1077
The Canadian Mineralogist
Vol. 50, pp. 1077-1094 (2012)
DOI : 10.3749/canmin.50.4.1077
CONTRASTING ORIGINS OF THE MIXED (NYF + LCT)
SIGNATURE IN GRANITIC PEGMATITES, WITH EXAMPLES
FROM THE MOLDANUBIAN ZONE, CZECH REPUBLIC
Milan NOVÁK§
, Radek ŠKODA and Petr GADAS
Department of Geological Sciences, Masaryk University, Kotlářská 2, CZ–611 37 Brno, Czech Republic
Lukáš KRMÍČEK
Department of Geological Sciences, Masaryk University, Kotlářská 2, CZ–611 37 Brno, and AdMaS Research Centre,
Brno University of Technology, Veveří 95, CZ–602 00 Brno, Czech Republic
Petr Černý
4C Minerals, s.r.o. Korunní 29, CZ–120 00 Praha 2, Czech Republic
Abstract
Two granitic pegmatites with mixed (NYF + LCT) signatures from the Moldanubian Zone, Czech Republic, were examined
to determine their origin. On the basis of geological setting, paragenesis, geochemical modeling and chemical composition
of rocks and minerals, two contrasting modes of origin were discerned. The Li-bearing (lithium micas + elbaite) Kracovice
pegmatite, with “amazonite”, samarskite and fergusonite, is the product of the strong fractionation of pegmatite-forming melt
derived from the orogenic I-type Třebíč pluton. Geological, petrological, compositional and isotopic data from this ultrapotassic
melasyenite–melagranite point to mixing of a mantle-derived magma with (leuco)granitic melt from crustal rocks. The granite–
pegmatite system of the Třebíč pluton and the mainly Li-bearing Kracovice pegmatite are typical examples of the mixed
(NYF + LCT) petrogenetic family. The contaminated elbaite-subtype pegmatite Bližná I, Český Krumlov Unit, with lithium
tourmalines (elbaite, liddicoatite, uvite), primary REE minerals [bastnäsite-(Ce), parisite-(Ce), allanite-(Ce)] and Ca(Mg)-rich
minerals (diopside, uvite, titanite), gained its mixed signature through a unique pre-emplacement process involving the external
contamination with Ca, Mg and REE of an evolved (LCT) pegmatite-forming melt by distal carbonatite-like marbles with an
NYF signature. Despite the clearly mixed-signature mineralogy and geochemistry, the Bližná I pegmatite represents a special
type of contaminated LCT pegmatite rather than a member of the mixed family.
Keywords: Li-bearing pegmatites, mixed (NYF + LCT) signature, origin, contamination, mixing test, Moldanubian Zone, Czech
Republic.
§	 E-mail address: mnovak@sci.muni.cz
Introduction
The current classification of granitic pegmatites
includes two main petrogenetic families, LCT (enriched
in lithium + cesium + tantalum) and NYF (enriched in
niobium + yttrium + fluorine) (Černý 1991a, Černý &
Ercit 2005, Ercit 2005, London 2008); however, some
pegmatites share mixed (NYF + LCT) geochemical
and mineralogical characteristics, e.g., Høydalen near
Tørdal, Telemark, Norway, and the O’Grady Batholith,
Selwyn plutonic suite, N.W.T., Canada (Černý & Ercit
2005). These pegmatites contain minor to accessory
Li-bearing minerals (lithium micas, elbaite) along with
various accessory Y,REE minerals [e.g., (Nb,Ta,Ti)
oxides, silicates] and they are assigned to a mixed
family. The following possibilities have been considered
for the genesis of the mixed granite–pegmatite systems
(Černý 1991b, Černý & Ercit 2005): “(i) a pristine NYF
magma from depleted crust may become contaminated
by digestion of undepleted supracrustal lithologies,
(ii) the crustal protolith may have been only partially
depleted, and (iii) the anatexis may have affected a
mixed range of depleted and undepleted protoliths”.
The spectrum of genetic possibilities may considerably
expand once various models of NYF-granite derivation
and diverse potential modes of LCT enrichment
1078	 the canadian mineralogist
or external contaminations of the pegmatite-forming
melt are considered (Černý & Ercit 2005, Martin &
De Vito 2005).
The two pegmatites are characterized by the presence
of typical LCT-signature minerals (lithium tourmalines,
lithium micas) and typical NYF-signature minerals
[allanite-(Ce), Y, oxides of REE. Nb, Ta and Ti, primary
Y,REE fluorcarbonates]. They occur in the Moldanubian
Zone, Czech Republic. The lithium-bearing pegmatite
(lithium micas + elbaite) from Kracovice, with Y,REE
minerals, is related to the Třebíč pluton (Němec 1990,
Novák et al. 1999a, Škoda et al. 2006); the contaminated
elbaite-subtype pegmatite Bližná I (Novák et
al. 1997, 1999b) contains common primary REE
minerals. To reveal the factors controlling the origin of
their mixed signatures, we describe (i) the geological
setting of the pegmatites, including geochemistry of
parental granites and host-rock complexes, (ii) results
of a paragenetic study, (iii) the chemical composition
of rocks and minerals, and (iv) mixing tests based on
the whole-rock chemical data.
Granitic Pegmatites of the Moldanubian Zone
and a Summary of the Geological Setting
of the Regions Examined
The Moldanubian pegmatite field is characterized
by numerous granitic pegmatites of different origin and
mineralogy (Černý & Ercit 2005, Novák 2005, Breiter
et al. 2010; Fig. 1). Pegmatites of the rare-element class
are the most abundant and exhibit a high variability in
size, textural differentiation, degree of fractionation
and mineralogy, from barren to highly fractionated
pegmatites with both LCT and NYF signatures. Most
pegmatites of LCT signature are typically enriched in
B with tourmaline (dravite – schorl – foitite – elbaite
– rossmanite – liddicoatite; Novák & Povondra 1995,
Selway et al. 1998, 1999, Novák et al. 1999b, 2004)
as an omnipresent accessory to minor mineral. Both
lepidolite- and elbaite-subtype pegmatites are typical
(Fig. 1). Pegmatites of the NYF family, varying from
primitive allanite-type to more evolved pegmatites
of euxenite type, occur exclusively in the Třebíč and
Fig. 1.  Schematic geological map of the Moldanubian Zone showing the major occurrences of complex Li-bearing pegmatites
(Breiter et al. 2010). Stars: lepidolite-subtype pegmatites, triangles: elbaite-subtype pegmatites, Bližná I (B), circle: Kracovice
(K) pegmatite. ČB: the Čertovo břemeno pluton, T: the Třebíč pluton.
	 the mixed (nyf + lct) signature in granitic pegmatites	 1079
Čertovo břemeno syenite plutons (Fig. 1) and also
contain accessory tourmaline (dravite – schorl – uvite;
Novák et al. 2011). The pegmatites of the rare-element
class (both LCT and NYF) crystallized in a short
period of ~338–333 Ma (Novák et al. 1998, Ertl et al.
2004) and closely followed an episode of high-grade
metamorphism. The NYF pegmatites are accompanied
by contemporaneous mafic calc-alkaline (orogenic
lamprophyres) to peralkaline (orogenic lamproites) dike
intrusions derived from the different parts of the metasomatized
mantle (Krmíček 2010, Krmíček et al. 2011).
Porphyritic, amphibole–biotite melasyenite to quartz
melasyenite and melagranite (durbachite) of the Třebíč
pluton are emplaced in medium- to high-grade metamorphic
rocks of the Moldanubian Zone at an uppercrust
level at P ≈ 2–4 kbar (Novák & Houzar 1996,
Houzar & Novák 2006) and at 334.8 ± 3.2 Ma (Kotková
et al. 2010). Its bulk composition is metaluminous (ASI
in the range 0.85–0.93), with high concentrations of
K2O (5.2–6.5 wt.%), MgO (3.3–10.4%), P2O5 (0.47–
0.98%), Rb (330–410 ppm), Ba (1100–2470 ppm),
U (6.7–26.2 ppm), Th (28.2–47.7 ppm), Cr (270–650
ppm), Cs (20–40 ppm), and high K/Rb = 133–171, but
with unusually low CaO and Sr contents, and a high
Rb/Sr value, 0.8–1.3 (for more details, see Holub et al.
1997, Janoušek et al. 2000). The geochemical signature
as well as isotopic Sr (87Sr/86Sr337 in the range
0.709–0.7125) and Nd (Nd337 = –6.3) data require
an origin from anomalously enriched mantle domains
(Holub 1997, Wenzel et al. 1997, Parat et al. 2010)
perhaps contaminated by the deeply subducted mature
crust (Janoušek & Holub 2007, Lexa et al. 2011). Subsequently,
these magmas were subjected to hybridization
by crustally derived, leucogranitic melts (Holub 1997).
The pegmatite district Černá v Pošumaví, including
the more or less contaminated elbaite-subtype pegmatites
Bližná I and Bližná II, is located in the southern
part of the Český Krumlov Unit, Moldanubian Zone,
Czech Republic (Novák et al. 1997, Černý 2004, Novák
2005, Fig. 1; for details of the regional geology, see
Dallmeyer et al. 1995). In analogy with rare-element
pegmatites elsewhere in the Moldanubian Zone (Ackermann
et al. 2007, Breiter et al. 2010, Gadas et al. 2012),
the pegmatite-forming melts intruded relatively cold
rocks at T in the range 300–450°C and P ≈ 2–4 kbar.
as indicated by common primary petalite at several
South Bohemian pegmatites (Fig. 1). The area features
medium- to high-grade plagioclase–biotite paragneisses
with common intercalations of quartzitic paragneisses,
quartzites, calc-silicate rocks, amphibolites, abundant
metacarbonates and closely associated graphite beds.
Small bodies of leucocratic granites, locally with
nodular tourmaline and with thin tourmaline-rich
veinlets of pegmatite, cut this rock complex ~1.5 km
northwest of the Bližná pegmatite bodies; however, the
parental granite of the Bližná pegmatites is not known.
Two distinct types of metacarbonates were distinguished
in this region (Drábek et al. 1999, Houzar & Novák
2002). (i) Abundant calcite to calcite–dolomite marbles
locally with common silicates form large nodular to
tabular bodies, up to 30 m thick and 1 km long. (ii) Less
common carbonatite-like calcite–dolomite marbles have
been found as relatively thin layers, up to 3–4 m thick
(Drábek et al. 1999, Houzar & Novák 2002). They are
interpreted as metacarbonates from a shallow marine
environment containing a considerable proportion of
volcaniclastic material derived from alkaline volcanism
(Drábek et al. 1999). The amphibolite-facies metamorphism
of carbonatite-like marbles was dated on molybdenite
using the Re–Os method at ~ 495 Ma (Drábek &
Stein 2003). Both types of metacarbonate rocks form
bodies concordant to the volcanosedimentary sequence
and characterized by a highly heterogeneous chemical
and mineralogical composition.
Methods and Samples
The chemical compositions of minerals were
obtained on the Cameca SX 100 at the Joint Laboratory
of Electron Microscopy and Microanalysis, Department
of Geological Sciences, Masaryk University, Brno and
the Czech Geological Survey. Analytical conditions
used were: accelerating voltage 15 kV, and beam current
30 nA. As standards, we used synthetic minerals (for
more details, see Škoda & Novák 2007, Novák et al.
2011). A few electron-microprobe analyses of tourmaline
(Řečice, Ctidružice, part of Bližná and Kracovice)
and micas (Kracovice) were done using the Cameca
Camebax SX–50 instrument, University of Manitoba,
Winnipeg, with a beam diameter of 4–5 mm and an
accelerating potential of 15 kV (for more details see
Selway et al. 1999).
Bulk chemical analyses of rocks were carried out
at the Acme Chemical Laboratories Ltd, Vancouver,
Canada. Concentrations of the major elements were
established by ICP–ES after fusion with lithium borate
flux; concentrations of the trace elements, including
the REE, were established by ICP–MS with lithium
tetraborate fusion.
We used a graphical expression of the general
mixing equation of Langmuir et al. (1978) for the Bližná
I pegmatite: CM = XA 3 CA + (1 – XA) 3 CB, where CM
is the concentration of an element in the contaminated
melt, CA is the concentration of the same element in the
pegmatitic component, CB is the concentration of the
same element in the contaminant component, and XA
corresponds to the fraction of the pegmatitic component
participating in mixing and contamination (0–1). The
mixing equation can be rewritten as: XA = (CM – CB) /
(CA – CB). If mixing occurs, each element considered
should define a straight line in the (CM – CB) versus
(CA – CB) diagram. Subsequently, the slope of the line
gives the mass proportions of the mixture (Fourcade &
Allègre 1981).
1080	 the canadian mineralogist
Samples of rocks and minerals from the Třebíč pluton
and related pegmatites were collected on outcrops and
sporadically from fragments on fields (some pegmatites).
Pegmatites and both types of metacarbonate rocks
from Bližná were accessible in the abandoned graphite
mine Václav in 1991–1997 (Bližná I pegmatite and
host marbles) and in 1994–2007 (Bližná II pegmatite
and carbonatite-like marbles), respectively; currently,
both underground outcrops of the pegmatites are not
accessible. The samples ~0.5–1.0 kg of the individual
units of the granitic pegmatite Bližná I (BLAD, BLA,
BLB) and ~3 kg of metacarbonate rocks, respectively,
were crushed for whole-rock chemical analysis. The
samples of ordinary marble (BLM–1, BLM–2, BLM–3)
were sampled invariably at a distance of 0.2, 0.5 and 1
m from the contact with Bližná I pegmatite; the samples
of carbonatite-like marble (BLK–1, BLK–2, BLK–3)
come from an outcrop located ~200 m northwest from
the Bližná I pegmatite.
Granitic Pegmatites Related
to the Třebíč Pluton
The Třebíč pluton (Fig. 2) is characterized by abundant
intragranitic NYF pegmatites with common biotite
and tourmaline of two distinct varieties (Škoda et al.
2006, Škoda & Novák 2007, Novák et al. 2011): (i)
subhomogeneous allanite-type pegmatites form small
irregular nests and segregations, commonly with a
transitional contact to the host syenogranite; (ii) lenses,
dikes and irregular bodies of simply zoned euxenitetype
pegmatites (with aeschynite- or euxenite-group
minerals; Škoda & Novák 2007) are up to 2 m thick and
several meters long. The euxenite-type Klučov I pegmatite
is characterized by a higher degree of fractionation,
manifested by more abundant B-bearing minerals and
the chemical composition of the tourmaline (Novák et
al. 2011). The symmetrically zoned northwest-trending
pegmatite dike in Kracovice, ~1 m thick and 30 m
long, cuts graphitic gneiss ~300 m west of the edge of
the Třebíč pluton (Figs. 1, 2; Němec 1990, Škoda et
al. 2006). In its most differentiated part, the pegmatite
consists from outer to inner units of: a coarse-grained
granitic unit (Kfs + Pl + Qtz + Bt + Ms), an abundant
graphic unit (Kfs + Qtz ± Bt), evolving to minor blocky
K-feldspar, and an albite complex situated close to a
small quartz core. Major, minor and accessory minerals
typical of the individual types of pegmatites are given
in Table 1.
The most primitive allanite-type pegmatites contain,
along with major quartz, K-feldspar, plagioclase and
biotite, several accessory minerals including tourmaline
(Table 1). Euxenite-type pegmatites are characterized by
presence of Y,REE oxide minerals and several accessory
minerals (Table 1); some pegmatites contain beryl.
The most evolved euxenite-type pegmatite Klučov I is
slightly B-, Mn- and Sn-enriched, and the Kracovice
pegmatite contains Li-bearing minerals, muscovite
and several accessory minerals. An increasing degree
of fractionation from allanite-type pegmatites to the
Kracovice pegmatite is evident in the mineral assemblages
(Table 1).
Tourmaline-supergroup minerals are common accessories
in all pegmatites; hence, their compositional
evolution is a useful tool to reveal the fractionation
trend from primitive allanite-type pegmatites through
euxenite-type pegmatites, including the more evolved
Klučov I pegmatite to the Li-bearing Kracovice pegmatite.
Black tourmaline (dravite – schorl – uvite) generally
shows two trends distinct for the allanite- with
euxenite-type pegmatites and for the euxenite-type
pegmatite Klučov I (Fig. 3). Tourmaline from Kracovice
(Al-rich schorl to Mn-rich elbaite) shows very limited
variation in IVAl, and moderate to high contents of Mn
and F, all increasing from schorl to elbaite. All diagrams
in Figure 3 illustrate the compositional evolution from
intragranitic, less evolved allanite- and euxenite-type
pegmatites through the Klučov I pegmatite to the distal
Li-bearing Kracovice pegmatite.
The compositional trend in micas [only biotite with
moderate variation in Fe/(Fe+Mg) is known in all allanite-
and euxenite-type pegmatites] to more complex
assemblage in Kracovice with biotite, zinnwaldite and
masutomilite + Mn-rich polylithionite (Novák et al.
Fig. 2.  Schematic geological map of the Třebíč pluton
and pegmatite districts (slightly modified from Škoda et
al. 2006). Light grey: melagranite to melasyenite; dark
grey: leucocratic granites locally with tourmaline; dots:
pegmatite occurrences; Kracovice: star.
	 the mixed (nyf + lct) signature in granitic pegmatites	 1081
1999a) yielded high Mn/(Fe+Mn) values, ≤0.87. The
micas also exhibit high F contents, increasing with
the progress of fractionation just as in tourmaline. The
concentrations of Rb and Cs and the Cs/Rb values in
the lithium micas from Kracovice are similar to those
from complex LCT pegmatites in the Moldanubicum
(Černý et al. 1995, Novák & Povondra 1995, Novák
& Černý 1998a, Novák et al. 1999c). The primary
Y,REE minerals involve common allanite-(Ce) in all
intragranitic pegmatites, common AB2O6 minerals
(aeschynite-group and euxenite-group minerals), and
very rare monazite-(Ce) in euxenite-type pegmatites
(for details see Škoda & Novák 2007). The rare ABO4
oxide minerals (fergusonite, samarskite) and monazite(Ce)
+ xenotime-(Y) were identified in the Kracovice
pegmatite. Compositional trends in tourmalines and (Y,
REE, Nb, Ta, Ti)-rich oxide minerals (Figs. 3, 4) as well
as overall mineral assemblages (Table 1) corroborate
the genetic relationship of all pegmatites including the
Kracovice pegmatite to the single granite–pegmatite
system of the Třebíč pluton.
Contaminated Elbaite-Subtype
Pegmatites from Bližná and Associated
Metacarbonate Rocks
The metacarbonate rocks
Two distinct types of metacarbonates include (i)
abundant calcite to calcite–dolomite marbles and
(ii) less common carbonatite-like calcite–dolomite
marbles. (i) Ordinary metacarbonate rocks are texturally
and compositionally heterogeneous, banded,
fine- to medium-grained and locally rich in silicates
(diopside, tremolite, phlogopite > quartz, feldspars,
scapolite, muscovite, forsterite, spinel, tourmaline).
(ii) Less common carbonatite-like calcite–dolomite
marbles also are characterized by a highly heterogeneous
chemical and mineralogical composition (Table
2). They are locally layered and silicate-rich (diopside,
tremolite, phlogopite > quartz, forsterite), with sulfiderich
portions (pyrrhotite, pyrite, molybdenite, chalcopyrite,
galena, sphalerite). Locally common accessory
REE-bearing minerals (Th,REE-rich betafite, euxenite,
uranothorite), barite, ilmenite and zircon (Drábek et al.
1999) are rather randomly distributed. Ordinary marbles
from outcrops near the Bližná I pegmatite are enriched
in silicates; however, almost silicate-free metacarbonates
also are common in this region (Houzar & Novák
2002). Comparing ordinary marbles and carbonatitelike
rocks, the latter exhibits higher Si/Al and Na/K
values, and higher contents of Fe and Mn (Table 2). The
carbonatite-like marbles are characterized by variable
but locally high concentrations of Ba, Sr, Mo, Pb, Cu, Y,
Zr, Nb and REE (see Table 2). The two types of marble
also show distinct REE patterns (Fig. 5).
Geology, internal structure and mineralogy
of the Bližná I and Bližná II pegmatites
The Bližná I pegmatite dike, ~4 m thick and several
tens of meters long, generally northeast-trending and
dipping ~35° to the southeast, cuts silicate-rich ordinary
calcite–dolomite marble (Fig. 6). The dike is enclosed
in the rock sequence overlying a graphite bed, and the
closest known layer of the carbonatite-like marble is
at a distance of ~200 m to the northwest. The contacts
with the host marble are typically sharp except for a
tourmaline-rich exocontact zone described in detail by
Novák et al. (1999b), limited exclusively on the footwall
margin of the pegmatite (Fig. 6).
The textural-paragenetic units include a volumetrically
predominant, commonly coarse-grained
schorl unit (BLA) (Fig. 6) built of grey to bluish grey
perthitic microcline, subordinate quartz, albiteAn4–0
and minor black to brown-black Mg-bearing schorl to
Al-rich schorl. This unit contains randomly distributed
TABLE 1. PRIMARY MINERALS FROM THE INDIVIDUAL TYPES
OF PEGMATITES IN THE TØEBÍÈ PLUTON
____________________________________________________________
allanite-type euxenite-type Kluèov I Kracovice
pegmatites pegmatites
____________________________________________________________
quartz +++ +++ +++ +++
K-feldspar +++ +++ +++ +++
amazonitic Ksp ++ ++ ++
18plagioclase #An +++ +++ +++ +++
albite +++ +++ +++
dark micas +++ +++ +++ +++
muscovite ++
lithium micas +++
garnet ++
topaz ++
actinolite ++ +
dravite ++ ++ +
schorl + ++ +++ +++
elbaite ++
ilmenite ++ ++ ++
pseudorutile + +
titanite ++ ++ +
rutile + + +
niobian rutile + + ++
columbite-(Fe) + +
“wolframoixiolite” +
aeschynite group ++ ++
euxenite group ++ ++
samarskite group ++
fergusonite-(Y) +
scheelite +
allanite-(Ce) ++ ++ ++
monazite-(Ce) + + ++
xenotime-(Y) +
zircon + ++ ++ ++
beryl + +
bazzite +
phenakite +
hambergite ++
herzenbergite +
cassiterite + +
tinzenite +
fluorite + +
pyrite + + + +
____________________________________________________________
Abundance of minerals: +++: major and minor minerals, ++: common
accessory minerals, +: rare accessory minerals.
1082	 the canadian mineralogist
Fig. 3.  Composition of tourmaline from allanite-type pegmatites (blue symbol), euxenite-type pegmatites (red symbol), the
Klučov I pegmatite (black symbol), the Kracovice pegmatite (yellow symbol): a) (Na+K) – Ca – X-site vacancy plot; b)
Fetot–Mg–Al triangle; c) Fetot versus Mn; d) F versus Mn; e) Ca versus Al; f) Na versus Al. (in part modified from Novák
et al. 2011).
	 the mixed (nyf + lct) signature in granitic pegmatites	 1083
diopside-bearing nests (BLAD), ~20 cm in diameter
(Fig. 6), composed of feldspars, quartz, subhedral, elongate
grains of white diopside, up to 3 cm in long. The
schorl unit evolves to the elbaite–liddicoatite unit (ELU)
as nests, up to ~30 cm in diameter (Fig. 6). The grain
size increases from ~1–3 cm in the schorl unit to ~10
cm in the elbaite–liddicoatite unit. Blocky K-feldspar,
quartz and graphic textures (K-feldspar + quartz) and
brown-yellow-pink tourmaline are locally present, as
well as exceptional small fragments of massive graphite.
Fig. 4.  Chemical composition of aeschynite-, euxenite-, samarskite-group minerals and fergusonite. (A-site and B-site
occupancy). (in part modified from Škoda & Novák 2007).
Fig. 5.  Chondrite-normalized REE patterns of the rocks from the Bližná area. Chondrite data from Taylor & McLennan (1985).
1084	 the canadian mineralogist
TABLE 2. CHEMICAL COMPOSITION OF ROCKS IN BLIŽNÁ
___________________________________________________________________________________
BLAD BLA BLB BLM-1 BLM-2 BLM-3 BLK-1 BLK-2 BLK-3 extreme
values
___________________________________________________________________________________
2SiO wt% 69.16 75.93 63.39 42.74 33.29 35.80 21.14 13.74 12.96
2TiO 0.28 0.27 0.08 0.39 0.14 0.15 0.04 0.05 0.05
2 3Al O 13.67 13.29 18.38 8.14 2.75 1.82 0.42 0.44 0.29
2 3Fe O (tot) 0.25 0.10 0.15 4.12 1.99 1.45 7.59 3.05 3.36
2 3Cr O 0 0 0 0 0 0 0 0 0
CaO 5.87 3.56 4.71 24.22 34.01 35.16 32.37 39.10 44.42
MgO 2.34 0.31 0.50 10.90 4.83 9.58 17.53 11.54 5.38
MnO 0.27 0.04 0.07 0.70 0.07 0.13 0.24 0.35 0.43
2Na O 2.29 3.07 7.53 0.28 0.22 0.35 0.65 0.82 0.58
2K O 4.12 2.34 1.12 2.10 1.09 0.19 0.07 0.20 0.07
2 5P O 0.04 0.03 0.20 0.80 0.15 0.06 0.05 0.03 0.03
LOI 1.60 1.00 4.00 6.80 21.30 15.10 19.50 29.90 31.30
Total 99.89 99.94 100.13 101.19 99.84 99.79 99.60 99.22 98.87
W ppm 7.2 118.8 0.7 1.5 1.2 3.2 0.8 0 2.8
Nb 17.2 26.9 15.4 6.4 2.8 4.5 6.1 10.9 10.6 393 (a)
Ta 4.9 7 9.7 0.5 0.3 0.3 0 0 0 58 (a)
V 30 0 0 54 28 36 30 49 68
U 10.1 42.4 11 2.4 1.3 7 0.2 1 2.8 461 (a)
Th 1.7 14.4 6.3 5.6 2.3 2.7 3.6 24.7 127.8
Zr 67.2 23 21.4 7.6 26.4 37.6 8.7 20.4 19.8 4214 (a)
Hf 2.2 1.1 2.3 2.1 0.8 1.3 0.2 0.2 0.2
Sn 10 5 15 2 1 5 0 1 0
Sc 81 10 5 9 3 4 0 0 0
Ga 18.8 2.9 35.5 1.8 3.4 9.6 1.2 2 1.9
Sr 54.7 44.5 28.8 163.3 237.9 11.4 273.4 1264 2001
Ba 105 17 13 201 81 35 316 1648 4195
Be 16 19 6 1 0 8 5 11 12
Rb 26.8 14.8 77.1 86 47.5 12.9 1.1 3.7 1.4
Cs 7.6 4.3 7.9 5.1 2.6 0.5 0.1 0.1 0
Y 33 31.7 8.7 17.4 10 23.8 21.3 239.9 416
La 9.9 10.3 14.7 16.9 7.8 31.4 6.2 41.4 71.3
Ce 26.3 28.1 26.4 34.9 15.9 52.4 19.3 151.1 260
Pr 3.84 3.98 2.77 4.44 2.05 5.1 3.13 26.13 45.31
Nd 15.4 14.3 8.7 17.7 8.6 18.3 15.7 140.8 239.7
Sm 3.44 2.81 1.23 3.34 1.76 3.23 5.04 45.52 78.55
Eu 0.28 0.18 0.12 0.51 0.54 1 1.78 15.66 27.04
Gd 3.23 2.53 0.79 2.98 1.9 2.85 4.63 48.19 83.75
Tb 0.71 0.6 0.16 0.49 0.31 0.53 0.8 7.94 13.49
Dy 4.98 4.21 1.14 3 1.75 2.85 3.96 43.44 76.68
Ho 1.14 1.1 0.25 0.65 0.39 0.67 0.68 7.77 13.94
Er 3.71 3.54 0.93 1.94 1.09 2.14 1.61 19.33 35.42
Tm 0.66 0.77 0.22 0.29 0.15 0.39 0.23 2.58 4.7
Yb 4.93 5.89 2.19 1.8 0.99 2.86 1.2 13.91 27.15
Lu 0.69 0.86 0.4 0.27 0.15 0.5 0.13 1.6 3.29
As 5 0 0 6.7 2.1 0.9 0 0 0
Se 0 0 0 0.7 0 0 0.7 1.4 1.9
Bi 0.1 0 0 0.3 0.1 0.8 3 5.8 1.9
Co 0.5 0.3 0.5 10 9.4 3.8 13.8 3.9 4.5
Mo 0.2 0 0 0.9 1.9 8.4 25 315.1 377.2 1930 (b)
Cu 0.4 0.3 0.9 35.1 13.8 6.5 257.6 12 7.2 302 (b)
Pb 4 4.2 1.2 5.7 4.3 25.6 258 323.1 272.7 1909 (b)
Zn 5 3 0 12 4 18 66 69 21 255 (b)
Ni 0.6 0.8 0.8 24.8 14.1 16.8 4.3 4.8 2.1
Cd 0 0 0 0 0 0 0.5 0.9 1.9
Ag 0 0 0 0 0 0.2 0.5 0.9 0.7
___________________________________________________________________________________
Samples: pegmatite: BLA: schorl unit, BLAD: diopside-bearing nests, BLB: uvite–liddicoatite unit, BLM-1,
BLM-2, BLM-3: samples of ordinary marble collected from the body cut by pegmatite, BLK-1, BLK-2,
BLK-3: carbonatite-like marbles. The extreme values for selected trace-elements from carbonatite-like
marbles taken from: a) Houzar & Novák (2002) and b) Drábek et al. (1999).
	 the mixed (nyf + lct) signature in granitic pegmatites	 1085
The uvite–liddicoatite unit (ULU) adjacent exclusively
to the tourmaline-rich reaction zone (Fig. 6) differs
from the other units by lower amount of quartz and
K-feldspar, olive green to pink tourmaline, but mainly
by minor primary calcite; the Y,REE-bearing minerals
are absent. Chemical compositions of rocks (Table 2)
imply apparent contamination by Ca in all individual
pegmatite units. The normalized REE patterns indicate
a pronounced negative Eu anomaly and a slight enrichment
in the middle REE mainly for the samples BLAD
and BLA (Fig. 5).
The simply zoned elbaite-subtype pegmatite Bližná
II, a dike up to 6 m thick and ~100 m long, generally
northwest-trending and dipping ~70° to the northeast, is
hosted mainly in graphite-bearing biotite gneiss. It crops
out in two places: the chimney K15 and on the surface
outcrop (Černý 2004) ~200–250 m south of the Bližná
I pegmatite. Three distinct textural-paragenetic units
were found rather randomly distributed: a dominant
coarse-grained unit (Kfs + Ab + Qtz) with abundant
brown to black dravite–schorl and rare pink elbaite, a
minor graphic unit (Pl + Qtz) with dravite–schorl and
olenite, a blocky unit (Kfs + Qtz) and a rare albite-rich
unit with primary muscovite, most accessory minerals
and black schorl to pink elbaite. The Bližná I and Bližná
II pegmatites contain abundant tourmaline along with
major K-feldspar, plagioclase and quartz; Bližná I is
mica-free and contains more common Ca(Mg)-enriched
minerals (Table 3).
Two rather distinct assemblages with REE minerals
were distinguished in the Bližná I pegmatite. Yellowbrown
tabular crystals of bastnäsite-(Ce), up to ~1–2
mm in diameter, are enclosed in (Ca,Mg,Mn)-rich
schorl to uvite and associated with allanite-(Ce),
titanite and parisite-(Ce) in a diopside-bearing nest
(Fig. 7a). Well-developed, yellow to wax yellow,
tabular crystals of bastnäsite-(Ce), up to 5 mm in size
(Fig. 7b), from elbaite–liddicoatite unit are completely
enclosed or closely associated with zoned grains of
brown (Ca,Mg,Mn)-rich schorl–elbaite to pink Mn-rich
elbaite–liddicoatite. Most minerals contain very thin
veinlets of late minerals (REE fluorocarbonates, REEbearing
epidote, stillwellite-(La) (?) and dravite; Fig.
7b). In the Bližná II pegmatite, very rare, small inclusions
of thortveitite associated with tourmaline were
found at the surface outcrop (Černý 2004) and represent
along with rare accessory monazite-(Ce) and zircon the
only (Y,REE)-bearing mineral.
The pegmatites differ in chemical composition of
tourmaline (Fig. 8) as well. Tourmaline from Bližná I
is typically Ca-enriched and has elevated Mn in yellow
to brown elbaite (Fig. 8d). Tourmaline from the surface
outcrop at Bližná II is similar to that at Bližná I, showing
limited to strong enrichment in Ca. In the underground
outcrop at Bližná II, tourmaline is less contaminated by
Ca (Figs. 8b, c) but strongly Mn-enriched (≤1.28 apfu;
Fig. 8d). In general, the tourmaline crystals exhibit
chemical compositions similar to those from ordinary
Fig. 6.  Cross section through the Bližná I pegmatite enclosed in ordinary marble; BLA:
schorl unit, ELU: elbaite–liddicoatite unit, BLAD: diopside-bearing nests, BLB:
uvite–liddicoatite unit with narrow tourmaline-rich contact zone (modified from Novák
et al. 1999b).
1086	 the canadian mineralogist
elbaite-subtype pegmatites of the Moldanubian Zone
(Fig. 8; Novák & Povondra 1995, Novák et al. 1999b,
Novák 2000). The Bližná I pegmatite and the Bližná II
surface outcrop are close to the Ca-contaminated Řečice
pegmatite enclosed in pyroxene gneiss (Novák 1999,
Novák et al. 1999c), with a variable degree of external
contamination by Ca and Mg.
Discussion
Comparison of the Kracovice pegmatite
with similar Li-bearing (NYF + LCT) pegmatites
and origin of the mixed signature in the Třebíč
granite–pegmatite system
The Li-bearing Kracovice pegmatite exhibits some
mineralogical features (common lithium micas and
elbaite) similar to spatially related complex (LCT)
pegmatites of the Moldanubian Zone (Fig. 1). However,
minerals from both groups have fairly distinct compositional
trends and substitution mechanisms, signifying
an absence or low participation of Al in tourmaline
and a high participation of R2+ (Fe,Mn) in the lithium
micas in Kracovice (Černý et al. 1995, Novák et al.
1999a, 1999c, Novák 2000). In addition, the garnet has
elevated contents of Y, the feldspars are P-poor, apatite
is very rare, amblygonite or montebrasite is absent, and
(Y,REE,Nb,Ta,Ti)-rich oxide minerals predominate over
columbite-group minerals (Table 1). The Kracovice
pegmatite also is entirely different from peraluminous,
B-rich, (Li,F,REE)-poor anatectic pegmatites from this
region (Cempírek et al. 2010, Gadas et al. 2012), for
example in the isotopic composition of B in tourmaline
(Míková et al. 2010).
TABLE 3. PRIMARY MINERALS FROM THE INDIVIDUAL PEGMATITES
AND THEIR TEXTURAL-PARAGENETIC UNITS (OUTCROPS)
IN BLIŽNÁ I AND BLIŽNÁ II
____________________________________________________________
Bližná I Bližná II
_______________________ __________
unit-outcrop BLA BLAD ELU BLB under- surface
ground
____________________________________________________________
quartz +++ +++ +++ +++ +++ +++
K-feldspar +++ +++ +++ +++ +++ +++
albite +++ + +++ +++ +++ +++
33plagioclase #An + +++ + + +++
muscovite ++
spessartine ++ +
schorl ++ + + +++ +
dravite + + ++ +
uvite + ++
elbaite ++ + +
liddicoatite + +
olenite +
axinite + + +
datolite +
dumortierite +
diopside +++ +
titanite ++ + +
epidote +
calcite +
allanite-(Ce) +
bastnäsite-(Ce) + +
parisite-(Ce) +
thortveitite +
zircon + + + +
monazite-(Ce) + + +
apatite + +
columbite-(Mn) +
pyrochlore +
rutile + +
niobian rutile +
scheelite +
cassiterite +
pyrite + +
____________________________________________________________
Abundance of minerals: +++: major and minor minerals, ++: common
accessory minerals, +: rare accessory minerals.
Fig. 7.  BSE images of REE minerals from the Bližná I pegmatite. a) Homogeneous equidimensional grain of bastnäsite (Bsn)
enclosed in uvite (Uv) and associated with titanite (Ttn), allanite (Aln) and altered parisite (Pst). b) Fragment of euhedral
grain of heterogeneous bastnäsite (bright) in elbaite–liddicoatite. Late veining: dravite (dark) and stillwellite-(La)? (bright).
	 the mixed (nyf + lct) signature in granitic pegmatites	 1087
The Kracovice pegmatite has mineralogical features
similar with the mixed NYF + LCT pegmatite Høydalen
near Tørdal, Telemark, Norway (Bergstøl & Juve 1988,
Raade et al. 1993) and with the Leduc mine, Gatineau
River area, Quebec, Canada (Hogarth et al. 1972,
Ercit 2005). However, a lack of mineralogical and
geochemical data mainly from the second locality does
not enable a more detailed comparison. The Kracovice
pegmatite, characterized by high activities of B and F,
and very low activity of P, is a product of geochemical
fractionation of mixed pegmatite-forming melt derived
from the orogenic I-type Třebíč pluton. Contamination
(LCT) from the host-rock sequence is rather unlikely
because of the absence of textural indications (sharp
contacts with host gneiss, absence of any xenoliths) and
estimated very short transport from parental granite to
the site of emplacement. In addition, leucocratic tourmaline-bearing
granites developed along the border of
the Třebíč pluton (Fig. 2), which the pegmatite-forming
melt very likely passed through, are rather primitive
(Buriánek & Novák 2007) to cause external LCT-type
contamination.
The pegmatites of the O’Grady Batholith, Selwyn
plutonic suite, N.W.T., Canada, including the Li-enriched
ones (Ercit et al. 2003), are very similar to the Třebíč
pluton pegmatites and to the Kracovice pegmatite in
Fig. 8.  Composition of tourmaline from selected elbaite-subtype pegmatites of the Moldanubian Zone: Bližná I (yellow
triangles), Bližná II underground (red triangles), Bližná II surface (black triangles), Řečice (open squares), Ctidružice (blue
squares). Both latter localities are given to demonstrate typical examples of contaminated and non-contaminated elbaitesubtype
pegmatites from the Moldanubian Zone: a) (Na+K) – Ca – X-site vacancy plot; b) Fetot–Mg–Al triangle; c) Ca versus
Al; d) F versus Mn.
1088	 the canadian mineralogist
particular. This granite (hornblende quartz syenite)
has geological, geochemical and petrographic features
akin to the Třebíč pluton, such as major, minor and
trace-element populations, porphyritic texture, depth of
emplacement, and common scheelite-bearing skarns in
the contact aureole. Its mixed geochemical characteristics
are explained by a similar process of granite origin
as in the Třebíč pluton: contamination of mantle-derived
melt by undepleted crust (Coulson et al. 2000). Both
pegmatite suites have a comparable evolution from less
evolved pegmatites with mild to strong NYF signature
to most evolved Li-enriched pegmatites with elbaite
+ lithium-dominant micas. Abundant Ti-rich minerals
(ilmenite, rutile, pseudorutile, titanite) are characteristic
of both suites. The enrichment in Cs (20–40 ppm:
Třebíč pluton, 20 ppm: O’Grady Batholith) is manifested
by a nanpingite-like mica, Cs-enriched chabazite
and pollucite in pegmatites of the O’Grady Batholith
(Ercit et al. 2003) and by Cs-enriched beryl (Novák &
Filip 2010) and ltihium-dominant micas with up to 1.34
wt.% Cs2O in the Třebíč pluton. Also, an enrichment in
W is typical (7–8 ppm: Třebíč pluton, 8 ppm: O’Grady
Batholith); scheelite and W-enriched stibiocolumbite
are known in the O’Grady Batholith, whereas, scheelite,
“wolframoixiolite” and W-enriched (Y,REE,Nb,Ta,Ti)rich
oxide minerals are found in the Třebíč pluton,
respectively (Škoda et al. 2006, Škoda & Novák 2007).
Common W-bearing minerals in both granite–pegmatite
systems open a potential use of W as an indicator of the
mixed signature of a pegmatite. However, W is a typical
trace to minor element in (Nb,Ta,Ti)-oxide minerals in
both NYF (Škoda et al. 2006, Škoda & Novák 2007)
and in LCT pegmatites (e.g., Novák & Černý 1998b,
2001, Černý et al. 2007, Novák et al. 2008, Cempírek
et al. 2010) in the Moldanubian Zone.
The Třebíč pluton and O’Grady Batholith represent
granite–pegmatite systems with a similar origin of
parental granite and geochemistry. The evolution from
less evolved but pristine NYF pegmatites to more
evolved Li-bearing pegmatites with a mixed signature
at both regions is likely enhanced by the fractionation
process, in which the highly incompatible Li remains
until the late stages of primary crystallization relative to
the LREE, as is typical for more primitive NYF pegmatites.
Based on the geochemical and mineralogical data,
the granite–pegmatite system of the Třebíč pluton,
Moldanubicum, may be established along with the
O’Grady Batholith, Selwyn plutonic suite (Ercit et al.
2003), as typical examples of mixed granite–pegmatite
systems (cf. Černý & Ercit 2005, Simmons & Webber
2008). Remarkable similarities in the concentrations
of some trace elements (e.g., Cs, W) in the parental
granite and their presence in relevant accessory minerals
from pegmatites imply that highly evolved pegmatites
carry specific compositional features (fingerprints) of
their parental granites throughout their overall crystallization
up to the tail-end of primary crystallization
(London 2008). The granite–pegmatite system of the
Třebíč pluton differs from most typical NYF and mixed
granite–pegmatite systems (Černý & Ercit 2005) by
evident orogenic character typical for all ultrapotassic
intrusions of this region (e.g., Žák et al. 2005, Verner et
al. 2006, Janoušek & Holub 2007, Kotková et al. 2010,
Krmíček et al. 2011). Such granite–pegmatite systems
in ultrapotassic granites and related NYF-to-mixed
granitic pegmatites have not yet been examined; they
show that I-type synorogenic granites may generate
pegmatites with a NYF-to-mixed signature.
Origin of the mixed (NYF + LCT) signature
in the Bližná I pegmatite and a role of external
contamination in the origin of granitic pegmatite
The evolved LCT pegmatite-forming melt from
Bližná consumed and completely dissolved fragments
of carbonatite-like marbles with a strong NYF-like
geochemical signature during its ascent from the
parental intrusion to the site of emplacement. Owing
to a rather short transport of the melt from the site of
contamination (likely hundreds of m; Fig. 9), the melt
was not entirely homogenized, which can be seen from
the heterogeneous distribution of diopside-bearing nests
(BLAD; strongly digested fragments of carbonatitelike
marbles) within the schorl unit (Fig. 6). Further
evidence for pre-emplacement contamination by Ca,
Mg, and the REE include the chemical composition of
REE-bearing minerals rich in Ca(Mg) (parisite, allanite),
and their close spatial association with Ca(Mg)rich
minerals (diopside, uvite, titanite, liddicoatite). For
the origin of the diopside-bearing nests, a simplified
reaction describing contamination of the pegmatiteforming
melt by carbonate rock is given:
3CaMg(CO3)2 + NaAlSi3O8 +
NaFe3Al6Si6O18(BO3)3(OH)4 + SiO2 = CaMgSi2O6
+ CaAl2Si2O8 + CaFe2Mg2Al5Si6O18(BO3)3(OH)4
+ 6 CO2 + Na2O + FeO.
Dolomite is used as a contaminant, anorthite is present
as a component in plagioclase (Table 3); for the tourmaline
produced, a Fe-rich uvite composition is used
for simplification, and minor Ti, Mn and F present in
tourmaline (Novák et al. 1999b) are ignored.
Geochemical modeling offers further evidence
for contamination of the pegmatite-forming melt by
carbonatite-like marble. The best fit in the mixing test
was obtained between the dominant schorl unit (sample
BLA) as a pegmatitic component (SiO2 = 76.74 wt.%;
MgO = 0.31 wt.%; recalculated on a volatile-free
basis) and carbonatite-like marble (sample BLK–1)
as a contaminant, respectively (SiO2 = 26.39 wt.%;
MgO = 21.89 wt.%). The diopside-bearing nests are
considered to be the product of contamination (sample
BLAD; SiO2 = 70.36 wt.%; MgO = 2.38 wt.%). In the
	 the mixed (nyf + lct) signature in granitic pegmatites	 1089
(CM – CB) versus (CA – CB) diagram, the main oxides
and REE define a straight mixing line with an excellent
correlation (R = 0.998; Fig. 10). Consequently, it
is reasonable to consider that the diopside-bearing nests
are products of melt contamination by marble with a
carbonatite-like geochemical signature. The degree of
contamination by this contaminant component is only
~10% in this particular case.
The Bližná I pegmatite is characterized by a high
activity of B, but rather low activities of F and P. The
pre-emplacement external contamination in Y and the
REE of the LCT melt in the Bližná I pegmatite (Figs. 9,
10) is a unique process, which has no analogy in nature
insofar as we know. Its scarcity may be explained by
very low probability to mobilize Y, REE, Nb, Ta, and
other HFS elements in fluids at P–T conditions typical
for generation and ascent of pegmatites with LCT
signature in the upper crust (Martin & De Vito 2005),
and the rarity of rocks with a strong NYF-signature
such as carbonatite-like marble from Bližná in supracrustal
complexes. The Ca(Mg)-contaminated Bližná II
pegmatite enclosed in gneiss exhibits a lower but variable
degree of pre-emplacement contamination within a
single dike and obviously manifests high variability in
external contamination of pegmatites within this region.
Martin & De Vito (2005) described several examples
of hybrid NYF + LCT pegmatites from Madagascar,
where dominant contamination of pegmatites in calcium
Fig. 9.  Strongly schematic sketch showing pre-emplacement contamination of the
pegmatite-forming melt of the Bližná I pegmatite by carbonatite-like marble. A:
trapping of fragments of carbonatite-like marbles + very rare graphite fragments during
forcible ascent of melt to the site of emplacement; B: dissolution of marble fragments
and partial homogenization of the melt during the transport to the site of emplacement;
C: crystallization of incompletely homogenized pegmatite-forming melt. The sketch
is not in scale.
1090	 the canadian mineralogist
from host rocks played a significant role.Although these
pegmatites are geochemically quite strange, they likely
represent products of ordinary external contamination
from supracrustal host metasedimentary complexes rich
in carbonates (Novák 2007). However, this contamination
by Ca has geochemical character strikingly distinct
from NYF or LCT characteristics. Similar contamination
by Ca(Mg,Fe) was described from several pegmatites
in Czech Republic: contamination in Ca and Mg
from serpentinite and rodingite in Ruda nad Moravou
(Novák & Gadas 2010); contamination in Mg from
serpentinite in Věžná I pegmatite (Černý & Povondra
1966, Novák 1998, Novák et al. 2003, Dosbaba &
Novák 2012), and contamination by Ca and Fe from
a Fe-rich skarn in Vlastějovice (Kadlec 2007, Breiter
et al. 2010). A role of contamination (commonly Ca,
Mg) from host rocks or from channelways, through
which the pegmatite-forming melts were passing to
the site of emplacement (Novák 2007), should be
routinely included in discussions of pegmatite origin
in the cases where unusual bulk-compositions or, more
commonly, strange compositions of individual minerals
are observed. Up to now, significant contamination
has been documented almost exclusively in relatively
small bodies of pegmatite cutting rocks with contrasting
chemical composition (e.g., Černý & Povondra 1966,
Martin-Izard et al. 1995, Novák et al. 1999b, Tindle
et al. 2002, Breiter et al. 2010, Novák & Gadas 2010,
Kuznetsova et al. 2010). Only minor contamination
by Ca, Mg, and Ti in tourmaline and columbite was
decribed from the outer zones of the large Tanco pegmatite,
southeastern Manitoba, enclosed in metagabbro
(Selway et al. 2000, van Lichtervelde et al. 2006). Only
contamination by major and important minor elements
(e.g., Ca, Mg, Fe, Ti) is feasible. If we compare the
concentrations of Ca, Mg and Fe in host rocks (marbles,
serpentinite, Fe-rich skarn) relative to their concentrations
in minerals from the contaminated pegmatites
(Novák et al. 1999b, Novák & Gadas 2010, Breiter et al.
2010), we can hardly expect detectable contamination
by trace elements from host rocks without a significant
contamination by major elements.
Acknowledgements
The authors thank the reviewers Saskia Erdmann
and Mona-Lisa Sirbescu and the Guest Editor David
London for constructive criticism that considerably
improved the manuscript. The authors also thank
J.B. Selway for carrying out chemical analyses of
some minerals from Kracovice and V. Janousek for
unpublished results of chemical analyses of the Třebíč
granites. Milan Novák gratefully acknowledges his
mentor, Professor Petr Černý, University of Manitoba,
Winnipeg, for his outstanding contribution to research
on granitic pegmatites, their minerals and origin, as well
as to the way of thinking about them. His teachings also
indirectly but significantly influenced the approach to
research on pegmatites of his students, including those
participated in this paper (RS, PG, PČ). This work was
Fig. 10.  Distribution of major and minor oxides and REE in the (CM – CB) versus (CA
– CB) diagram of Fourcade & Allègre (1981). The pegmatitic component corresponds
to the sample BLA, the contaminant component, to the sample BLK–1, and the mixed
component, to the sample BLAD (see also Table 2 and Fig. 5).
	 the mixed (nyf + lct) signature in granitic pegmatites	 1091
supported by research project GACR P210/10/0743 to
MN, RS and PG.
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