895
The Canadian Mineralogist
Vol. 50, pp. 895-912 (2012)
DOI : 10.3749/canmin.50.4.895
COMPOSITIONAL EVOLUTION OF ZONED TOURMALINE CRYSTALS
FROM POCKETS IN COMMON PEGMATITES OF THE MOLDANUBIAN ZONE,
CZECH REPUBLIC
Petr GADAS§
, Milan NOVÁK and Josef STANĔK
Department of Geological Sciences, Masaryk University, Kotlářská 2, CZ–611 37 Brno, Czech Republic
Jan FILIP
Regional Centre of Advanced Technologies and Materials, Palacký University, 17. listopadu 12,
CZ–771 46 Olomouc, Czech Republic
Michaela VAŠINOVÁ GALIOVÁ
Department of Chemistry, Masaryk University, Kotlářská 2, CZ–611 37 Brno, Czech Republic
Abstract
Common pegmatites with pockets lined with crystals of smoky quartz, feldspars, muscovite, and black tourmaline commonly
occur in migmatized biotite–sillimanite gneisses and felsic granulites of the Strážek Unit, Moldanubian Zone, in the Czech
Republic. Mostly concordant dikes or irregular bodies (0.1–2 m thick) consisting of an outer granitic unit, a graphic unit and a
pocket unit with large crystals (up to 1 m long) of minerals show transitional to locally sharp contacts to the host migmatized
rocks. Thin muscovite-rich veins, 1–10 cm thick, with the assemblage muscovite ≥ albite, quartz and tourmaline are closely
associated spatially. Variable prismatic to lens-shaped tourmaline crystals and their aggregates, up to 30 cm across, from pockets
and muscovite-rich veins exhibit striking zoning in the optical microscope (distinct colors and pleochroism) and in BSE images:
core (foitite – schorl – magnesio-foitite), intermediate zone (schorl – dravite) and narrow outer rim (schorl – dravite); tourmaline
from muscovite veins is relatively homogeneous (dravite – magnesio-foitite). A slight decrease in X-site vacancy, in Fetot/(Fetot +
Mg) and Al contents but sharp increase of Ti from the core to intermediate zone and outer rim, respectively, are typical. Also, the
LA–ICP–MS study of a single crystal of tourmaline from a pocket demonstrates a very similar chemical composition of core and
intermediate zone, but a distinct composition of outer rim; Mn, Ni, Zn, Sc and Ga decrease, and V, Cr, Co and Sr increase in the
rim. Nearly all Fe was determined as Fe2+
(<3% of Fe3+
in both core and intermediate zones of the tourmaline) using Mössbauer
spectroscopy. The mineral assemblages (andalusite + cordierite) of common pegmatites and their geological and petrographic
features indicate P–T conditions of ~500–650°C and less than ~3–4 kbar for massive units, but lower for tourmalines and other
minerals from pockets and in particular for associated muscovite-rich veins. The distribution of pegmatites in migmatitic rocks,
their concordant and transitional (diffusive) contacts to the country rocks, simple assemblages of minerals, primitive chemical
composition of minerals (all typical for abyssal pegmatites), and common large pockets lined with well-developed crystals of
smoky quartz, feldspars, muscovite, and tourmaline (which is typical of miarolitic pegmatites), do not fit the current classifications
of granitic pegmatites.
Keywords: foitite, schorl, dravite, magnesio-foitite, compositional evolution, zoning, pocket, common pegmatite, Moldanubian
Zone, Czech Republic.
§	 E-mail address: pgadas@centrum.cz
Introduction
Compositional trends in tourmalines have been
studied in a variety of granitic pegmatites from barren
(e.g., Novák et al. 2004a, Roda-Robles et al. 2011,
Gadas et al. 2011) to highly fractionated complex (Li)
ones (e.g., Jolliff et al. 1986, Federico et al. 1998,
Selway et al. 1999, Tindle et al. 2002, Ertl et al. 2010).
During the primary crystallization of a pegmatite, tourmaline
crystals generally exhibit an increase in Al, Mn
and Li, and a decrease in Mg, Ti and Fe in the simplified
sequence dravite–schorl–foitite ! schorl–olenite !
schorl–elbaite ! elbaite ! rossmanite. Compositional
variations in tourmaline crystals from pockets were
896	 the canadian mineralogist
examined almost exclusively in Li-rich pegmatites
(e.g., Ertl et al. 2007, 2010, Lussier & Hawthorne
2011, Lussier et al. 2011, and references therein),
where a complex zoning (oscillatory and sectoral) was
generally observed. Tourmaline crystals from pockets
in primitive, Li-poor pegmatites have only rarely been
examined (Novák et al. 2004a).
Common pegmatites, with the mineral assemblage
(Pl + Kfs + Qtz + Ab + Bt + Ms + Tur ± Ap,And,Crd)
are enclosed in migmatized gneisses and granulites, and
occur irregularly but commonly in the Moldanubian
Zone, Czech Republic. Their constituent minerals,
mainly tourmaline, were studied from the 19th century
(e.g., Kolenati 1854, Slavík 1904, Sekanina 1928), but
few analytical data were published (Povondra 1981,
MacBride 2002, Novák et al. 2004a, Míková et al.
2010). Many common pegmatites contain pockets with
zoned crystals of black tourmaline, which typically
show the compositional trend foitite ! schorl ! dravite
! magnesio-foitite from core to rim, both parallel and
perpendicular to the c axis, showing a reverse evolution
to that in ordinary pegmatites (Gadas et al. 2011). We
present here compositional data (EMPA, LA–ICP–MS,
Mössbauer spectroscopy) to document tourmaline
crystals from common pegmatites with pockets and
associated muscovite-rich veins. We also discuss the
compositional evolution found within individual crystals
of tourmaline, as well as the classification of these
pegmatites.
Geological Setting and Outline of Granitic
Pegmatites from the Strážek Unit
Common pegmatites with pockets lined with crystals
of smoky quartz, feldspars, muscovite and tourmaline
occur in several regions comprised of migmatized
gneisses and migmatized felsic granulitic rocks within
the Moldanubian Zone (Fig. 1). The pegmatites are
concentrated mainly in the Strážek Unit, but rather
isolated occurrences were found in the Moldanubian
Zone west of the Třebíč pluton, in the area adjacent
to the Kutná Hora – Svratka Unit (Fig. 1), and in the
Austrian part of the Moldanubian Zone. The metamorphic
rocks of the Strážek Unit underwent a polyphase
metamorphic evolution; a HT–HP event in the upper
amphibolite to granulite facies at Tmax ~850–900°C
and Pmax = 12–18 kbar was overprinted during a rapid
decompression by an MP–HT event at T < ~700°C and
P ~4–6 kbar (e.g., Pertoldová et al. 2009, and references
therein), and this stage very likely produced a partial
melting of rocks. Mineral assemblages of migmatized
portions of biotite–sillimanite gneisses or granulitic
gneisses are simple (Pl + Qtz + Kfs + Bt ± Sil ± Crd ±
Grt ± Hc ± Tur) and very similar to those in common
pegmatites.
Granitic pegmatites of various size, internal structure
and geochemical signature and origin are common in
the Strážek Unit and essentially in the Bory Granulite
Massif and its close vicinity (Novák 2005, Cempírek
et al. 2010). They are represented, following estimated
P–T conditions of their formation, by: (i) a borosilicatebearing
pegmatite veinlet (grandidierite–ominelite +
boralsilite + werdingite + dumortierite + schorl) cutting
leucogranulite, which postdates the development of a
foliation in the host granulite at T ≈ 750°C and P ≈
6–8 kbar (Cempírek et al. 2010); (ii) coarse-grained,
cordierite-rich leucosome in dark gneisses (cordierite
[XFe in the range 0.44–0.50] + biotite + tourmaline ±
dumortierite), locally showing pegmatitic textures but
no pockets (Povondra et al. 1992, Kotková & Melichar
2003); (iii) the simply zoned common pegmatites, the
focus of this study, with accessory andalusite, which
mostly show transitional (diffusive) contacts to country
rocks and locally contain large crystals of smoky quartz
and feldspars in pockets (Gadas et al. 2011); (iv) crosscutting,
symmetrically zoned pegmatites (muscovite +
tourmaline + andalusite + sekaninaite [XFe in the range
0.74–0.97] + biotite + apatite) with sharp contacts and
containing primary diaspore, Fe–Mn phosphates, pyrite,
löllingite, and numerous accessory minerals, commonly
occurring in the most evolved, large bodies, up to 35 m
thick and several hundred m long (Duda 1986, Staněk
1991, 1997, Novák & Taylor 2005); (v) discordant,
symmetrically zoned, complex lepidolite-subtype
pegmatites (lepidolite + elbaite + amblygonite + rossmanite)
with sharp contacts to the host rocks, the most
highly fractionated pegmatites of the region (Selway et
al. 1999, Novák et al. 2004b). The U–Pb radiometric
data on monazite from the discordant pegmatite (type
iv) in Dolní Bory – Hatě yielded the ages of 335.8 ±
2 and 337.2 ± 2 Ma (Novák et al. 1998) comparable
with the age of other pegmatites of the Moldanubian
Zone (Ertl et al. 2004). Whatever the origin and degree
of fractionation, all pegmatite types occurring in the
Bory Granulite Massif and its envelope have similar
geochemical signatures: peraluminous character, high
activity of B, presence of accessory minerals with Ti,
W, Sc, andAs, and total absence of Be-bearing minerals.
The pegmatites originated in a short period of ~5–7
Ma during rapid decompression and were sequentially
generated under rather distinct P–T conditions (for more
details see Cempírek et al. 2010).
Internal Structure and Mineralogy
of the Common Pegmatites
The common pegmatites with pockets have been
rarely found in good outcrops, and are most common
as fragments or isolated crystals found in agricultural
fields. Classical localities include Bobrůvka, Cyrilov,
Dolní Bobrová, Dolní Bory, Horní Bory, Meziboří,
Netín, Rousměrov, Suky, Vídeň and Znětínek (Fig. 1).
The pegmatites form concordant (Figs. 2a, 2b) and,
less commonly, discordant dikes or irregular bodies
with transitional to locally sharp contacts with the host
migmatized rocks (biotite–sillimanite gneiss, migma-
	 zoned tourmaline, pegmatites of the moldanubian zone	 897
tized leucocratic granulite rocks). Transitional and sharp
contacts between individual textural-paragenetic units
may be developed within a single pegmatite body. The
internal structure of pegmatites evolved from common,
simply zoned thin dikes, several cm to several dm thick
(Figs. 2a, 2b, 3), to rare, texturally more complicated
dikes, up to 2 m thick. The pegmatites are commonly
built of (i) an outermost, medium- to coarse-grained
granitic unit (Pl + Qtz + Kfs ± Bt ± Ms), (ii) a graphic
unit (Qtz + Kfs ± Bt or Ms), and (iii) a pocket unit with
large crystals of primary smoky quartz I (up to 1 m
long), K-feldspar (up to 30 cm in size), albite, muscovite
I (up to 5 cm in size) and commonly also tourmaline (up
to 30 cm long; Figs. 2c, 2d). In some pegmatite dikes,
tourmaline is absent. Larger dikes contain (iv) blocky
K-feldspar evolving gradually from graphic K-feldspar
+ quartz intergrowths and locally (v) a small quartz
core (Fig. 3). The mineral assemblages of granitic and
graphic units and in blocky K-feldspar include (along
with major and minor minerals) andalusite replaced by
muscovite, strongly altered cordierite, fluorapatite and
rare accessory dumortierite, almandine–spessartine,
pyrite, ilmenite, rutile, monazite-(Ce), xenotime-(Y)
and Zn-rich hercynite.
The pockets are distributed close to the core of
pegmatite bodies (Figs. 2a, 3), and the total volume
of pockets relative to massive pegmatite units is
highly variable within the individual bodies. The early
Fig. 1.  Selected occurrences of common pegmatites with pockets and muscovite-rich veins, plotted on the simplified geological
map of the northeasternmost part of the Moldanubian Zone. (slightly modified from Gadas et al. 2011). Gneisses and
granulites are commonly migmatized.
898	 the canadian mineralogist
minerals from pockets (chiefly K-feldspar, tourmaline
and quartz) extend their growth from the surrounding
massive pegmatite (graphic unit and blocky K-feldspar),
as is typical for miarolitic pegmatites (Černý 2000). In
pockets, smoky quartz I, K-feldspar, albite, muscovite
I and tourmaline are dominant minerals (Figs. 2c, 2d,
3). Large crystals of K-feldspar are commonly corroded
and replaced by medium-grained secondary muscovite
II and small aggregates of subparallel crystals of smoky
quartz II. Rare, but perfectly developed crystals of fluorapatite,
garnet, anatase, brookite and rutile and microscopic
inclusions of pyrrhotite and “wolframoixiolite”
in quartz and tourmaline crystals also were found.
Fine- to coarse-grained aggregates and large flakes of
muscovite and yellow to brown masses of clay minerals
typically fill the void space of pockets and represent
the latest stage of mineral deposition (see Černý 2000).
Thin muscovite-rich veins, ~1–10 cm thick and
differing from pegmatite dikes in shape, size and
internal structure, have been sporadically found in close
vicinity to common pegmatites with pocket or filling
the cracks of pegmatite dikes. They are built of porous
masses of fine- to coarse-flaked muscovite as a dominant
mineral within veins cutting the host migmatized
gneisses. Moreover, they exhibit a simple assemblage
of minerals: muscovite ≥ albite, quartz and tourmaline;
K-feldspar and accessory minerals typical of common
pegmatites, except for apatite, are commonly absent.
According to similarities in mineral assemblages and
apparent spatial relations, the muscovite-rich veins
Fig. 2.  Photographs of the outcrop of a pegmatite dike enclosed concordantly in migmatized gneiss, locality Věžná III (a) and
its cut-out detail showing xenoliths of the country rock with a locally diffuse contact marked by the arrow (b). Tourmaline
crystals from pockets in pegmatites: c) thick columnar crystal of tourmaline with smoky quartz covered in part by muscovite
I, locality Krásněves, and d) thin columnar crystals of tourmaline intergrown on albite and muscovite II, locality Bobrůvka.
	 zoned tourmaline, pegmatites of the moldanubian zone	 899
seem to be late satellite veins genetically related
to common pocket pegmatites (Gadas et al. 2011);
however, poor outcrops do not enable us to attempt a
detailed study of the relations between pegmatites and
muscovite-rich veins.
Methods and Samples
The chemical composition of tourmaline from
pockets and muscovite veins was determined using a
Cameca SX100 electron microprobe at the Joint Laboratory
of Electron Microscopy and Microanalysis, Department
of Geological Sciences, Masaryk University, and
Czech Geological Survey, in Brno. The measurements
were carried out in wavelength-dispersive mode, with
an acceleration voltage of 15 kV, a beam current of
10 nA, and a spot size of ~2–5 mm. The following
standards and X-ray Ka lines were used: sanidine
(Si, Al, K), albite (Na), olivine (Mg), andradite (Ca,
Fe), rhodonite (Mn), hornblende (Ti), chromite (Cr),
topaz (F) and ZnS (Zn). The counting time on peaks
was 10 second for major elements and 20–40 seconds
for minor to trace elements. The background counting
time was one half of the counting time on peaks on the
high- and low-energy background position. The raw
data were reduced using appropriate PAP matrix corrections
(Pouchou & Pichoir 1985). The crystal-chemical
formulae of tourmaline were calculated on 31 anions
to a general formula XY3Z6T6O18(BO3)3V3W, where X
= Na, Ca, K, vacancy, Y = Fe, Mg, Mn, Ti, Al, and V,
Z = Al, and Mg; T = Si, and Al; B = B = 3 apfu; V +
W = OH + F = 4 (or 3.5, see Novák et al. 2004a), and
using total Fe as FeO (see Mössbauer spectroscopy).
Tourmaline crystals from the following localities were
examined using the electron microprobe: tourmaline
from massive pegmatite units (Znětínek), tourmaline
from pockets (Bobrůvka, Cyrilov, Dlouhá Brtnice,
Dolní Bory, Golčův Jeníkov, Hodíškov, Krásněves,
Fig. 3.  Idealized cross-section through a common pegmatite with pockets from Znětínek.
Note different mineral assemblages on the hanging-wall part (large crystals of smoky
quartz I up to 25 cm long + albite I) and the footwall part of the pocket (large corroded
crystals of K-feldspar up to 30 cm in size + muscovite II + subparallel crystals of smoky
quartz II + tourmaline). a) Host migmatized biotite–sillimanite gneiss, b) tourmaline
on the contact, c) medium- to coarse-grained granitic unit, d) graphic unit, e) blocky
K-feldspar with massive quartz (grey), f) tourmaline (black), g) large crystals of smoky
quartz I + albite I, h) quartz II + albite II + muscovite II.
900	 the canadian mineralogist
Meziboří, Netín, Pikárec, Radenice, Sedletín, Sklenné,
Strážek, Suky, Věžná III, Vídeň, Záseka, Znětínek),
and from muscovite-rich veins (Hodíškov, Horní Bory,
Radenice).
The transmission 57Fe Mössbauer spectrum of
powdered tourmaline samples (ground under acetone
using an agate mortar) was recorded in constant acceleration
mode at room temperature using a 57Co(Rh)
source. The isomer shift value was calibrated against
an a-Fe foil. Spectra were folded and fitted by Lorentz
functions using the computer program CONFIT2000
(Žák & Jirásková 2006). The effects of non-ideal thickness
of the absorber and variable recoil-free fractions
for iron atoms in non-equivalent structural sites were
expected to be within experimental errors (hyperfine
parameters ±0.01 mm s–1, relative spectral area ±1%).
Prior to analysis, all samples were washed in a cold
dilute hydrochloric acid in order to remove any possible
interstitial iron oxides and oxyhydroxides. The core and
intermediate zone were examined on two zoned crystals
from pockets (Hodíškov and Suky).
Instrumentation for the LA–ICP–MS at the Department
of Chemistry, Masaryk University, Brno, consists
of a laser-ablation system UP 213 (New Wave, USA)
and anAgilent 7500 CE ICP–MS spectrometer (Agilent,
Japan). A commercial Q-switched Nd:YAG laser-ablation
device works at the fifth harmonic frequency, which
corresponds to the wavelength of 213 nm. The ablation
device is equipped with programmable XYZ stages to
move the sample along a preset trajectory during ablation.
The ablation cell was flushed with helium (carrier
gas), which transported the laser-induced aerosol to
the inductively coupled plasma – mass spectrometer
(1 L/min). A gas flow of argon was admixed to the
helium carrier gas flow after leaving the laser-ablation
cell. Therefore, the total gas flow was 1.6 L/min. For
LA–ICP–MS measurements, we used the hole-drilling
mode (fixed position of sample during laser ablation)
for the duration of 60 seconds per each spot. Laser
ablation was performed with a laser spot-diameter of
80 mm, laser fluence 4.5 J cm–2 and repetition rate 10
Hz. We examined a zoned crystal of tourmaline with
well-developed core, intermediate zone and outer rim
from pocket in the pegmatite Suky.
Description, Mineral Assemblages
and Zoning of Tourmaline
Black tourmaline, a widespread accessory mineral
in common pegmatites, is present in several morphological
types in the texturally more evolved larger
bodies of pegmatite (Fig. 3). Prismatic crystals and
their aggregates are commonly enclosed in blocky
K-feldspar, massive quartz and albite; tourmaline is
commonly absent in the graphic unit. Radial aggregates
of tourmaline were also sporadically found in country
rocks near or directly on the contact with pegmatite
(Fig. 3); nevertheless, the amount of tourmaline in
massive pegmatite units (least in the graphic unit, and
in subequal proportions in the blocky K-feldspar and
the massive quartz) is much smaller relative to pockets.
In the muscovite-rich veins, well-developed isolated
crystals of tourmaline and aggregates are present.
Tourmaline from pockets forms nearly euhedral
long prismatic to short bipyramidal crystals (with a
hexagonal or trigonal cross-section, Figs. 2c, 2d, 4)
and their parallel to subparallel intergrowths, both
up to 30 cm in size. Rarely, long doubly-terminated
prismatic crystals are hemihedral with a pyramidal
analogous pole, whereas a pedion usually terminates
the antilogous pole. Crystals typically show prismatic
striations and a strong vitreous luster (Figs. 2c, 2d, 4).
Long prismatic crystals commonly grew from adjacent
massive-pegmatite unit (mostly blocky K-feldspar)
into the open space of pocket. In contrast, lens-shaped
crystals, doubly-terminated prismatic to tabular crystals
and some subparallel intergrowths grow on crystals of
quartz or albite, and the whole volume of the tourmaline
crystal was formed within pockets. Exceptionally, late
hair-like fibrous aggregates of pale brown tourmaline
occur in pockets (see Dutrow & Henry 2000). Tourmaline
crystals and aggregates are generally overgrown by
muscovite, quartz and albite, and all these minerals are
present in two (or more) generations in pockets, where
they crystallized with a more or less evident hiatus. The
textural relations suggest that K-feldspar and tourmaline
crystals extending from the massive pegmatite unit are
the earliest minerals to crystallize into the pockets (see
also Němec 1992).
Almost all crystals of tourmaline from pockets in
common pegmatites exhibit striking zoning (transmitted
light) and in the BSE images as well (Fig. 5), both
parallel and perpendicular to the c axis. The core is
volumetrically dominant and exhibits a sharp contact
with the intermediate zone. The outer rim is usually
narrow, from 5–20 mm thick, only exceptionally up
to 300 mm (locality Suky, Fig. 5), typically with sharp
contacts with the intermediate zone. The individual
zones have different pleochroism (Fig. 5); in the core:
O: greyish blue to khaki green, E: pale yellowish to
colorless; intermediate zone: O: brown, E: pale brown
to yellowish; outer rim: O: dark brown to brown, E:
pale brown to yellowish. Within the core, a weak to
moderate sector zoning and rare fine-oscillatory or
patchy zoning were observed; oscillatory zoning is
common in the intermediate zone (Fig. 5). Only locally,
the core is partly replaced along the contact with the
intermediate zone (locality Suky, Fig. 5). Also, late
veins with a composition close to the outer rim replace
core and intermediate zones (locality Suky, Fig. 5). The
thin outer rim is commonly homogeneous, rarely with
fine oscillatory zoning. On the contrary, tourmaline
crystals from muscovite-rich veins are optically and
compositionally rather homogeneous, and pleochroic
(O: brown, E: pale brown).
	 zoned tourmaline, pegmatites of the moldanubian zone	 901
The Chemical Composition of Tourmaline
Wet-chemical analyses of tourmaline crystals from
the common pegmatites at the localities Bobrůvka,
Dolní Bobrová, Cyrilov, Dolní Bory, Horní Bory,
Meziboří, Pikárec and Rousměrov were published by
Povondra (1981). The following minerals of the tourmaline
supergroup (cf. Henry et al. 2011) were identified:
schorl, “oxy-schorl”, dravite, “oxy-dravite” and foitite;
however, these data represent bulk compositions of
Fig. 4.  Crystals of tourmaline from common pegmatites; a) Dolní Bory, b) Meziboří, c)
Cyrilov. Drawings of crystals from Sekanina (1928), photographs by P. Gadas.
902	 the canadian mineralogist
Fig. 5.  Photomicrographs combining BSE images of zoned crystals of tourmaline from pockets in common pegmatites. The
cuts are perpendicular to the c axis of the crystals; C: core, I: intermediate zone, R: outer rim or late veining (Suky). Note the
sharp contacts between the individual zones and the alteration of core in the crystal from Suky.
	 zoned tourmaline, pegmatites of the moldanubian zone	 903
whole crystals, and evident optical and compositional
zoning (Fig. 5) was mostly overlooked. Only different
density fractions from the individual zoned crystals
were analyzed separately at some localities. Generally,
low Fe3+ (<0.2 apfu), Si (6.01–5.84 apfu) and a
content of B in the range 2.91–3.07 apfu, close to the
stoichiometric value (3) were found in these tourmalines,
along with highly variable Fe/(Fe + Mg), in the
range 0.80–0.40 (Povondra 1981, Novák et al. 2004a).
Electron-microprobe data
In the Znětínek pegmatite (Fig. 3), the following
paragenetic types of tourmaline were examined: grains
from host rock and the needle-like crystals from contact
with country rock (both Mg-rich schorl), prismatic
crystals of foitite in blocky K-feldspar, small prismatic
crystals occurring in pockets (foitite ≈ schorl > dravite)
associated with quartz II and muscovite II, respectively.
They exhibit a great variation in Fetot/(Fetot + Mg)
(0.52–0.56, 0.80–0.81, 0.44–0.75); foitite from blocky
K-feldspar is Ca- and Ti-poor with ≤0.02 and ≤0.03
apfu, whereas tourmalines from both contact and host
rock are slightly enriched in these elements, with ≤0.10
apfu Ca and ≤0.10 apfu Ti relative to tourmalines from
pegmatite.
The optical zoning and compositional zoning in individual
crystals from pockets are only partly consistent
(Fig. 5, Table 1). The core (foitite ≈ schorl > magnesiofoitite)
with Fetot/(Fetot + Mg) in the range 0.99–0.41)
and intermediate zone (schorl > dravite) with Fetot/(Fetot
+ Mg) in the range 0.99–0.39) are compositionally
similar, showing mostly a slight to moderate decrease
(rarely also a slight increase) in Fetot/(Fetot + Mg) and in
Al, and a slight decrease in the X-site vacancy (Fig. 6).
Rims of crystals from pockets (schorl ≈ dravite) are
generally more homogeneous, with Fetot/(Fetot + Mg)
in the range 0.71–0.36. The only exception in Fe/Mg
behavior is a zoned crystal from Bobrůvka (Fig. 5),
where the intermediate zone has evidently higher Fetot/
(Fetot + Mg), in the range 0.88–0.81, relative to the
core, with 0.61–0.62, and the rim, with 0.56–0.60. On
the other hand, tourmaline from Suky shows almost
identical Fetot/(Fetot + Mg) in core and intermediate zone
(0.98–0.97), but very low Fetot/(Fetot + Mg) (0.36–0.37)
in outer rim (Fig. 6). A sudden increase of Ti from
the core to the intermediate zone and locally from the
intermediate zone to the outer rim (Fig. 6c) is a typical
feature of all crystals. Variation in X-site vacancy shows
a moderate decrease from core (0.63–0.28 pfu) to intermediate
zone (0.51–0.23 pfu) and rim (0.47–0.12 pfu).
Low Ca contents (≤0.05 apfu, exceptionally up to 0.1),
are typical of the core and intermediate zone; rims are
slightly Ca-enriched, up to ≤0.15 apfu.
Chemical variability of tourmaline from muscoviterich
veins is generally low, with high variability in
X-site vacancy (0.59–0.15 pfu) (Fig. 6), but only slightly
variable Fetot/(Fetot + Mg) (0.45–0.31). Tourmaline is
also enriched in Ti, up to 0.18 apfu, 1.46 wt.% TiO2,
except for the narrow outer rim, with ≤0.10 apfu Ti
(Fig. 6c). Calcium has very similar behavior, with up
to 0.21 apfu Ca in the core but only ≤0.15 apfu Ca in
the outermost rim (Fig. 6a).
With his results of wet-chemical analyses, Povondra
(1981) identified also “oxy-schorl” and “oxy-dravite” in
the common pegmatites. However, the formula calculations
normalized on V + W = OH + F = 4 or on 3.5 apfu,
as recommended by Novák et al. (2004a), yielded better
results (e.g., Si close to 6 apfu) for the normalization
V + W = OH + F = 4. This suggests a low proportion
of oxy-tourmaline components (Henry et al. 2011) in
most tourmalines.
Mössbauer spectroscopy
The Mössbauer spectra acquired for two zoned
crystals from pockets in pegmatites (locality Suky and
Hodíškov) were fitted with four doublets corresponding
to [6]Fe2+ and one doublet corresponding to [6]Fe3+ (all
iron in a high-spin state; Fig. 7). The resulting hyperfine
parameters of these doublets and their structural assignments
(Table 2) are comparable to previously studied
tourmalines (cf. Andreozzi et al. 2008, and references
therein). Almost identical Mössbauer spectra collected
from both core and intermediate zone of each single
crystal of tourmaline indicates only slight variations
in next-nearest-neighbor populations in our tourmaline
crystals. The quantitative interpretation of Mössbauer
spectra yielded nearly all iron as divalent (<3% Fe3+/
Fetot) for both core and intermediate zone, respectively
(Fig. 7). Consequently, we could exclude the role of
Fe3+ fluctuation in zoning or a different pleochroism
among particular zones; this highlights the role of Ti in
the zoning observed (as indicated above; Fig. 5). Rims
of the tourmaline crystals were not examined owing
to their small size (Fig. 5). The results of Mössbauer
spectroscopy are only slightly different from the results
of wet-chemical analyses of Povondra (1981), where
higher but still low contents of Fe3+, less than 0.2 apfu
(<13% Fe3+/Fetot), were only exceptionally revealed.
The LA–ICP–MS data
A single crystal of tourmaline from a pocket in
common pegmatite at the locality Suky (Figs. 5, 8, Table
3) with a well-developed zoning, including a relatively
thick outer rim, was studied using LA–ICP–MS. The
results show a quite complicated behavior of some trace
elements related to the zonal development observed
with the optical microscope and in BSE images of
the crystal. Titanium is the only element showing
increasing concentrations from core (413–1586 ppm)
through intermediate zone (1573–3288 ppm) to outer
rim (3268–6008 ppm), invariably with sharp contacts
904	 the canadian mineralogist
(Fig. 8, Table 3). These concentrations are generally
equal with those measured by EMP. Along with low
contents of Fe3+, these results suggest Ti, possibly
through an intervalence charge-transfer interaction
involving Fe2+ and Ti (Pezzotta & Laurs 2011), is
very likely a chromophore that causes a brown color
(and pleochroism) of these otherwise compositionally
comparable zones. The other elements commonly
demonstrate very similar concentrations in core and
intermediate zone, but distinct levels in the outer rim;
Mn, Ni, Zn, Sc and Ga decrease, and V, Cr, Co, Sr and
REE increase in the rim, respectively (Fig. 8). Some
elements do not show any evident variation, and their
concentrations within core, intermediate zone and outer
rim are rather constant (P, Cu, Sn, Pb; see Table 3 and
Fig. 8). The additional elements sought (Be, As, Y, Zr,
Ag, Cd, Sb, Cs, Ba, Hf, Ta, W, Bi, Th, U) were found
to be below or mostly close to their detection limits.
Lithium was found at a concentration of about the
detection limit (~50 ppm) in all zones.
TABLE 1. REPRESENTATIVE COMPOSITIONS OF TOURMALINE FROM SELECTED LOCALITIES
IN POCKETS FROM COMMON PEGMATITES AND FROM MUSCOVITE-RICH VEINS
_______________________________________________________________________________________________________________
pegmatites muscovite-rich veins
_______________________________________________________________ __________________________
Dolní Bory F Bobrùvka Ä Suky G Ä Ä G G
_________________ _________________ _________________ _____ _____ _____ _____
C I R C I R C I R C R C R
_______________________________________________________________________________________________________________
2SiO wt.% 35.96 34.94 35.43 36.86 35.26 35.49 34.99 34.35 36.02 35.95 36.05 35.93 36.44
2TiO 0.20 0.87 0.85 0.32 0.79 1.03 0.09 0.39 0.86 1.25 1.02 1.43 0.63
2 3Al O 34.79 33.95 33.01 35.12 34.45 34.01 36.11 34.97 33.48 33.14 34.83 31.88 33.57
2 3Cr O 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.17 0.03 0.16 0.08
2 3V O 0.00 0.00 0.00 0.00 0.03 0.03 0.00 0.00 0.03 0.17 0.08 0.13 0.05
FeO 13.28 13.77 10.01 9.26 12.27 9.29 13.33 14.24 6.52 6.93 6.44 7.19 5.70
MnO 0.15 0.19 0.08 0.06 0.19 0.05 0.25 0.31 0.02 0.01 0.03 0.03 0.02
MgO 0.79 0.84 3.67 3.25 1.52 4.08 0.18 0.22 6.50 6.08 5.58 6.61 6.42
CaO 0.03 0.11 0.21 0.17 0.19 0.44 0.05 0.08 0.74 0.82 0.39 1.09 0.47
2Na O 1.30 1.75 1.63 1.49 1.66 2.11 1.40 1.83 1.59 1.94 1.68 1.94 1.43
F 0.36 0.45 0.41 0.11 0.48 0.44 0.46 0.67 0.25 0.00 0.00 0.22 0.17
O=F -0.15 -0.19 -0.17 -0.05 -0.20 -0.19 -0.19 -0.28 -0.11 0.00 0.00 -0.09 -0.07
2H O* 3.44 3.36 3.38 3.63 3.37 3.44 3.38 3.24 3.55 3.67 3.70 3.55 3.58
2 3B O * 10.46 10.35 10.37 10.68 10.44 10.57 10.43 10.32 10.64 10.64 10.71 10.59 10.60
Total 100.61 100.39 98.88 100.90 100.45 100.79 100.48 100.34 100.09 100.77 100.54 100.66 99.09
Si apfu 5.976 5.865 5.937 5.998 5.872 5.833 5.832 5.785 5.883 5.872 5.850 5.896 5.975
Al 0.024 0.135 0.063 0.002 0.128 0.167 0.168 0.215 0.117 0.128 0.150 0.104 0.025IV
B 3.000 3.000 3.000 3.000 3.000 3.000 3.000 3.000 3.000 3.000 3.000 3.000 3.000
Al 6.000 6.000 6.000 6.000 6.000 6.000 6.000 6.000 6.000 6.000 6.000 6.000 6.000Z
Al 0.790 0.582 0.456 0.734 0.634 0.421 0.925 0.726 0.327 0.252 0.511 0.061 0.462Y
Ti 0.025 0.110 0.107 0.039 0.099 0.127 0.011 0.049 0.106 0.154 0.124 0.176 0.078
Cr 0.000 0.000 0.000 0.000 0.000 0.000 0.000 0.000 0.000 0.022 0.004 0.021 0.010
V 0.000 0.000 0.000 0.000 0.004 0.004 0.000 0.000 0.004 0.022 0.010 0.017 0.0073+
Fe 1.846 1.933 1.403 1.260 1.709 1.277 1.858 2.006 0.891 0.947 0.874 0.987 0.7822+
Mn 0.021 0.027 0.011 0.008 0.027 0.007 0.035 0.044 0.003 0.001 0.004 0.004 0.003
Mg 0.196 0.210 0.917 0.788 0.377 1.000 0.045 0.055 1.583 1.480 1.350 1.617 1.569
ÓY 2.878 2.862 2.894 2.829 2.850 2.836 2.874 2.880 2.914 2.878 2.877 2.883 2.911
Ca 0.005 0.020 0.038 0.030 0.034 0.077 0.009 0.014 0.129 0.144 0.068 0.192 0.083
Na 0.419 0.570 0.530 0.470 0.536 0.672 0.452 0.598 0.503 0.614 0.529 0.617 0.455
ÓX 0.424 0.590 0.568 0.500 0.570 0.749 0.461 0.612 0.632 0.758 0.597 0.809 0.538
G 0.576 0.410 0.432 0.500 0.430 0.251 0.539 0.388 0.368 0.242 0.403 0.191 0.462X
F 0.189 0.239 0.217 0.057 0.253 0.229 0.242 0.357 0.129 0.000 0.000 0.114 0.088
OH 3.811 3.761 3.783 3.943 3.747 3.771 3.758 3.643 3.871 4.000 4.000 3.886 3.912
_______________________________________________________________________________________________________________
The compositions were established with electron-microprobe analyses. The symbols are as defined in Figure 4.
	 zoned tourmaline, pegmatites of the moldanubian zone	 905
Fig. 6.  Left: Compositional evolution of tourmalines in a plot of Fetot/(Fetot+Mg) versus X-site vacancy. Individual dikes of
pegmatite as well as muscovite-rich veins are distinguished by different symbols; grey-colored symbols represent central
parts, and white-colored symbols, the outer rim of tourmaline crystals. Right: Triangular plots showing X-site compositions
(a), Fe–Al–Mg compositions (b), and Ti/Al plot (c) of the individual types of tourmaline from pegmatite dikes and muscoviterich
veins. Colored symbols are related to the localities shown in Figure 5 and Table 1: blue circles: Dolní Bory, yellow
triangles: Bobrůvka, red squares: Suky.
906	 the canadian mineralogist
Discussion
Compositional trends in zoned crystals of tourmaline
Tourmaline crystals from common pegmatites with
pockets exhibit rather primitive compositions, with low
Li, Mn and F contents (Tables 1, 3; see also Povondra
1981, Novák et al. 2004a), but a highly variable Fetot/
(Fetot + Mg) value, low to high Al, and low to moderate
contents of Ti and Ca (Table 1, Fig. 6). Similar primitive
compositions are typical of Al-rich metapelites
(Henry & Dutrow 1996), and only rarely have they been
described from granitic pegmatites (e.g., Roda et al.
2005, Roda-Robles et al. 2011, Hezel et al. 2011, Novák
et al. 2011). The core (foitite – schorl – magnesiofoitite)
and intermediate zone (schorl–dravite), being
volumetrically dominant in most crystals from pockets
(Fig. 5), are compositionally similar, commonly
showing a slight decrease in X-site vacancy and Al, but
a significant increase of Ti, from the core to the intermediate
zone. The Fetot/(Fetot + Mg) value commonly
decreases (only rarely increases) from the core to the
intermediate zone (Fig. 6). However, the core compositions
at the individual localities vary significantly, from
foitite–schorl with Fetot/(Fetot + Mg) = 0.99 at Hodíškov
to dravite – magnesio-foitite with Fetot/(Fetot + Mg) =
0.43 and 0.41 in the pegmatite Pikárec (Figs. 6a, b).
The crystals, which evidently grew continuously from
surrounding massive pegmatite units into pockets, have
commonly a higher Fetot/(Fetot + Mg) value, whereas
crystals growing solely in pockets are enriched in Mg.
Fig. 7.  Room-temperature 57
Fe Mössbauer spectrum of tourmaline sample from common
pegmatite with pockets (locality Suky, Table 2): a) core, b) intermediate zone. White
doublets: Fe2+
, grey: Fe3+
(see the text for more details).
	 zoned tourmaline, pegmatites of the moldanubian zone	 907
Geochemical fractionation, documented mainly
by an evident increase in Fe/(Fe+Mg), was indicated
only in tourmaline from the contact zone of the blocky
K-feldspar in the pegmatite Znětínek and in a zoned
crystal of tourmaline from a pocket at the locality
Bobrůvka (Figs. 5, 6a, b, c), where the Fe/(Fe + Mg)
value increases significantly from core to intermediate
zone. Most tourmaline crystals from pockets in common
pegmatites and all crystals from muscovite-rich veins
are more or less Mg-enriched, and such reverse compositional
evolution in Fetot/(Fetot + Mg) distinct from
those found in granitic pegmatites is striking (Fig. 6).
A late tourmaline (outer rims of crystals or fibrous
aggregates) from granitic pegmatites with a dominant
dravite component was found at some localities, e.g.,
the contaminated elbaite-subtype pegmatite Bližná I
(Novák 1998, Novák et al. 1999a, 2012) and an intragranitic
NYF euxenite-type pegmatite Kožichovice
III from the Třebíč pluton (Novák et al. 2010). The
early tourmaline crystals at these localities (Mn-rich
elbaite–liddicoatite at Bližná I and Ti-enriched dravite
– schorl – uvite at Kožichovice III) are compositionally
very distinct (e.g., 0.33 and 1.25–1.41 apfu Mg, respectively).
It seems that a Ca- and Ti-poor dravitic tourmaline
with low to moderate YAltot (~0.0–0.3 apfu), but
high and variable X-site vacancy (0.2–0.5 pfu) is a stable
composition at low-T conditions (see e.g., Sperlich
et al. 1996, Henry & Dutrow 1996). The outermost
rim of tourmaline crystals from muscovite-rich veins,
TABLE 2. ROOM-TEMPERATURE Fe MÖSSBAUER HYPERFINE57
PARAMETERS FOR THE CORE AND INTERMEDIATE ZONE OF THE
TOURMALINE CRYSTAL FROM POCKETS AT SUKY AND HODÍŠKOV
____________________________________________________________
Valence Parameter Suky Hodíškov Assignment
of iron ____________ ____________
core int. zone core int. zone
____________________________________________________________
Fe ä (mm s ) 1.09 1.08 1.09 1.092+ –1
QÄE (mm s ) 2.46 2.49 2.46 2.48 Y1 site–1
à (mm s ) 0.29 0.28 0.28 0.29–1
RA (%) 43 47 41 35
Fe ä (mm s ) 1.08 1.07 1.08 1.092+ –1
QÄE (mm s ) 2.17 2.20 2.16 2.24 Y2 site–1
à (mm s ) 0.30 0.29 0.32 0.27–1
RA (%) 31 26 33 21
Fe ä (mm s ) 1.05 1.05 1.04 1.082+ –1
QÄE (mm s ) 1.78 1.82 1.65 1.97 Y3 site–1
à (mm s ) 0.38 0.31 0.46 0.37–1
RA (%) 10 7 17 23
Fe ä (mm s ) 1.00 1.02 0.95 1.032+ –1
QÄE (mm s ) 1.36 1.45 1.08 1.31 Z site–1
à (mm s ) 0.60 0.56 0.53 0.55–1
RA (%) 13 16 7 18
Fe ä (mm s ) 0.29 0.29 0.27 0.343+ –1
QÄE (mm s ) 0.36 0.35 0.42 0.54 Y site–1
à (mm s ) 0.27 0.26 0.30 0.23–1
RA (%) 3 3 2 2
____________________________________________________________
See Figure 7 and the text for more details). Notation: ä: isomer shift (±0.02
Qmm s ), ÄE : quadrupole splitting (±0.02 mm s ), Ã: peak width (±0.02 mm–1 –1
s ), RA: relative area in the spectrum (±3%), and int.: intermediate.–1
TABLE 3. CONCENTRATION OF TRACE ELEMENTS (MOVING AVERAGE)
FOR CORE, INTERMEDIATE ZONE AND OUTER RIM OF TOURMALINE FROM SUKY
___________________________________________________________________________________
ele- core intermediate zone rim d.l.
ment ___________________ ____________________ ____________________
range ä ¯x range ä ¯x range ä ¯x
___________________________________________________________________________________
P 150 - 314 28 217 162 - 370 33 225 160 - 434 49 222 3
Sc 82 - 251 27 133 80 - 174 27 115 45 - 113 15 84 9
Ti 413 - 1586 217 988 1573 - 3288 217 2455 3268 - 6008 650 4299 4
V b.d.l. - - b.d.l. - - 277 - 607 68 430 0
Cr 1 - 6 1 2 1 - 9 1 3 85 - 270 37 149 1
Mn 970 - 3482 380 1864 1066 - 3535 380 2312 129 - 292 36 204 2
Ni 374 - 884 107 579 350 - 888 107 623 209 - 384 46 286 0.3
Co b.d.l. - - b.d.l. - - 7 - 17 2.6 11.6 0.1
Cu 14 - 40 5 20 14 - 50 4 22 12 - 34 4 18 4
Zn 286 - 821 90 465 306 - 927 90 546 72 - 194 27 119 3
Ga 23 - 56 8 39 62 - 203 23 136 70 - 212 24 124 2
Sr b.d.l. - - b.d.l. - - 33 - 98 13 58 0.2
Sn 70 - 181 19 103 77 - 170 19 109 57 - 131 15 93 4
Pb b.d.l. - 0.76 0.1 0.26 0.2 - 1.4 0.1 0.5 0.8 - 3 0.5 1.6 0.1
Nb 0.3 - 2.1 0.3 1 0.8 - 4.7 0.3 1.8 b.d.l. - 0.5 0.1 0.2 0.1
ÓREE 0.2 - 1.8 0.3 0.7 0.4 - 4 0.3 2.1 3.6 - 11.4 2 6.8 0.1
___________________________________________________________________________________
Notations: d.l.: detection limit, b.d.l.: below detection limit, ä: standard deviation, ¯x average.
Concentrations are quoted in ppm.
Notations: d.l.: detection limit, b.d.l.: below detection limit, : standard deviation, x: average. Concentrations
are quoted in ppm.
908	 the canadian mineralogist
Fig. 8.  LA–ICP–MS data (see also Table 3) and plots of
compositional evolution from the core (C) through the
intermediate zone (I) to the rim (R) of tourmaline from
locality Suky (Fig. 5) in comparison to EMPA results along
the same profile.
	 zoned tourmaline, pegmatites of the moldanubian zone	 909
which are the latest and evidently crystallized from
hydrothermal fluids, have mostly a very similar compositional
signature (Fig. 6), except for elevated contents
of Ti. Hence, only the very narrow outer rim is Ti-poor
(≤0.10 apfu) and fits perfectly the compositions of the
late dravite (Novák 1998, Novák et al. 1999a, 2010).
Trace-element profiles from our LA–ICP–MS study
of the sample from the locality Suky reveal distinct
behavior within the individual zones (Fig. 8). However,
except for Ti, all other elements have very similar to
almost equal concentrations in the core and intermediate
zone, whereas the rim is distinct (Table 3, Fig. 8).
On the basis of the compositional data (Table 1,
Fig. 6) and the textural development of zoned crystals
from pockets (Fig. 5), the crystallization of a moderately
evolved melt in a closed system resulted in the core
zone of the tourmaline crystals. The striking change in
the zonal texture but only a weak change in chemical
composition from the core to intermediate zone (except
for Ti; Fig. 8, Table 3) indicate some change in a
parent medium (e.g., transition from a magmatic to a
hydrothermal stage). Both core and intermediate zone
crystallized in a somewhat closed system related to a
primary process of growth. The crystallization of the
outer rim of crystals (and whole crystals of tourmaline
from muscovite-rich veins) proceeded in hydrothermal
conditions in an open system, with the fluids of rather
constant composition corresponding to a compositional
uniformity of the country rocks. Also, fine oscillatory
zoning in tourmaline, common mainly in the intermediate
zone and less abundant in the outer rim (Fig. 5),
is a feature found in many examples of hydrothermal
tourmaline from magmatic–hydrothermal systems (e.g.,
London & Manning 1995, Buriánek & Novák 2004);
the associated pegmatites were the likely source of
fluids. However, these results are only preliminary, and
a more thorough chemical and isotopic study of fluid
and solid inclusions is required to reveal the process of
crystallization.
Geological position of common pegmatites
and remarks on their classification
The regional distribution of common pegmatites
with pockets is not strictly consistent with all areas
of regional migmatization within the Moldanubian
Zone. They are evidently concentrated in the Strážek
Unit (Fig. 1), where discordant rare-element-enriched
pegmatites also are very abundant (Breiter et al. 2010,
Cempírek et al. 2010). Unfortunately, a lack of suitable
outcrops rule out a systematic structural and
petrological study of the common pegmatites and their
host rocks. Such an investigation would be required
to determine the compositional-textural relations
and relevant magmatic or metamorphic or anatectic
or deformation event that may have generated these
pegmatites. Nevertheless, relative to other regional
units of the Moldanubian Zone, a fertility of the Strážek
Unit favoring the formation of more evolved and large
pegmatites, commonly with pockets lined with crystals
of feldspars, quartz, muscovite and various tourmalines
(schorl, elbaite, liddicoatite, foitite), is evident. It is
manifested by the occurrences of famous pegmatites,
e.g., the sekaninaite-bearing pegmatites with pockets
at Dolní Bory (Černý et al. 1997), the pocket-bearing
elbaite-subtype pegmatite from Řečice (Novák et al.
1999b, Novák 1999), lepidolite-subtype pegmatites
from Rožná (Černý et al. 1995, Selway et al. 1998,
Breiter et al. 2010), from Dobrá Voda (Selway et al.
1999, Novák & Taylor 2000) and from Laštovičky
(Selway et al. 1999, Novák et al. 2004b).
The distribution of common pegmatites with
pockets (Fig. 1), their geological position, as well as
their commonly concordant character and transitional
contacts with host rocks (Figs. 2a, 2b, 3), suggest that
they may have originated during regional anatexis
[authigenic pegmatites in the sense of London (2008)].
The transport of anatectic melts was likely insignificant
to absent, especially in the case of small concordant
pegmatite bodies with diffusive contacts. Also a relatively
large, zoned pegmatite body from the locality
Znětínek (this study) is concordant to foliation of
the host migmatized biotite gneiss (Fig. 3), although
relatively sharp contacts indicate transport of the
pegmatite-forming melt. The source of B in the melt
is not known, and its examination is beyond the scope
of this paper. The presence of accessory tourmaline in
the host migmatized gneisses and granulites indicates
that its breakdown during anatectic melting may have
supplied B (Kawakami 2001, van Hinsberg et al. 2011).
Nevertheless, a pluton-derived origin of the common
pegmatites cannot be excluded, although their regional
distribution (Fig. 1) does not indicate any relation to
potential parental plutons.
The prevailing concordant relationships of common
pegmatites with pockets to host rocks (Figs. 2a, b),
their zoned internal structure, the typical pegmatite
textures (e.g., graphic intergrowths of K-feldspar +
quartz, blocky K-feldspar, quartz core; Fig. 3), and
overall mineral assemblages suggest that the massive
parts of common pegmatites crystallized from a melt. In
contrast, the textural relations and mineral assemblages
of most tourmaline crystals in pockets and chiefly from
muscovite-rich veins indicate that they rather crystallized
from hydrothermal fluids at a lower T. The mineral
assemblages and overall geological and petrographic
features indicate a wide range of P–T conditions at T
<~500–650°C and P less than ~3–4 kbar for massive
units (with andalusite + cordierite) and lower T, down
to ~400–200°C in the mineral assemblages of pockets
characterized by primary muscovite I and common
replacement of K-feldspar by the assemblage muscovite
II + smoky quartz II. Abundant muscovite and the
absence of K-feldspar in muscovite-rich veins imply
lower P–T conditions, but these are not elucidated in
detail.
910	 the canadian mineralogist
The common pegmatites with pockets from the
Moldanubian Zone have been rarely found as outcrops
(Figs. 2a, b); these were mostly destroyed by mineral
collectors. This makes their structural, geochemical
and petrological study and discussion of origin as
well as classification uncertain. They exhibit a simple
zonal internal structure, textural–paragenetic units
and mineral assemblages typical for common granitic
pegmatites. Their spatial, compositional, mineralogical
and genetic relations to anatexis (migmatization of
gneisses and granulites) indicate that they may belong
to the abyssal class of pegmatites (Černý & Ercit 2005,
London 2008, Simmons & Webber 2008). However,
the main textural difference that they exhibit relative to
ordinary abyssal (anatectic) pegmatites is the presence
of abundant pockets. The combination of evidently
concordant and transitional (diffusive) contacts to
host rocks and primitive chemical composition of
minerals as typical features of abyssal pegmatites,
and of common large pockets lined with large crystals
of smoky quartz, feldspars, micas, and tourmaline as
typical features of miarolitic pegmatites, does not fit the
current classification of granitic pegmatites. However,
it documents the extremely high variability of granitic
pegmatites and their origin (London 2008).
Acknowledgements
The reviews by D. Henry and G. Morgan VI, as
well as the comments of the Guest Editor D. London,
are gratefully acknowledged. We authors thank to T.
Kadlec for samples of tourmaline from locality Golčův
Jeníkov and S. Houzar, Moravian Museum in Brno
for the samples of tourmaline from Meziboří, Sedletín
and Věžná. Milan Novák gratefully acknowledge Petr
Černý, University of Manitoba, Winnipeg, for his
outstanding contribution to the research on granitic
pegmatites, their minerals and origin, as well as to
the way of thinking about them, his influences also
indirectly but significantly influenced the approach to
research of pegmatites of his students, including the
first author. This work was supported by (i) the research
project GAČR P210/10/0743 to PG and MN, (ii) the
Operational Program Research and Development for
Innovations, European Regional Development Fund
(project CZ.1.05/2.1.00 /03.0058 of the Ministry of
Education, Youth and Sports of the Czech Republic) for
JF, and (iii) the long-term Research Plan of the Ministry
of Education of the Czech Republic MSM0021622412
(INCHEMBIOL) to MVG. A small part of the laboratory
work was done during the second author’s tenure
of a Postdoctoral Fellowship in 1991–1993, awarded
by the Faculty of Science, University of Manitoba.
Research costs were covered by the Natural Sciences
and Engineering Research Council of Canada (Major
Installation, Major Equipment and Infrastructure Grants
to P. Černý and F.C. Hawthorne).
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Received July 27, 2011, revised manuscript accepted June
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