)
tantalum (D. Black, personal communication, (Palma et al., 1982). A mineralogical study was
2003). In order to assess this resource, develop a done on four representative samples from outcrops
model for its petrogenesis, and assess the potential south of the Holly Road by Hutchinson (1982),
of the surrounding area, a detailed mapping collected as part of the Shell Canada Ltd.
program, with follow-up petrological studies, was exploration program. Significantly, Hutchinson

Kontak, D. J. 2004: in Mineral Resources Branch, Report of
Activities 2003; Nova Scotia Department of Natural Resources,
Report 2004-1, p. 41-68.

42 Mineral Resources Branch

Figure 1. (A) Regional geological map of southern Nova Scotia showing the location of the study area (Fig. 1B
inset). (B) Geological map of southwest Nova Scotia (after White et al., 2001) showing location of Brazil Lake
pegmatite (BRZ) and the East Kemptville tin deposit (EK).


Figure 2. (A) Geological setting of the Brazil Lake pegmatites with reference to the Holly Road (map
modified after map of D. Black, Champlain Resources Inc., 2003). The pegmatites located north and
south of the Holly Road are referred to informally as the northern and southern pegmatites, respectively.
(B) Geological setting of the southern pegmatite, Brazil Lake.


(1982) recognized a metasomatic halo about the was obtained for the volcanic rocks (MacDonald et
Brazil Lake pegmitite, revealed by the conspicuous al., 2002). The Breton pluton, a probable
presence of tourmaline in the quartzite and the rare subvolcanic intrusion related to the White Rock
occurrence of the Li-bearing amphibole Formation based on its chemistry (MacDonald et
homquistite, generally diagnostic of nearby Li- al., 2002) and 439 Ma U/Pb zircon age (Keppie and
bearing pegmatite (e.g. London, 1986a). Krough, 2000), is in fault contact with both the
White Rock and Halifax formations. The intrusion
MacDonald et al. (1992) conducted a is highly deformed and corresponds composition-
geochemical study over the pegmatite area in order ally to a biotite-muscovite syenogranite to
to evaluate the signature of this deposit within the monzogranite. Within the intrusion are two mica-
surficial environment, including the vegetation. bearing, garnet-tourmaline pegmatites that
Corey (1993) drilled the northern pegmatite as part commonly cut the fabric of the granite.
of a larger program undertaken by the Nova Scotia
Department of Natural Resources, and concluded Deformation in the area occurred during the
that it was a single, zoned, sub-vertical dyke of 10- Acadian Orogeny and produced northeast-trending,
25 m thickness. Sampling and analysis of this core upright folds with a shallow southwest plunge and
by Gwalia Resources of Australia in 2002 provided a related penetrative fabric. An overprinting,
the first extensive geochemical data set (see probably Alleghanian age fabric (Culshaw and
below). Hughes (1995) provided a more Reynolds, 1997), crenulates the S1 fabric and the
comprehensive petrological investigation of the fold axis is gently south-southeast plunging (White
northern pegmatite that included mineral chemical et al., 2001). The metamorphic facies varies from
data, recognition of new minerals, the first fluid greenschist to amphibolite, with higher facies
inclusion observations and data, and a modern localized to the contact area between the White
petrogenetic model. Rock and Goldenville formations on the south side
of the Yarmouth Syncline (MacDonald, 2000).
Geological Setting This also coincides with a boundary between two
distinct trends of vertical gradient magnetics, which
O’Reilly et al. (1992) termed the Deerfield Shear
The study area is located in the southwestern end of
Zone.
the province, just past the western extent of the
380 Ma, peraluminous South Mountain Batholith
In the area of the BLP, the host rocks are a
(SMB), and roughly 25 km from the past-
northeast-trending sequence of folded meta-
producing (1985-1992) East Kemptville tin deposit
volcanics and metasediments of the White Rock
(Fig. 1b). The Brazil Lake area is underlain by a
Formation that fall in the middle of the Yarmouth
mixed package of metasedimentary and
Syncline (Fig. 1b). Rock types include fine- to
metavolcanic rocks, which are cut by small
coarse-grained amphibolite, minor mafic tuff, dark
pegmatite bodies, and the Brenton Pluton, which is
green-black pelite, psammite and a fine-grained,
also transected by pegmatites. The oldest rocks are
tourmaline-bearing, silica-rich rock adjacent to the
part of the Cambro-Ordovician Meguma Group,
pegmatite. The pelitic unit typically contains
which consists of an older, sandstone-dominant
staurolite, garnet and andalusite, whereas
Goldenville Formation, and younger, overlying
tourmaline occurs in the amphibolite adjacent to
siltstone and shale-dominant rocks of the Halifax
the pegmatite (thin section observation). In
Formation. Overlying the Meguma Group are
addition, elliptical, buff-colored plagioclase clots,
mixed sedimentary and volcanic rocks of the
with steep lineations, occur in amphibolite near the
Silurian White Rock Formation. The sedimentary
pegmatite. The silica-rich nature of the quartzite
stratigraphy is dominated by massive quartzite with
may be primary or, in part, an exomorphic
minor pelitic beds. The volcanic rocks are of
alteration (i.e. silicification) related to pegmatite
basaltic composition, although west of the study
emplacement (D. Black, personal communication,
area near Yarmouth felsic rocks also occur (White
2003).
et al., 2001). A recent U/Pb zircon age of 438 Ma


Geology of the Brazil Lake Geology of the Southern
Pegmatite Pegmatite

The Brazil Lake pegmatite consists of two distinct Stripping of the southern pegmatite in 2002
sheets that occur south and north of the Holly Road provided complete exposure of this unit and it was
(Fig. 2a), referred to informally as the northern and mapped in detail in 2003 (Figs. 3, 4). Below is a
southern pegmatites. Previously, the few scattered summary of findings resulting from this mapping.
outcrops of these pegmatites that represent their The northern pegmatite is scheduled to be stripped
surface expression were mapped by Hutchinson in 2004 and will be subsequently mapped in detail.
(1982) and Hughes (1996), respectively.
Essentially, both these workers recognized three Wallrocks
zones within the BLP that were characterized by
modal enrichment in spodumene, K-feldspar (KF) The immediate wallrock consists of an interbedded
and albite (their aplitic albite). The southern sequence of mafic volcanics (amphibolites), pelitic
pegmatite is dominated by zones of megacrystic schist, and quartzite. There is no apparent structural
blocky K-feldspar (BKF), spodumene (Spd), fine- continuity between the pegmatite and wallrocks,
grained albite, and coarse-grained pegmatite the contact is a zone of faulting or shearing. The
composed of variable proportions of Spd-KF- sequence strikes northeastwards and dips steeply to
quartz. Further subdivisions can be made based on the northwest. Adjacent to the pegmatite, all three
textures, grain size and mineral proportions. rock types are found due to the fact that the
Subdivision of the BLP compared in general with pegmatite is oblique to the strike of the beds.
that observed in albite-spodumene rare-element Within the amphibolitic rocks occur thin, beige
pegmatites, which are otherwise generally ellipses, ca. 0.5-1 cm long, of plagioclase
characterized by a heterogeneous and complex aggregates that are oriented subvertical in the
internal structure (Černý, 1991a). cleavage plane. Along the margin of the pegmatite
occur tourmaline-rich (i.e. 40-50%) xenoliths of
The pegmatites are steeply-dipping sheets (i.e. altered amphibolite; tourmaline grains are <1-2 cm
75-80° SE) of 10-20 m width that strike north- long. In thin section tourmaline locally comprises
easterly at ca. 30-40°. Although the pegmatites lie 10-20% of the mode of amphibolite adjacent to the
within the White Rock Formation, they obliquely pegmatite. The quartzite beds locally lose their buff
crosscut bedding, such that they are in direct colour adjacent to the pegmatite, as noted above,
contact with quartzite, pelitic schist and which may relate to silicification. Chemical
amphibolite along their strike length. In the analysis of these rocks indicates up to 98.5% SiO2
quartzite unit marginal to the pegmatite, tourmaline (D. Black, personal communication, 2003). No
occurs disseminated as isolated grains or megascopic change is noted in pelitic beds adjacent
aggregates, often with radial habit and rarely to the pegmatite.
exceeding 3-5%. The overall dimensions of this
zone remain to be defined as part of future work. Zoning in the Southern Pegmatite
There is no regional structure that the BLP appears
to have accessed during emplacement, and contacts There is a distinct development of zones within the
between pegmatite and wallrock are welded with southern pegmatite that permits mapping out areas
no apparent structural discontinuity or locus of that are characterized by a dominant mineral or
subsequent displacement. On strike and southwest texture, and these are discussed below. It should be
of the southern pegmatite is a recently exposed emphasized that some variability may occur in such
quarry that does not contain pegmatite; thus, the zones, but in general one zone can be easily
southern pegmatite body either plunges to the distinguished from a contrasting zone. These zones
southwest beneath these exposures, pinches out, or (Figs. 3, 4) are dominated by blocky K-feldspar or
is faulted off. their albitized equivalents, spodumene-rich areas,


Figure 3. Detailed geological maps of outcrops comprising the southern pegmatite (see Fig. 2 for location). Figure 3A
shows the location of the outcrops and in Figures 3B and C are the detailed geological features of these pegmatitic
outcrops.


Figure 4. Detailed geological map of part of the southern pegmatite. See Figure 2B for location of the outcrop and
Figure 3 for the legend.

coarse matrix pegmatite, and a beaded quartz- albitized (Fig. 6b). These large megacrysts are
textured zone. subhedral to euhedral (compare Figs. 6a to e) and
are generally inclusion free on a macroscopic scale.
Marginal or Contact Zone Although zones may be dominated by K-feldspar,
There is no well-developed, continuous wall zone they may also contain variable amounts of quartz
to the southern pegmatite. Wall zones consisting of and spodumene (e.g. Figs. 6a, e). The BKF crystals
fine-grained granite or aplite are common in other vary from equant to elongate and, in the latter case,
zoned rare-element pegmatites (e.g. Černý, 1991a; the long axis is oriented perpendicular to the
Simmons et al., 2003). However, locally within contact (Fig. 6c). Where the K-feldspar has an
1 m of the contact there is a marked decrease in the elliptical shape (e.g. Fig. 6b), the outline may
grain size and euhedral spodumene oriented reflect post-crystallization modification due to
perpendicular to the contact is surrounded by superimposed stress, which is not uncommon in
smaller quartz euhedra within an aplite matrix pegmatites (Černý, 1991a). The BKF zone varies
(Fig. 5). The mineralogy of this matrix is presently from greyish, representing the freshest material, to
undetermined. Elsewhere the contact zone may various hues of pinkish-red, and white where
become more siliceous, as seen along the altered to fine-grained albite. On fresh surfaces the
southwestern contact where both the abundance K-feldspar contains a flame perthite texture.
and grain size of quartz increases (Figs. 3c, 8g).
Although there may be alignment of quartz and Intergrown with the BKF zones may be coarse
spodumene subparallel to the contact (Fig. 4), this (<10-15 cm) quartz of anhedral elliptical shape to
contrasts markedly with the general orientation of euhedral grains (Figs. 6a, 8c). Where this type of
megacrystic K-feldspar and spodumene quartz coalesces and becomes continuous, the term
perpendicular to the contact elsewhere (Figs. 3b, c, beaded quartz texture (BQT) is used to describe the
6c, e). feature and it can be mapped within the pegmatite
(Figs. 3, 4, 6b, d). Thus, there is a continuum
Blocky K-feldspar (BKF) Zones between BKF and BQT zones. In addition, there is
Zones of BKF, with individual crystals of <1.5 m a continuum between BQT zones dominated by
(Figs. 6a, c, e), occur throughout the pegmatite quartz, and more polymineralic (i.e. quartz±
(Figs. 3b, c), but in the northeastern end such zones muscovite±spodumene±feldspar) areas where the
are rarely preserved and, instead, have been proportions of minerals vary. In these areas the


Figure 5. Outcrop photos of border zone, southern pegmatite, Brazil Lake. (A) Spodumene megacrysts in upper right
bordered by smaller spodumene crystals in matrix of fine-grained, sacchroidal-textured aplite/albite with quartz grains.
Note that the long dimension of the spodumene crystals are oriented perpendicular to the contact (lower left).
(B) Enlargement of part of Figure 5A showing intergranular material between spodumene megacrysts. Note the quartz
grains that are growing with their c-axis perpendicular to the spodumene crystals. (C) Close up of wall zone texture
showing the euhedral, translucent quartz grains in the fine-grained aplitic material.


BKF is often replaced by either fine-grained subdivided into several ellipitical subzones by the
sacchroidal albite or cleavelandite (Figs. 6b, f, g). Cut BQT material. Internally these albite zones may
slabs of this K-feldspar indicate that the albitization develop into coarser albite (cleavelandite) and also
process is controlled by fractures (Fig. 6a inset) that have a vuggy texture with 1-2 cm pockets lined
gradually coalesce to form massive albite, and further with clear euhedra of albite and quartz. In one
alteration may result in the fine-grained albite exceptional case where this was observed, a zone
becoming cleavelandite (Fig. 6f). of coarse, primary BKF is overgrown by a layer of
comb quartz and radial albite (?), which is
Spodumene Zones succeeded by a zone of fine-grained albite and then
Spodumene-rich zones are dominated by megacrystic a distinct vuggy zone dominated by secondary fine-
spodumene that reaches is maximum size (i.e. <1.5- grained albite and cleavelandite.
2 m) in the central part of the pegmatite and
diminishes in grain size toward the margin (<0.5 m) The vuggy albite-rich zone is dominated by
(Figs. 7a, b, f). One particularly spodumene-rich zone fine-grained albite, but locally a variety of quartz
is observed along the southeastern part of one of the types occur along with concentrations of coarse,
exposed outcrops where the spodumene defines a clear to light brownish and silvery mica. The quartz
distinct fabric (Fig. 3c). Where the megacrysts of occurs in the following manner: (1) elliptical to
spodumene are preferentially oriented, their long axis rounded, anhedral aggregates (?) of clear to dark
generally lies perpendicular to the contact zone grey quartz in a sea of albite, and (2) as millimetre
(Figs. 3, 4, 7b, f), although internally more random to centimetre euhedra within multi-centimetre size
orientations occur. Spodumene is often intergrown vugs.
with BKF as subparallel grains oriented
perpendicular to the contact (Fig. 6a) and penetrating In thin section the albite zone is >98% albite
grains (Figs. 6e, 7c, d). The megacrysts of with minor residual K-feldspar and accessory
spodumene are euhedral and inclusion free, except amblygonite, white mica, Ta-Nb oxides, garnet,
for subhedral to euhedral quartz along their margins. triplite, cassiterite and zeolite (identified to date).
The pods of spodumene consist of several The albite is subhedral to euhedral, is free of
interlocking grains of different size with minor mineral inclusions, albite twinned and
amounts of intergranular quartz (euhedral to exceptionally fresh. Albite crystals are
anhedral), feldspar (K-feldspar or albite), finer- preferentially aligned, but not strained. Thus,
grained spodumene, and muscovite (Fig. 7f). In some thermal annealing of the albite outlasted any stress
cases, quartz grains are oriented perpendicular to that may have been responsible for the orientation
spodumene, as if the grains had acted as a site of of albite. Accessory phases are subhedral to
nucleation for quartz (Fig. 5c). The spodumene is euhedral and are preferentially concentrated in
rarely deformed, but rare cases of kinking have been zones, perhaps reflecting fracture-controlled fluid
observed. migration. Zeolite occurs as the latest stage
accessory mineral and occurs alone along fractures.
Albite Zones The texture of the K-feldspar is described in detail
Large areas (many square metres) of pegmatite below.
contain fine-grained albite after primary BKF (see
above and Fig. 6b). The occurrence of residual K- Intergranular Zones
feldspar as irregular-shaped, multi-centimetre The areas between megacrystic spodumene and
crystals is the evidence for this replacement (Fig. 6g), BKF, including albitized zones, consist of coarse-
along with the presence of albite lining fractures that grained (<20-30 cm), intergrown quartz,
transect BKF where the albitization process was spodumene, feldspar (K-feldspar or albite) and
arrested (inset Fig. 6a). These albite zones are muscovite, in varying proportions (e.g. Fig. 8a).
massive, have a sacchroidal texture, and may contain For purposes of this general description, the
disseminated apatite and shiny dark phases that material is referred to as coarse leucogranite (lcgr)
include tantalite and dark brown cassiterite. As and may include the beaded quartz texture material
already noted above, the zones are generally (Fig. 6b) described previously. Textures in the


leucogranite zones are variable, and include: (<2-3 cm) tourmaline. In thin section they are
(1) delicate intergrowths of quartz and cleavelandite uniformly dark brown to slightly zoned.
(secondary albite; Fig. 8b), (2) anhedral to euhedral
quartz in fine-grained albite (after K-feldspar,
Fig. 8e, f), (3) coarse cleavelandite-spodumene,
Mineralogy and Mineral
(4) coarse books of muscovite intergrown with quartz Chemistry of the Southern
±feldspar± spodumene, and (5) coarse euhedral Pegmatite
intergrowth of quartz-feldspar between metre-size
spodumene (Fig. 7g). A detailed evaluation of the mineralogy and
mineral chemistry of the pegmatite is currently in
This leucrogranite material also includes large progress. A preliminary assessment is presented
areas that are not dominated by BKF or spodumene below. Major and minor element analyses were
megacrysts and, instead, consists of coarse determined using wet chemical methods (DalTech,
leucogranite and is referred to as matrix in Figures 3 Halifax) and electron microprobe analysis (EMPA;
and 4. Such material is best seen along the western Dalhousie University Earth Science Department),
side of the outcrop shown in Figure 3c, where there is whereas trace elements were determined by ICP-
a distinct enrichment in quartz, in places including MS (Memorial University, Newfoundland).
intergrowth of quartz and euhedral K-feldspar. Such Imaging of mineral phases and qualitative analyses
an area may be a candidate for the best estimate of of some minerals were also done using the electron
the primary bulk composition of the pegmatitic melt. microprobe with an energy dispersive operating
system. The mineralogy can be subdivided into
White Mica Zone primary and secondary stages; the first represents
There are no zones of significant size that are formation during the magmatic stage, whereas the
dominated by white mica, such that they can be latter is of hydrothermal origin. There is a
mapped out. Instead, mica occurs as pods replacing continuum in formation of some minerals (e.g.
parts of BKF, disseminated within albitized zones, apatite) such that it is difficult to distinguish
and intergrown with coarse leucogranite zones as primary and secondary origins. As is the case for
both primary and secondary phases. Thus, although other minerals (e.g. K-feldspar) their texture and
there is some primary mica as part of the leucogranite chemistry is a mixture of primary and secondary
intergranular zones, the majority of the mica is stages.
secondary in origin.

Wallrock Inclusions Major Mineral Phases
Xenoliths of wallrock amphibolite occur as small to
medium size (<1 m) inclusions within the marginal K-feldspar
parts of the pegmatite. The xenoliths may contain
abundant, black to dark brownish, coarse-grained This was the most dominant mineral phase in the

Figure 6. (next page) Outcrop photos showing features of K-feldspar (KF), along with some spodumene (Spd) in
southern pegmatite, Brazil Lake. Knife for scale is ca. 10 cm long. (A) Megacrysts of fresh KF in blocky KF zone; note
the subhedral to euhedral outlines of the megacrysts. Dark material between the KF are quartz-rich areas, in part with
beaded quartz texture (BQT). Inset photo is cut slab of a partially altered KF showing albite invading along fractures.
(B) Blocky KF zone with intergranular quartz with the BQT. Note that the white color of the KF is due to partial to
complete replacement by fine-grained albite. Inset photo shows close up of the BQT, which consists of euhedral quartz,
muscovite books, and minor Spd here. (C) Oriented KF and Spd megacrysts near contact of the pegmatite (lower part of
photo). (D) Blocky KF zone with megacrysts of KF. Inset photo shows a mushroom-shaped KF with zonally arranged
quartz grains around it. Note the BQT in the background. (E) Large KF megacryst intergrown with Spd and oriented
perpendicular to pegmatite contact. Note that the KF is in contact with translucent quartz on left side with euhedral faces
(see inset). The KF is whitish here because of alteration to albite that includes both fine-grained sacchroidal albite and
euhedral cleavelandite. (F) Close up of previous area in Figure 6E showing albitized KF, secondary cleavelandite, and
porous texture of the feldspar that was generated during alteration. (G) Close up of albitized KF megacryst with residual
patches of KF (marked KF).


Figure 7. Outcrop photos showing features of spodumene (Spd) in southern pegmatite, Brazil Lake. Knife scale
ca. 10 cm long. (A, B) Outcrop dominated by Spd megacrysts oriented perpendicular to contact of pegmatite.
(C) Intergrowth of Spd and blocky K-feldspar (KF) at contact between zones enriched in these minerals. (D) Spd
crystals penetrating KF megacryst, which is now albitized. (E) Intergrowth of Spd and quartz in beaded quartz texture
zone between KF megacrysts. (F) Spd-rich zone at margin of pegmatite with blocky KF zone on top of it. Note that the
Spd is oriented perpendicular to the contact. Box outlines area enlarged in next photo. (G) Close up of intergranular
material between Spd megacrysts consisting of subhedral to euhedral quartz with albite and cleavelandite after earlier
KF. (H) Close up of Spd against cleavelandite in albitized zone showing that the Spd was not affected by the
metasomatism.


pegmatite prior to sodium metasomatism, which Mg mica (i.e. chlorite phase). Traces of Fe, Cr, Ni
converted much K-feldspar to sacchroidal albite and Cu phases, either as native elements or oxides,
and cleavelandite. However, remnant areas of fresh occur in the porous-textured areas (Fig. 11l). This
K-feldspar remain, particularly in the southwestern type of mineralization is common in pegmatites
part of the study area where BKF domains of beige and reflects a lack of sulphur in the melts and fluid
to light orange occur. Cut slabs of this K-feldspar (Černý, 1991b).
show perthitic textures with minor albite, consistent
with bulk analysis (n=4) of Or70-80Ab30-20 (Fig. 9a) Spodumene
and a minimal An component (<0.02 wt. % CaO).
These bulk analyses are similar to bulk Spodumene is present as a very pure phase with
compositions of K-feldspar from leucogranite- megacrysts rarely containing mineral inclusions,
hosted pegmatites of the South Mountain Batholith although small quartz euhedra (<l cm) locally occur
and suggest primary compositions (Fig. 9b; Kontak along margins of grains. Spodumene has a glassy
et al., 1995). Trace element chemistry (n=4) of the lustre and can be transparent; colours vary from
same K-feldspar separates indicates elevated Rb whitish, beige, grey-blue to green and, rarely, clear.
(3870 to 4870 ppm), but depleted Sr (17-75 ppm) Prized gem varieties such as kunzite, heddenite and
and Ba (32-190 ppm) contents. Similar triphane have not been observed. Where fractures
concentrations of these elements were also are present or deformation induced
obtained by Hughes (1995) for K-feldspar recrystallization, alteration to muscovite or a green
concentrates (n=4) from the northern pegmatite, phase (chlorite ?) is found. However, where
although he detected up to 5600 ppm Rb in one metasomatic albite occurs after K-feldspar, the
sample. Chondrite-normalized rare-earth element spodumene appears unaffected by the process
patterns are depleted compared to, for example, K- (Figs. 7d, h). Although few thin sections of
feldspar from pegmatites at East Kemptville and spodumene from the southern outcrop have been
the Brenton Pluton and compare, instead, to observed, it is noted that Hughes (1995) mentions
patterns for K-feldspar from pegmatites in the most that alteration of spodumene is common in the
evolved parts of the SMB (Fig. 10). Phosphorus northern pegmatite, with pseudomorphic
levels in the K-feldspar are low (<0.2 wt. % P2O5) replacement by albite, muscovite, K-feldspar,
and contrast with high levels (to 1.5 wt. %) in K- cookite, and chlorite. In addition, a spodumene-
feldspar from pegmatites of the SMB (Kontak et quartz intergrowth noted by Hughes (1995) has
al., 1995). also been observed in one sample, which may
represent spodumene-quartz intergrowth formed
Imaging of the freshest K-feldspar indicates after petalite (e.g. Černý and Ferguson, 1972).
typical flame perthite lamellae occur with no Compositions of spodumene approximate a pure
vestige of film perthite, as found, for example, in end member, with minor Fe at levels <0.3 wt. %
pegmatitic K-feldspar at Peggys Cove (Kontak et FeO and trace Mn (177 to 610 ppm) (Hughes,
al., 2002). Instead, coarser bleb perthite is more 1995).
common (Fig. 11a) and pitted textures are not
uncommon (Figs. 11a, b). Remnant patches of K- Quartz
feldspar in albite domains (i.e. metasomatic rocks)
are characterized by a very porous sieve texture Quartz varies considerably in its habit and colour
(Figs. 11b, c) and secondary apatite is common within the pegmatite. Rarely is it subhedral to
(Fig. 11b). In detail, the porous texture is seen to euhedral where intergrown with K-feldspar
consist of a network pattern with isolated domains (Fig. 6e) or as part of the BQT zones, but instead
of residual K-feldspar (Fig. 11c). The chemistry of anhedral forms are the most common and this is, in
the Or and Ab domains of K-feldspar indicates part, a result of post-crystallization deformation
equilibrated compositions of Or90-100 and Ab100, (Figs. 8d, e). Where fractured or brecciated, quartz
respectively (Fig. 9b), which reflect exchange is surrounded and invaded by cleavelandite, often
down to below 300°C. In rare cases such remnant with a comb or radial texture about the quartz, or
patches of K-feldspar are replaced by clay and Fe- intergrown with it, which suggests continued


crystallization. Although most quartz is translucent indicated trace amounts of Rb (10-65 ppm) and Sr
to transparent, colours range from cloudy white (13-175 ppm); other elements analyzed were at
through clear to black, with no consistent pattern very low levels (e.g. Li, Nb, Ta, Cs, Ba).
observed (Fig. 8), except that deformed quartz is
generally darker. No chemical analyses are Muscovite
available for quartz, but slabbed samples indicate
that micro-inclusions of apatite and Ta-Nb oxides Muscovite in the southern pegmatite is both of
are locally common. primary and secondary origin, based on its habit
and textural relationship with other phases. Primary
Albite muscovite is part of the beaded quartz texture or
leucrogranite zones that surround megacrysts of
Two varieties of albite occur, a fine-grained BKF, leucogranite around coarse spodumene, and
sacchroidal-textured type, and platy to acicular part of the coarse leucrogranite matrix. The
cleavelandite; both types are of Ab100 composition primary muscovite, estimated at <1% modally,
(Fig. 9). The former occurs as a replacement of occurs as coarse books <1-2 cm and is mostly light
blocky K-feldspar (Figs. 6b, g), which has a fabric brown to clear. In contrast, secondary muscovite is
defined by subparallel laths in thin section; this generally associated with albitized zones, either
fabric is inferred to be of syntectonic origin. In after BKF or in beaded quartz texture, or occurring
some cases the albite is crystal clear and lines as fracture coatings or veins <5-10 mm wide.
cavities in metasomatized BKF zones. Imaging Boulders of massive (i.e 80-90%) muscovite have
indicates the albite is clear to pitted in texture with been observed, but such material has not been seen
such grains adjacent each other (Figs. 11d, e) and in situ. The secondary muscovite is fine- to coarse-
often they terminate within voids (Fig. 11d). The grained, and may be silvery, brown, clear or green.
albite also contains disseminated euhedra of apatite
(Figs. 11d, e). Cleavelandite occurs as euhedral to Muscovite is close to its end member in
subhedral grains in a variety of settings that composition, with minor Fe (to 1.0 wt. % FeO) and
represent various types of metasomatism: Na (to 0.4 wt. % Na2O), as seen in the ternary
(1) replacement, either along linear to irregular (M2+-Al-Si) plot of Monier and Robert (1986;
fractures cross-cutting K-feldspar megacrysts Fig. 12). Compositions for a variety of textural
(Fig. 6f), (2) patches within or entirely replacing K- types are all similar and suggest high temperature
feldspar, and (3) intergrown with quartz as part of (i.e. 600°C) equilibration, regardless of
intergranular areas to coarse spodumene or K- paragenesis. Bulk analysis of muscovite from
feldspar. All types of albite generally contain massive pods of the same material (n=3) indicates
disseminated fine-grained apatite and Nb-Ta high abundances of Rb (3000-4600 ppm), Nb (120-
oxides, and slabbed samples of the massive albite 160 ppm), and Ta (211-61 ppm). Hutchinson
indicate that in some cases these minerals can be (1982) also noted high contents of Rb in muscovite
abundant. Chemical analysis of two albite pods from the northern pegmatite.

Figure 8. (next page) Outcrop photos showing features of quartz in Brazil Lake pegmatite. Knife scale ca. 10 cm long.
(A) Close up of the beaded quartz texture (BQT) developed between blocky K-feldspar (KF) megacrysts. The quartz is
intergrown with spodumene and albite (after KF). (B) Translucent quartz intergrown with secondary cleavelandite. Note
the penetrating nature of some cleavelandite crystals (circled) and euhedral outline of the quartz (dashed line). (C,
D) Megacryst of quartz among blocky KF. This quartz is typically dark grey to black in color and has a jig saw pattern
possibly due to autobrecciation, as highlighted by the outline in dashed white line. Note that albite occurs as part of the
intergranular matrix and some cleavelandite is developed that is intergrown with the quartz. (E) Anhedral quartz
disseminated within mixture of fine-grained albite and acicular cleavelandite after KF megacryst (slightly darker areas
are patches of orange KF). Inset shows possible autobrecciated quartz grain. (F) Similar feature as in previous photo,
but here there is apatite intergrown with the angular quartz grains and in the fine-grained albite. (G) Intergrowth of
coarse smoky quartz and euhedral KF in quartz-rich part of pegmatite near contact. (H) Intergrowth of quartz and albite
(after KF) in intergranular matrix to Spd megacrysts. Some of the quartz grains have been traced to show the variation in
habit from euhedral to anhedral(where ruptured) with albite filling what was once open space between the quartz grains.


Accessory Minerals
Accessory mineral phases include tourmaline,
apatite, garnet, beryl, chlorite, Ta-Nb oxides,
carbonate, triplite, amblygonite, cassiterite,
wolframite, sphalerite, zeolite, zircon, epidote, clay
and a variety of phosphate phases. The chemistry
and distribution of these phases are currently being
studied; only some of the minerals are discussed
here and a more complete description of these
phases is in preparation.

Tourmaline occurs as brown-black to green-
brown and dark blue, centimetre-size euhedra
within altered wallrock inclusions (i.e.
amphibolites) along the margin of the pegmatite
and also as smaller grains (<0.5 mm) in
amphibolites adjacent to the pegmatite. The grains
are both homogeneous or complexly zoned.
Preliminary analysis of pegmatite-hosted
tourmaline indicates dravite-schorl compositions
with some extreme Fe enrichment noted (Fig. 13).
Trends of the chemical data are typical of
pegmatitic tourmaline originating from
contamination due to pegmatite-host rock
interaction (Fig. 13; Tindle et al., 2002). Hughes
(1995) has also identified elbaite and indicolite
(Na+Li type) in the northern pegmatite.

Garnet occurs as multi-centimetre, subhedral to
euhedral grains within albite-rich zones, with or
Figure 9. Electron microprobe (circles) and bulk
without secondary muscovite. The garnet often has analysis (triangles) of feldspar phases in Brazil Lake
subgrain development due to fracture-related pegmatite plotted in ternary (Ca-Na-K) and binary (Na-
deformation. Several grains have been analyzed K) diagrams. Note that it is the cationic proportions,
(this study and Hughes, 1995) revealing a uniform based on 8 oxygens per formula unit (pfu), that are
plotted in the diagrams. The range of KF in pegmatites
chemistry dominated by Fe and Mn with a general
in lcgr refers to samples from the South Mountain
composition of Alm20-28Spess72-80. Batholith, as discussed in the text.

Beryl crystals, either as isolated grains or in or disseminated in sacchroidal albite after BKF.
clusters, are clear to pale green, <3-4 cm in size, The smaller grains are also common along
and occur along the eastern side of the pegmatite. fractures in deformed quartz. Fine-grained apatite
No chemical data are yet available for the beryl. Of euhedra intergrown with albite may locally be
the grains observed, the internal fracturing and abundant (Fig. 11f) and are complexly zoned
faint green colour precludes their use as gem (inset in Fig. 11f). This apatite may be inclusion
material (B. Wilson, personal communication, rich, including carbonates and sulphides
2003). (Fig. 11g). Apatite also occurs along fractures and
fills voids in albite (Fig. 11h), and pitted textures
Apatite occurs as euhedral to anhedral macro- occur associated with a second generation, Mn-
(<1-2 cm) or micro-crystals (mm size) within rich apatite (Fig. 11i). Micrograins of euhedral to
leucogranite areas, intergrown with cleavelandite anhedral apatite occur as disseminations within


Figure 10. Chondrite-normalized rare-earth element diagrams for K-feldspar (KF) separates from southern pegmatite,
Brazil Lake. (A) Compiled data set for KF separates from the South Mountain Batholith (Kontak and Martin, 1997)
showing general decrease in REE with fractionation: Grd=granodiorite, Mzgr=monzogranite, Pmzgr=pegmatite in
monzogranite, Plcgr=pegmatite in leucogranite. (B) KF from Brazil Lake pegmatite compared to field for KF from East
Kemptville pegmatites (Kontak et al., 2001). Sample BRP-2001-2 is from the pegmatite in the Brenton Pluton and BRZ-
2003-21D is a duplicate of sample BRZ-2003-21.


K-feldsparr (Fig. 11b) and secondary albite, mineralization, and the origin of the Ta:Nb
(Fig. 11d) or along fractures in quartz and albite. variability.
Similar euhedral apatite crystals are also common
in pitted K-feldspar and albite (Fig. 11e). A complex group of phosphate phases
occurs, including montebrasite, goyazite,
Compositions of apatite vary considerably and crandallite, lithiophillite and fillowite. The most
grains may be homogeneous to complexly zoned common phase is montebrasite which occurs in
reflecting continued re-equilibration with a fluid. fine-grained sacchroidal albite as a subhedral to
The early, coarser-grained and subhedral to euhedral phase (Fig. 11k), but Hughes (1995)
euhedral apatite is generally Mn poor and contains also reports it within coarse K-feldspar. The
several wt. % Cl. In contrast, texturally late stage montebrasite has a uniform composition [LiAl
and finer-grained apatite, or apatite overgrowing PO4(OH)] and its F-rich equivalent, amblygonite,
earlier apatite (Fig. 11g, i), is enriched in Mn via has not been found in the pegmatite.
the substitution of MnXCa and up to 15-18 wt. % Montebrasite is invariably altered to crandallite
MnO occurs. The Mn-rich apatite is Cl deficient and then goyazite, which record the low
and, therefore, inferred to be hydroxylapatite. temperature (300°C) alteration of the precursor
Hughes (1995) reports the occurrence of phosphate phase. In some cases the montebrasite
fluorapatites with 4 wt. % F in albitic aplite zones. is also altered to an unidentified clay mineral
(Al-Si phase from EDS spectra).
Tantalite-columbite occurs within the albite-
rich zones, along fractures in quartz and in In a few rare cases, native elements and
leucogranite areas. Most of this oxide oxide phases of Fe, Cr, Ni and Cu were observed
mineralization shows a spatial association with in K-feldspar associated with secondary albite
albite, an observation that is supported by whole- (Fig. 11l). Determining the nature and origin of
rock chemistry discussed below. Chemical this material requires further work, but such
analysis of selected grains indicates highly variable phases are not uncommon in pegmatites due to
Ta:Nb ratios, although most are enriched in the lack of sulphur to combine with these
Nb>Ta. Grains vary from homogeneous to elements to form sulphide phases (Černý,
intricately zoned (Inset in Fig. 11j). Ongoing work 1991b).
is required to sort out the nature of this oxide

Figure 11. (next page) Electron microprobe images of samples from Brazil Lake pegmatite. All images except C and
L are back scattered electron(BSE) images where the higher the average atomic number of the phase the brighter it is
(e.g., see tantalite (T) in Fig. 11J hosted by albite). Images in C and L are secondary electron images (SEI) that reflect
the surface topography of samples (e.g., holes, defects, etc.). (A) K-feldspar (KF) host with albite blebs. The KF is
characterized by a pitted texture with intervening areas free of pits. (B) Residual grain of KF in albite (dark
background). Note the porous nature of the KF and presence of anhedral apatite grains (bright phases at bottom and
top) in it. Area in box enlarged in C. (C) SEI of part of KF in previous figure showing the ver porous texture of the grain
that relates to Na metasomatism of the KF. (D) Albite with pitted texture in places, disseminated grains of apatite
(bright phases), and euhedral grains that terminate in the open space. (E) Close up of albite with pitted texture with
rare apatite (Apt) filling the pores. (F) Apatite grains of euhedral to subhedral shape in albite. Note that there is
dissolution along the margins of some grains and in detail they contain micro-inclusions and are chemically
heterogeneous. Inset shows close up of apatite grain with large variation in Mn content (bright areas have up to 18 wt.
% MnO). (G) Close up of apatite grain from previous image showing inclusions of Fe-poor sphalerite (ZnS) and
carbonate (Mn-bearing) in Mn-poor apatite that is rimmed by Mn-rich apatite. (H) Apatite filling open space in albite
host. Note the euhedral terminations of the apatite indicating it once filled a void. Inset shows the apatite euhedra and
small inclusions of an Fe oxide phase. (I) Apatite grain of uniform composition with second generation Mn-bearing
apatite along fractures that are lined with pitted texture. (J) Albite hosting montebrasite (M), apatite (A) and tantalite
(T) phases. Inset diagram shows tantalite grain in high contrast mode to emphasize the zoning in Ta and Nb ratio.
(K) Close up of montebrasite grain in previous image to illustrate the secondary alteration of this phase to crandallite
(Cran), goyazite (Goy) and clay. Inset is enlargement of part of the big grain to show the secondary phases. (L) Chip
of KF with inclusions of albite blebs (Alb) and various mixtures of Fe, Ni, Cr oxides and Cu oxide phase. Note that only
minor amounts of S were detected in the analysis.


also shows a positive correlation with phosphorus.
(3) Enrichment of both Ta and Sn are associated
with increasing sodium abundance.
(4) There is no association of Rb with sodium (not
shown) or phosphorus enrichment. Instead, Rb is
strongly correlated with potassium and occurs in
either K-feldspar or muscovite based on the
mineral chemistry discussed above.

Structural Features of the
Southern Pegmatite
Detailed mapping of structural elements of the
pegmatite is incomplete, but a few pertinent
observations are noted.

(1) The overall features of the pegmatite indicate
that a single stage of open-space infilling occurred,
such that the pegmatitic melt was injected into a
dilatant zone in the host rocks. The orientation and
size of the megacrysts indicate a single dilation
event, rather than multiple injections of magma.
(2) Quartz megacrysts are often oval or elliptical,
but subhedral outlines may reflect the original
Figure 12. Electron microprobe analysis of muscovite shape of megacrysts (Fig. 8c). These grains were
from Brazil Lake pegmatite plotted in Monier and subsequently ruptured during deformation
Robert’s (1986) ternary diagram with isotherms.
(Figs. 8d, e) and, in certain cases, the subgrains
Abbreviations are Cel=celadonite, Ph=phengite,
Ms=muscovite, Ann=annite, Phl=phlogopite. have serrated or irregular outlines and the
intervening space is filled with oriented albite
grains (Fig. 8d). These textures suggest that
Whole-rock Chemistry pegmatitic melt was injected into an active shear
zone environment, and that the pegmatite was
A database of 250 whole-rock geochemical subjected to deformation prior to complete
analyses has been generated by Gwalia Resources crystallization.
of Australia and Champlain Resources Inc. (3) Shear zones oriented subparallel to the
Samples of 0.4-1.8 m long core intervals, although pegmatite-wallrock contact occur throughout and
the majority were about 1 m long, were assayed for are manifest by flattened quartz megacrysts, kinked
major and trace elements. Only some salient spodumene and shear fabrics in muscovite-rich
highlights of these data are discussed below; a areas. The fabric is generally oriented northeasterly
more detailed assessment of the results is in with a subvertical dip, and the kink folds have
preparation. The following points are noted with subvertical axes.
reference to Figures 14 and 15.
Age of the Brazil Lake
(1) As expected, there is a negative correlation of
both lithium and potassium with sodium. Pegmatite
(2) Both calcium and phosphorus show a positive
correlation with sodium, thus confirming the The age of the Brazil Lake pegmatite has
association of phosphates, in particular apatite, previously been constrained by field relationships,
with albite-rich zones. Manganese (not shown) with a maximum age equivalent to the host White


Figure 13. Electron microprobe analysis of tourmaline from Brazil Lake pegmatite in binary plots with fields for
tourmaline classification (after Tindle et al., 2002). The terms P-HR refers to pegmatite-host rock interaction and
reflects contamination. Circles are from this work and squares are from Hughes (1995).


Rock Formation and a minimum age being the time Although the SMB is located some 20-25 km from
of the deformation that affected the pegmatite. the Brazil Lake area, a distance considered to be
However, the presence of both Acadian and excessive for transport of a pegmatite melt from a
Alleghanian deformation in the region (White et fertile, progenitor granite (Baker, 1998), this does
al., 2001) makes it difficult to infer a minimum age not preclude the possibility that an unexposed
for the pegmatite. In order to resolve the absolute granite was the source. As noted by Černý (1991b),
age of pegmatite formation, samples from the there is no plausible model for rare-element
southern pegmatite were selected for U/Pb pegmatite genesis other than a magmatic one, thus
(tantalite), Re-Os (molybdenite) and Ar/Ar a granitic source is assumed and the 378 Ma age is
(muscovite) analysis. The results will be discussed very suggestive that granite underlies the Brazil
in detail elsewhere (Kontak et al., in prep.), thus Lake area. Relevant to this argument is the
only a summary is given below. presence of numerous tin and base metal showings
throughout the Meguma Group metasedimentary
Analysis of a single fraction of separated, rocks east of the study area (Chatterjee, 1983;
euhedral, columbite-tantalite grains disseminated Kontak et al., 1990) and on strike with the East
within an albite-spodumene-muscovite assemblage, Kemptville tin deposit. This mineralization likely
part of a blocky K-feldspar zone, yielded a originated in underlying granite, such as occurs at
concordant U/Pb age of 378 ± 1 Ma. Three Re-Os the Kempt Snare Lake (Soehl, 1988 ) and Duck
age determinations for various size fractions of Pond (Pitrie and Richardson, 1989) mineralized
molybdenite from wallrock quartzite on the centres. As noted by Dostal and Chatterjee (1995),
northwest side of the southern pegmatite yielded the Davis Lake Pluton of the SMB is strongly
ages of 351.7, 351.9 and 354.2 Ma (all ± 2.5 Ma). fractionated toward the west and the nature of
Finally, several Ar/Ar spot laser ages for a coarse, contours for a variety of elements (e.g. Rb, Li, F)
euhedral muscovite flake, of primary magmatic and ratios (e.g. K/Rb) suggests that there may be
origin, from a beaded quartz-textured zone gave highly-fractionated granitic phases beneath the
ages of 318 to 348 Ma, with the former from the veneer of sediments overlying the continuation of
rim and the latter from the core of the grain. this pluton, which fed the mineralization noted
above. Thus, it may also be possible that one of
The aforementioned ages indicate that the time these centres is also the fertile source of the Li-rich
of pegmatite formation is constrained by the U/Pb melt that gave rise to the Brazil Lake pegmatites.
tantalite age, which coincidently is similar to a U/
Pb age of 380 Ma for the nearby South Mountain P-T Conditions of Emplacement
Batholith (Kontak et al., 2003). The ca. 353 Ma
Re-Os molybdenum age is similar to a U/Pb age of
of the Brazil Lake Pegmatite
357 Ma for the Wedgeport Pluton south of
The pressure-temperature (P-T) conditions of
Yarmouth (White et al., 2004), whereas the Ar/Ar
pegmatite formation are relevant to petrogenetic
ages approximate the time of the Alleghanian
modeling of the Brazil Lake pegmatite. The
deformation in the area (e.g. Culshaw and
constraints imposed on P-T conditions are:
Reynolds, 1997).
(1) presence of primary muscovite in beaded quartz
texture material; (2) occurrence of primary
Discussion spodumene as the dominant sink for Li rather than
petalite or eucryptite. However, the presence of
Implications of the Age of rare spodumene-quartz intergrowth (this study and
Hughes, 1995) suggests that rare early
Pegmatite Formation crystallization of petalite may have occurred
locally, although alternate interpretations of this
The age reported here for the BLP is 378 Ma, texture are possible; (3) occurrence of aqueous
which is indistinguishable from the time of fluid inclusions in spodumene with homogenization
emplacement of the South Mountain Batholith temperatures of ≤315°C and salinities of 5 wt. %
(SMB) (Kontak et al., 2003; Carruzzo et al., 2004). equivalent NaCl (Hughes, 1995); (4) solidus of Li-


Figure 14. Whole-rock geochemical plots for pegmatite samples from Brazil Lake. See text for discussion.

rich felsic melt (Martin, 1983). Using the stability units in rare-element pegmatites is sometimes
of the phase assemblages and projecting the equivocal, but of economic interest because of the
isochore for a 5 wt. % equivalent NaCl fluid, an concentrations of Be, Li, Rb, Cs, Nb, Ta, Sn and U
estimated P-T path for emplacement and (London, 1990). In the case of the BLP, there is a
crystallization of the pegmatite is derived, which clear association of rare elements with sodic
indicates initial emplacement at ca. 3.5-4 kbar and enrichment (Figs. 8f, 14, 15). Whereas small
near 600°C, which is comparable to that inferred amounts of metasomatism are easily explained
for the spodumene-bearing Harding pegmatite, because of pseudomorphic replacement textures,
New Mexico (London, 1984). These conditions the large areas underlain by albite/cleavelandite or
compare to the estimated level of emplacement of mica are more equivocal since such textures are
the SMB of 3.5 kbar (Raeside and Mahoney, 1996) lacking, although Soviet geologists have long
and granite and pegmatite formation at the East argued for a metasomatic origin (e.g. Ginzburg,
Kemptville tin deposit of 3.5-4.0 kbar (Halter and 1960; Beus, 1960). As noted by others, the large
Williams-Jones, 1999; Kontak et al., 2001). Li-bearing minerals, in this case spodumene, often
project into these albite areas with no evidence of
Metasomatism (?) in the Brazil alteration (e.g. Figs. 8c, d). However, in these cases
the fact that such Li minerals provide the substrate
Lake Pegmatite for nucleation of coarse radiating cleavelandite, of
The origin of the voluminous albitic or mica-rich assumed magmatic origin, is used to argue for a


Figure 15. Whole-rock geochemical plots for pegmatite samples from Brazil Lake. See text for discussion.

late, residual magmatic origin for the spodumene, vapor saturation and the concomitant loss of boron
along with the coexisting quartz and mica (Jahns and other volatiles, which suddenly raises the
and Tuttle, 1963; Jahns and Burnham, 1969; solidus temperature of the residual melt and
London 1990). Although the petrological thereby promotes crystallization (i.e. boron quench
observations discussed above are interpreted to model, London, 1987). Upon crystallization of
favor a metasomatic origin for albite-rich zones in these melts, as bodies of albite ± mica and quartz,
the BLP, both sacchroidal albite and cleavelandite, the exsolved aqueous vapor phase, formed from the
an alternative model presented by London (1990) is elements not conserved by the crystalizing
discussed below. components, promotes the metasomatism of
adjacent areas. Formation of the exsolved vapor
London (1990) explains that the inferred late also results in extensive fracturing of the pegmatite,
alkali-sodic metasomatic units (e.g. albite-mica which leads to an open bimetasomatic exchange
zones) were related to formation of a late solution- between pegmatite and wallrock, as manifest, for
melt, as represented by silicate-rich fluid inclusions example, by the presence of exomorphic
found in pegmatites (e.g. London, 1986b, c). The tourmaline in the host rock.
sudden formation of ore-bearing albite-mica zones,
according to London (1990), occur due to sudden The origin of the extensive albitic zones in the


Brazil Lake pegmatite requires additional work to fertile granites underlie the metasedimentary
resolve; however, the presence of these zones is landscape, and that the Brazil Lake pegmatite is
emphasized for two reasons: (1) such zones destroy probably related to one of these fertile intrusions,
the blocky K-feldspar areas which, due to their as suggested for the pegmatite fields in the
high rubidium content, are a valued industrial Wodgina district of Australia (Sweetapple and
mineral; and (2) the albitic zones are enriched in Collins, 2002).
muscovite and also rare elements (e.g. Ta, Nb).
Thus, the recognition of such zones and their extent As discussed by London (1990), the absence of
is relevant to exploitation of these pegmatites and early phenocrystic phases in rare-element
future work will address this issue. pegmatites, including the BLP here, indicates that
the pegmatites were emplaced as already
Exploration Potential for Li-rich fractionated melts rather than evolving in situ. This
implies, therefore, that there should be an along-
Pegmatite in the Brazil Lake Area strike variation in the mineralogy and chemistry
that can be used as an exploration guide. Pegmatite
Exploration potential in the Brazil Lake area is
fields can be characterized by both unidirectional
inferred based on analogies with other rare-element
or concentric zonation; however, this zonation style
pegmatite fields globally, where numerous
can be discerned by using the mineralogy (e.g.
pegmatites occur over large areas, some with
beryl versus spodumene rich; Breaks and Moore,
considerable strike length (e.g. Černý, 1991b).
1992) and mineral chemistry (e.g., K/Rb, K/Cs of
Often these pegmatites are laterally zoned with
BKF; Černý et al., 1985) to define the type of
LCT types generally distal from the fertile granite
zonation. With such limited outcrop as
source, although the source is not always identified
characterizes the Brazil Lake area this approach
(e.g. Little Nahanni pegmatite field; Groat et al.,
could prove useful.
2003). Excellent examples of such fields occur in,
for example, the Superior Province of Canada
Finally, local control on the occurrence of the
(Breaks and Moore, 1992) and the Wodgina
Brazil Lake pegmatite remains unresolved.
pegmatite district of the Pilbara Craton of western
However, in many pegmatite fields, structure is
Australia (Sweetapple and Collins, 2002). This
considered to be a dominant feature controlling the
latter area, with some of the world’s largest
locus of intrusion (Černý, 1991b). Future work will
reserves of Ta (-Sn), is of particular relevance
focus on the regional geology and potential
because of many similarities between it and the
influence of a dominant structural feature that may
Brazil Lake pegmatite and evolved Davis Lake
have localized the pegmatitic melt. It is, therefore,
pluton of the South Mountain Batholith.
relevant to note that the mineralization at East
Kemptville lies within a regional shear zone (East
The occurrence of the highly-evolved and
Kemptville-East Dalhousie Fault Zone; Horne et
chemically-zoned Davis Lake Pluton (Dostal and
al., 1992) and greisen formation was structurally
Chatterjee, 1995) at the western end of the SMB,
controlled.
with all the attributes of a fertile granite related to
LCT pegmatite fields (Černý, 1991a), is considered
potentially significant. As already noted, there are References
numerous tin and base-metal occurrences between
the termination of this pluton and the BLP and a Beus, A. A. 1960: Geochemistry of beryllium and
semi-continuous boulder terrain of pegmatite float genetic types of beryllium deposits; Moscow,
(D. Black, personal communication, 2003). In Akakemii Nauk SSSR (in Russian); translated by
addition, along the western edge of the most L. R. Page, ed., 1967, W. E. Freeman, San
evolved part of the Davis Lake Pluton southwest of Francisco, 401 p.
the East Kemptville tin deposit, small centres of
Ta-Nb occur in coarse-grained, albite-topaz - rich Breaks, F. W. and Moore, J. M., Jr. 1992: The
rocks. Collectively, both the style and abundance of Ghost Lake batholith, Superior Province of
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