ORIGINAL PAPER
Lattice-preferred orientations of late-Variscan granitoids
derived from neutron diffraction data: implications
for magma emplacement mechanisms
Axel Mu¨ller • Bernd Leiss •
Klaus Ullemeyer • Karel Breiter
Received: 6 October 2009 / Accepted: 6 August 2010
 Springer-Verlag 2010
Abstract The lattice-preferred orientation (LPOs) of two
late-Variscan granitoids, the Meissen monzonite and the
Podlesı´ dyke granite, were determined from high-resolu-
tion time-of-flight neutron diffraction patterns gained at the
diffractometer SKAT in Dubna, Russia. The results dem-
onstrate that the method is suitable for the LPO analysis
of polyphase, relatively coarse-grained (0.1–6 mm) rocks.
The Meissen monzonite has a prominent shape-preferred
orientation (SPO) of the non-equidimensional minerals
feldspar, mica and amphibole, whereas SPO of the Podlesı´
granite is unapparent at the hand-specimen scale. The
neutron diffraction data revealed distinct LPOs in both
granitoids. The LPO of the non-equidimensional minerals
feldspar, mica and amphibole developed mainly during
magmatic flow. In the case of the Meissen monzonite, the
magmatic flow was superimposed by regional shear tec-
tonics, which, however, had no significant effect on the
LPOs. In both samples, quartz shows a weak but distinct
LPO, which is atypical for plastic deformation and differ-
ent in the syn-kinematic Meissen monzonite and the post-
kinematic Podlesı´ granite. We suggest that, first of all, the
quartz LPO of the Meissen monzonite is the result of ori-
ented growth in an anisotropic stress field. The quartz LPO
of the Podlesı´ granite, which more or less resembles a
deformational LPO in the flattening field of the local strain
field, developed during magmatic flow, whereby the
rhombohedral faces of the quartz crystals adhered to the
(010) faces of aligned albite and to the (001) faces of
zinnwaldite. Due to shape anisotropy of their attachments,
the quartz crystals were passively aligned by magmatic
flow. Thus, magmatic flow and oriented crystal growth are
the major LPO-forming processes in both granitoids. For
the Meissen monzonite, the solid-state flow was too weak
to cause significant crystallographic re-orientation of the
minerals aligned by magmatic flow. Finally, the signifi-
cance of our results for the evaluation of the regional
tectonic environment during magma emplacement is dis-
cussed. The discussion on the regional implications of the
more methodologically oriented results provides the basis
for future, more regionally aimed studies in view of the
fabric characteristics of such plutons and their developing
mechanisms.
Keywords Neutron diffraction  Lattice-preferred
orientation  Shape-preferred orientation  Magmatic flow 
Podlesı´ granite  Meissen Massif
Introduction
Preferentially oriented minerals are a ubiquitous feature of
granitic plutons (e.g. Bouchez 1997). However, parameters
A. Mu¨ller (&)
Geological Survey of Norway,
Postboks 6315 Sluppen, Trondheim 7491, Norway
e-mail: Axel.Muller@ngu.no
B. Leiss
Geowissenschaftliches Zentrum Go¨ttingen,
Goldschmidtstr. 3, 37077 Go¨ttingen, Germany
e-mail: bleiss1@gwdg.de
K. Ullemeyer
Institut fu¨r Geowissenschaften, Universita¨t Kiel,
Otto-Hahn-Platz 1, 24118 Kiel, Germany
e-mail: kullemeyer@ifm-geomar.de
K. Breiter
Institute of Geology, v.v.i.,
Academy of Sciences of the Czech Republic,
Rozvojova´ 269, 16500 Praha 6, Czech Republic
e-mail: breiter@gli.cas.cz
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DOI 10.1007/s00531-010-0590-6
Int J Earth Sci (Geol Rundsch) (2011) 100:1515–1532
/ Published online: 1 September 2010
controlling type and intensity of the preferred orientations
in granitic rocks are manifold, and discussion about their
significance is still controversial (Paterson et al. 1989,
1998; Schulmann et al. 1997; Vernon 2000; Sen and
Mamtani 2006; Zˇa´k et al. 2008). Two main categories
of mineral-preferred orientations are recognised: shape-
preferred orientation (SPO) and lattice-preferred orientation
(LPO; e.g. Shelley 1993). SPO describes the anisotropic
spatial arrangement of the long and/or short axis of elon-
gated, oblate, platy or flaky (‘non-equidimensional’) min-
erals. LPO describes the anisotropic spatial arrangement of
the crystal lattices in a population of mineral grains. Some
mineral-preferred orientations consist either of a LPO or
a SPO; others contain both these elements. SPOs of
non-equidimensional mineral grains such as feldspar
phenocrysts and mica flakes are fairly obvious at the hand-
specimen scale or in thin sections and define magmatic
foliations. LPOs are less obvious; hence, optical universal
stage (U-stage) and diffraction measurements or indirect
methods such as anisotropy of magnetic susceptibility
(AMS) measurements have to be applied to quantify the
characteristics of the preferred orientation.
LPOs and SPOs of granitic rocks can be caused by
magmatic flow, solid-state flow, oriented crystal growth
and combinations of these processes (e.g. Blumenfeld and
Bouchez 1988). Vernon (2000) defined end-member cri-
teria, which are evident for magmatic flow and solid-state
flow, respectively. Magmatic flow causes alignment of
non-equidimensional mineral grains in granite melts by
means of passive grain rotation. Solid-state flow in syn-
kinematic granites causes crystallographic alignment of the
mineral grains due to intracrystalline slip, rotation recrys-
tallisation and sub-grain formation. Fabrics reflecting
transitional conditions between magmatic and solid-state
flow are difficult to distinguish from the rock fabric, e.g.,
because of strain partitioning into interstitial melt (Paterson
et al. 1998). Hence, careful distinction and characterisation
of flow-induced fabrics in magmatic rocks are essential
for understanding the timing, architecture, deformation
mechanisms and tectonic constraints of pluton emplace-
ment. Another process causing LPO and/or SPO is oriented
crystal growth during magma solidification after magma
emplacement. The unidirectional solidification fabric is a
typical example of macroscopically visible LPO resulting
from oriented crystal growth (e.g. Shannon et al. 1982;
Kirwin 2005). The term ‘unidirectional solidification
fabric’ refers to multiple, sub-parallel layers of mm- to
dm-scale comb crystals oriented perpendicular to the layers
(e.g. Shannon et al. 1982). In granitoid rocks, the comb
crystals are usually parallel or sub-parallel to a nearby
intrusion–wallrock or sub-intrusion–intrusion contact
(e.g. Kirwin 2005).
Sander (1929) introduced the statistical analysis of
quartz c-axes orientations in syn-kinematically emplaced
granites using the U-stage. Sander’s and most of the later
studies of quartz orientation in plutons are from orogenic
settings, in which the host rocks underwent regional
deformation contemporaneously with magma emplace-
ment. The LPO of quartz in these syn-kinematic granites
may be explained by magmatic flow superimposed by
solid-state flow during the final stage of magma solidifi-
cation and/or post-crystallisation deformation (e.g. Phillips
1965; Hobbs et al. 1976; Vernon 1976; Gapais and Barb-
arin 1986; Paterson et al. 1989; Vernon 2000 and refer-
ences therein). In most of these examples, it remains
unclear whether the LPO of quartz records magma flow
(intraplutonic magma dynamics) or contemporaneous
regional tectonics or both. Maroscheck (1933), Watznauer
and Behr (1966), Behr (1967, 1968), Mierzejewski (1968)
and others demonstrated the presence of quartz LPOs in
late-Variscan post-kinematic granites in the Bohemian
Massif. However, they could not adequately explain the
mechanisms of LPO formation.
The first petrofabric analyses on quartz applying time-of-
flight (TOF) neutrons were carried out by Bankwitz et al.
(1985) and Damm et al. (1990). In this study, analyses of the
LPOs of all rock-forming minerals in two granitic rocks
were performed at the SKAT-diffractometer at the pulsed
reactor IBR-2 in Dubna, Russia (Ullemeyer et al. 1998). The
two granitoids are the Meissen monzonite of the Elbe Zone
at the NE border of the Eastern Erzgebirge in Germany and
the Podlesı´ dyke granite of the Western Krusˇne Hory
(Western Erzgebirge) in Czech Republic. The Erzgebirge
and the Elbe Zone are located at the northern margin of the
Bohemian Massif and form parts of the Saxothuringian Zone
of the Variscan orogeny. The Meissen monzonite syn-
kinematically intruded the Elbe Zone at 334 ± 3 Ma
(Hofmann et al. 2009), whereas the Podlesı´ dyke granite was
emplaced during a quite passive post-orogenic tectonic
event at 311 ± 1 Ma (Breiter et al. 2005; Fig. 1).
The aims of the study were as follows:
• To test the applicability of neutron diffraction method for
LPO analysis of medium- to coarse-grained and poly-
phase rocks with low-symmetrical minerals, such as
granitoids.
• To examine the effect of magmatic flow, oriented
crystal growth and solid-state flow on the LPO forma-
tion in granitoids.
• To utilise LPO analyses for the better understanding of
crystallisation and fabric development during magma
emplacement.
• To discuss implications for the regional tectonic
environment during magma emplacement.
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Int J Earth Sci (Geol Rundsch) (2011) 100:1515–15321516
Geological setting and petrography
Meissen monzonite
The Meissen monzonite represents the oldest and main
intrusion stage of the late-Variscan Meissen Massif NW of
Dresden, Germany (e.g. Pfeiffer 1964; Wenzel et al. 1997;
Fig. 1b). The plutonic complex of Meissen developed as a
typical telescope intrusion with K-rich dioritic to mainly
monzonitic rocks at the margin and granodioritic to granitic
rocks in the centre. The rock composition of at least three
main intrusion stages changed from dioritic/monzonitic,
granodioritic/monzonitic (‘Hauptgranit’) to leuco-monz-
ogranites (‘Riesensteingranit’) from the margin towards the
centre of the Meissen Massif (Pfeiffer 1964; Wenzel et al.
1991). The NW–SE-striking pluton intruded a pull-apart
structure of the Elbe Zone during regional dextral strike-
slip tectonics (e.g. Pietzsch 1927; Mattern 1996; Linne-
mann and Schauer 1999). The Elbe Zone is interpreted as
being a Late-Carboniferous NW–SE-trending ductile shear
zone (Rauche 1991; Mattern 1996), which formed along
the northern margin of the Bohemian Massif.
40Ar/39Ar cooling ages of amphiboles (329.1 ± 2.8 Ma,
330.4 ± 2.8 Ma, Wenzel et al. 1997) and 238U/206Pb
SHRIMP ages of magmatic rims on zircons (326 ± 6 Ma,
330 ± 5 Ma, Nasdala et al. 1999; 334 ± 3 Ma, Hofmann
et al. 2009) are indistinguishable; however, they demon-
strate the intrusion of the monzonitic magmas during the
uppermost Vise´an. Muscovite of the ‘Hauptgranit’ and the
‘Riesensteingranit’ yielded 40Ar/39Ar plateau ages of
323.4 ± 1 Ma and 323.6 ± 1 Ma (Sharp et al. 1997).
Our sample originates from the SE tail of the intrusion at
the valley Plauenscher Grund near the Felsenkeller brewery
(Fig. 1b) and represents the syn-kinematic example of our
study. The term ‘syn-kinematic’ is related to strike-slip
tectonics of the Elbe Zone, being part of the final stage of
the Variscan orogenesis and the formation of Pangaea
(e.g. Linnemann and Schauer 1999; Hofmann et al. 2009).
Fig. 1 a Simplified geological map of the Erzgebirge/Krusˇne´ Hory
and adjacent regions showing the local distribution of late-Variscan
granites and the two sample localities. The inset shows the location of
the study area within central Europe. b Simplified geological map of
the Meissen Massif according to Eilers et al. (2000). The monzonite
sample originates from the SE tail of the intrusion. c Geological
cross-section of the Podlesı´ granite according to Breiter et al. (2005).
The sample originates from a quarry in the central roof of the
intrusion
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Int J Earth Sci (Geol Rundsch) (2011) 100:1515–1532 1517
The sample is a fine- to medium-grained weakly porphyritic
monzonite containing K-feldspar laths (1–6 mm long;
32–33 vol.%), oligoclase (0.5–5 mm long; 43–44 vol.%),
edenitic and actinolitic amphibole (1–5 mm long; 14–15
vol.%), quartz (0.1–3.5 mm; 5–6 vol.%), biotite (\1 mm; 1
vol.%) and diopside (0.6 vol.%; quantified X-ray diffraction
data; Figs. 2a, b, 3a). K-feldspar, oligoclase, edenitic
amphibole and diopside form usually sub-hedral to euhedral
phenocrysts embedded in a somewhat finer-grained ground-
mass. The large ([2 mm) euhedral crystals are interpreted as
phenocrysts, i.e., they crystallised in different PTX environ-
ments prior to final magma emplacement as indicated by their
variable core to rim composition (Wenzel et al. 1997).
Occasionally, amphibole grains contain diopside cores due to
mixing of K-rich shoshonitic magma and granitic crustal
magma during an early stage of the monzonite evolution
(Wenzel et al. 1997), which is additional evidence for the
early crystallisation of the phenocrysts. The groundmass
predominantly consists of weakly or non-deformed anhedral
quartz, K-feldspar and plagioclase. Common accessory
minerals are apatite, titanite, magnetite and zircon (altogether
3–5 vol.%). Titanite forms up to 2-mm-long prisms (Fig. 3b).
The monzonite exhibits a macroscopic SPO characterised by
aligned euhedral feldspar laths, amphibole and titanite. The
SPO at the pluton margin where the sample comes from is
more pronounced.
Aggregates of anhedral quartz fill interstices between
feldspar laths and amphiboles. The lacquer peel method
reveals a weak SPO of the elongated quartz aggregates
(Fig. 2b). The quartz shows deformation lamellae and sub-
grain formation due to rotation recrystallisation (e.g.
Passchier and Trouw 2006; Fig. 3b, c). Tiny quartz veins
fill the intracrystalline cracks of broken K-feldspar laths.
Myrmekite aggregates are common at K-feldspar faces
sub-parallel to the magmatic foliation.
Podlesı´ dyke granite
The Podlesı´ granite forms a small tongue-like, late-Variscan
intrusion, which outcrops over an area of 0.3 km2 at the
eastern margin of the Eibenstock–Nejdek pluton in the north-
western Czech Republic (Fig. 1a). It is the youngest
(311 ± 1 Ma; Breiter et al. 2005) and most differentiated
granite of the Eibenstock–Nejdek pluton and well studied
regarding geochemistry, petrology and mineralogy (Breiter
et al. 1997; Chlupa´cˇova´ and Breiter 1998; Ta´borska´ and
Breiter 1998; Breiter 2001, 2002; Maros et al. 2002; Mu¨ller
et al. 2002; Breiter et al. 2005). The granite intruded slightly
older biotite granites and Ordovician phyllites. The major part
of the Podlesı´ intrusion consists of medium-grained albite-
annite-topaz granite (stock granite). Several sub-horizontal
dykes of albite-zinnwaldite-topaz granite (dyke granite) were
intruded into the uppermost part of the stock granite (Fig. 1c).
The sample was taken from the dyke granite, which is
exposed in a 7-m wide, sub-horizontal dyke in a small
quarry near Podlesı´. In the uppermost 50 cm, the dyke
shows prominent layers with unidirectional solidification
fabrics (Breiter et al. 2005). The solidification fabrics
comprise fan-like zinnwaldite, comb quartz and K-feldspar
up to 6 cm length embedded in fine-grained granite. The
sample originates from approximately 1 m below the upper
contact and 0.5 m below the solidification fabrics.
The fine-grained dyke granite (Fig. 2c, d) consists of
quartz drops (0.1–1.5 mm; 22–34.5 vol.%), zinnwaldite
flakes (6.5–8 vol.%), K-feldspar (33.5–39.5 vol.%), albite
prisms (0.5–2 mm long; 18–26 vol.%) and topaz (3.5–6
vol.%), embedded in a microcrystalline mixture of albite,
K-feldspar, quartz and topaz (Breiter 2002; Fig. 3d).
Breiter (2002) distinguished three K-feldspar generations
within the dyke granite: (1) scarce perthitic phenocrysts
with 0.15–0.20 wt% Rb and 0.4% P2O5, (2) euhedral comb
crystals in layers with unidirectional solidification fabric
with 0.3–0.4 wt% Rb and 0.6–0.8 wt% P2O5 and (3)
abundant non-perthitic K-feldspar with 0.5–0.7 wt% Rb
and 0.8–1.5 wt% P2O5. Generation (2) does not occur in
the investigated sample. The rims of generation (3) are
strongly enriched in P2O5 indicating late crystallisation
from the residual P-rich dyke granite melt. Crystals of
generation (1) presumably represent inherited phenocrysts
from the Podlesı´ stock granite, because the composition of
the phenocrysts resembles the composition of the pheno-
crysts in the stock granite (Breiter 2002).
SPO of minerals is invisible at the hand-specimen scale.
At a microscopic scale, some of the larger albite prisms
are semi-parallel to the dyke granite contacts, defining a
weakly developed magmatic foliation. The lacquer peel
method (Behr 1966) reveals minor cm-scale layers of
variable quartz/feldspar ratio and crystal size (Fig. 2c, d).
These layers are parallel to the magmatic foliation.
Quartz occurs as ‘snowball’ quartz, which is defined as
isometric to ellipsoidal, late-magmatic crystals with con-
centrically entrapped groundmass minerals, mostly albite
(Beus et al. 1962; Fig. 3e, f). Despite the generally iso-
metric shape, the ‘snowball’ has complex, dendritic grain
boundaries. Albite prisms are tangential to and envelop the
‘snowball’ quartz. The chemistry and CL characteristics of
the ‘snowball’ quartz are different from that of the early
crystallised quartz phenocrysts occurring in the stock
granite (Mu¨ller et al. 2002). The structural and chemical
features of the ‘snowball’ quartz imply that the crystals
grew more or less in situ (Mu¨ller et al. 2002; Breiter et al.
2005), i.e., the features are indicative for highly evolved,
fluid-rich magma (Mu¨ller and Seltmann 1999). The
extrapolated solidus temperature of the dyke granite magma
determined from melt inclusion studies is 610 ± 26C
(Thomas et al. 1996). Cathodoluminescence imaging
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Int J Earth Sci (Geol Rundsch) (2011) 100:1515–15321518
reveals intragranular oscillatory growth zoning with trigo-
nal habit, indicating that the ‘snowball’ quartz crystallised
in the low-quartz stability field (Fig. 3e). The temperature
of the low/high-quartz transition is 573C at 1 atm and
increases with increasing crystallisation pressure (Yoder
1950). The pressure during emplacement of the Podlesı´
granite was about 1 kbar (Breiter et al. 2005), which caused
an increase in the transition temperature to 600C (Yoder
1950). This temperature is within the error range of the
magma temperature calculated from the melt inclusion data
by Thomas et al. (1996).
Methods
LPO evaluation from neutron diffraction data
The diffraction experiments were carried out at the TOF
diffractometer SKAT at the pulsed reactor IBR-2 in Dubna,
Russia (Ullemeyer et al. 1998). Application of TOF neu-
trons offers the opportunity to record complete diffraction
patterns, i.e., to measure all interesting pole figures
simultaneously. The SKAT is, in particular, characterised
by good d resolution (d: lattice spacing) and by a large
beam cross-section (50 9 50 mm2). Both these character-
istics were important for our investigations, because the
granite samples are polyphase composites with constituents
of low crystal symmetry and, therefore, the diffraction
patterns contain many Bragg reflections (Fig. 4). In addi-
tion, the samples are rather coarse-grained, i.e., large
sample volumes are required to ensure sufficient grain
statistics. Cylindrical samples of about 50 cm3 were pre-
pared for the diffraction experiment; in the case of the
more coarse-grained Meissen monzonite, three cylinders
(40 9 40 mm) were measured, and the recorded diffrac-
tion patterns were summed up to improve grain statistics.
For Quantitative Texture Analysis (QTA) the WIMV
algorithm was applied (Matthies and Vinel 1982). Despite
optimal experimental conditions, QTA of polyphase rocks
is crucial and was handled as an interactive procedure,
because various combinations of input pole figures may
lead to dissimilar results (Leiss et al. 2002). We, therefore,
Fig. 2 a Photograph of a
polished hand specimen of the
Meissen monzonite showing
shape-preferred orientation of
amphibole (black) and
K-feldspar (pinkish white)
crystals. b Black-and-white scan
of the lacquer peel of the
Meissen monzonite. The peel
was made from a polished and
HF-etched hand specimen (for
the method, see Behr 1966).
Anhedral quartz (black) fills
cavities between aligned
feldspar and amphibole (white;
not distinguishable) and
microcracks in feldspars. The
arrow indicates the orientation
of the magmatic foliation
formed by aligned crystals.
c Photograph of a polished
hand-specimen photograph of
the fine-grained Podlesı´ dyke
granite. d Black-and-white scan
of the lacquer peel of the
Podlesı´ dyke granite. Quartz
preferentially forms isometric
and ellipsoid crystals. The
weakly developed magmatic
foliation (arrow) is indicated by
variations in the quartz/feldspar
(black/white) ratio
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Int J Earth Sci (Geol Rundsch) (2011) 100:1515–1532 1519
checked the outcome of several QTA runs with different
input for reliability, which can be done by comparing
the reproduction (RP) values (Matthies et al. 1988), and
comparing recalculated pole figures to particular experi-
mental pole figures not used for the calculations. Mini-
mising the errors of LPO determination in such a way
ensures the optimum reliability of the final result. The pole
figures are presented such that the foliation plane/flow
plane is horizontal and the reference joint plane is vertical
(Figs. 5, 6).
Special attention was focussed on the quartz (011)(101)
reflection of the Podlesı´ granite, which overlaps the zinn-
waldite (001) basal plane reflection. The volume fraction of
zinnwaldite approaches 6.5–8 vol.%. Assuming preferred
orientation of the basal planes parallel to the foliation
plane/flow plane, which must be expected due to the grain-
shape-related re-orientation mechanism of micas, the
intensity maximum close to the foliation pole in the quartz
rhomb pole figure is partly due to the zinnwaldite (001)
reflection. Hence, the region around the foliation pole was
excluded from QTA of quartz, as indicated by a dotted
small circle in the quartz rhomb pole figure (Fig. 6).
Finally, the kinematically significant pole figures of all the
phases where QTA was possible were calculated from the
orientation distribution function.
Special attention was also put on the quartz (011)(101)
reflection of the Meissen granitoid. Due to the low volume
fraction of quartz (5–6 vol.%), the strong (011)(101)
reflection was the only reflection, which could be used to
construct a reliable pole figure. All the other quartz
reflections are either too low in intensity or could not be
separated from the reflections of the other mineral phases.
For trigonal crystal symmetry, QTA with a unique solution
is not possible from a single pole figure (Helming 1992).
Fig. 3 a Fabric of the Meissen
monzonite characterised by
preferentially oriented
K-feldspar laths with twinning
(kfs; crossed polarizers).
am—amphibole. b Sub-grain
formation in quartz (qtz) caused
by local strain imposed by the
neighbouring, more rigid
amphibole (am; arrows; crossed
polarizers). ti titanite.
c Sub-grain formation in
interstice quartz (qtz; crossed
polarizers). kfs K-feldspar,
pl plagioclase. d Fabric of the
Podlesı´ dyke granite with drop-
like quartz (‘snowball’ quartz;
qtz) embedded in a fine-grained
groundmass of albite (crossed
polarizers). e SEM-CL image of
‘snowball’ quartz (qtz)
revealing oscillatory growth
zoning with trigonal habit.
Alteration caused the lowering
of CL intensity (dark grey
areas) at the crystal margins.
The crystal is attached with the
rhombohedral face to a
zinnwaldite (zwd) flake.
ab—albite. f ‘Snowball’ quartz
(qtz) stitched to an albite plate
(ab; crossed polarizers).
Euhedral and inclusion-rich
topaz (toz) is common in the
rock
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However, to determine how the c-axes distribution may
appear, we calculated the orientation distribution function
from the (011)(101) pole figure applying the WIMV
algorithm and compared the significant recalculated pole
figures to particular pole figures obtained by means of
texture component deconvolution (Helming and Eschner
1990; for applications, see e.g. Leiss et al. 2002, Leiss and
Molli 2003). Each algorithm for QTA is characterised by
specific errors leading to somewhat dissimilar results;
however, similarities between recalculated pole figures can
be used to define a semi-quantitative estimate of the c-axes
distribution of interested.
Scanning electron microscope cathodoluminescence
(SEM-CL)
SEM-CL images were obtained from the JEOL 5900LV
analytical SEM with an attached GATAN Mini-Cathodo-
Luminescence detector at the Natural History Museum of
London. The applied acceleration voltage and current was
20 kV and *1 nA, respectively. The images were col-
lected from 4 scans of 20 s photo speed each and a pro-
cessing resolution of 1280 by 960 pixels and 256 grey
levels.
Results of LPO analyses
Meissen monzonite
The experimental pole figures of K-feldspar and plagio-
clase of the Meissen monzonite display more pronounced
LPOs, whereas the LPO of edenite (only the (040) pole
figure could be extracted from the TOF patterns without
overlaps) appears to be less pronounced (Fig. 5). The only
experimental pole figure of quartz (011)(101) shows a
three-fold maximum distribution, which is symmetrical
with respect to the magmatic foliation plane; the degree of
preferred orientation is weaker compared to the feldspars.
The ‘WIMV’-derived and ‘components’-derived recalcu-
lated (011)(101) pole figures are very similar to the
experimental pole figure; however, the recalculated c-axes
pole figures show distinct differences. While it seems to be
clear that the c-axes form a great-circle distribution sub-
parallel to the foliation plane with evidence for maxima on
the great circle, the pole figure recalculated from the
WIMV-ODF reveals an additional maximum normal to the
foliation plane. This maximum cannot be reproduced with
the component method.
Because of the pronounced LPOs, all experimental oli-
goclase and K-feldspar pole figures shown in Fig. 5 were
applicable to QTA. Recalculated (010) pole figures of both
minerals display a very strong maximum parallel to the
foliation normal. The (100) and (001) faces of K-feldspar
display uniform intensity distributions on great circles
around the (010) maximum. Due to weaker LPO, the (100)
girdle of oligoclase is broader, and the (001) girdle
degenerates to a small circle around the (010) maximum.
Preferred orientation of both these lattice planes is not a
direct consequence of the active deformation process,
because the intensity distributions on the great circle/small
circle are uniform. This holds true for K-feldspar and the
edenite (040) pole figure as well. Concerning edenite,
the consequence is that no information about the active
Fig. 4 Time-of-flight
diffraction pattern of the Podlesı´
dyke granite showing the large
number of Bragg reflections of
polyphase rock samples.
Prominent Bragg reflections are
labelled; reflections used for the
QTA are bold faced
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Int J Earth Sci (Geol Rundsch) (2011) 100:1515–1532 1521
re-orientation mechanism could be obtained from the LPO.
The observed parallelism of the (010) faces of oligoclase,
K-feldspar and edenite and the macroscopic magmatic
foliation is the most significant result of the LPO analyses.
The recalculated pole figures of the feldspars do not indi-
cate a magmatic lineation.
Fig. 5 Experimental (oligoclase, K-feldspar, quartz, edenite) and
recalculated (oligoclase, K-feldspar, quartz) pole figures in the
Meissen monzonite. Units are multiples of a random distribution;
the maximum intensity is indicated at the bottom right. Pole figures
indicated with an asterisk were used for QTA. Orientation of the pole
figures with respect to the reference joint plane 290/78 and to the
foliation plane is indicated by a sketch diagram
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Int J Earth Sci (Geol Rundsch) (2011) 100:1515–15321522
Podlesı´ dyke granite
The quartz and albite experimental pole figures of the
Podlesı´ dyke granite show very weak but distinct preferred
orientations, which are more or less symmetrically arranged
with respect to the macroscopic reference joint plane
351/83 (plunge direction/plunge angle). In contrast, the
K-feldspar pole figures appear to be random (Fig. 6). As
mentioned earlier, the zinnwaldite (001) reflection overlaps
the quartz (011)(101) reflection. The postulate that the
Fig. 6 Experimental (quartz, albite, K-feldspar) and recalculated
(quartz, albite) pole figures in the Podlesı´ dyke granite. Orientation of
the pole figures with respect to the reference joint plane 351/83 and
to the assumed sub-horizontal foliation plane is indicated by a sketch
diagram. For further explanations, refer to Fig. 5
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Int J Earth Sci (Geol Rundsch) (2011) 100:1515–1532 1523
intensity maximum close to the foliation pole is partly due to
the preferred orientation of the zinnwaldite (001) reflection is
supported by the (021)(201) ? zw ? kfs ? alb pole figure
(Fig. 6), which shows a small-circle intensity arrangement
around the intensity maximum in the (011)(101) ? zw pole
figure. Crystal structure calculations for all the minerals
present in the sample indicate that the intensity distribution
of the (021)(201) ? zw ? kfs ? alb pole figure is domi-
nated by some low-indexed zinnwaldite reflections with an
angular distance of 30 to 60 to the basal plane normal.
Hence, the small-circle intensity distribution in the
(021)(201) ? zw ? kfs ? alb pole figure indicates missing
preferred orientation of particular zinnwaldite reflections, as
well as preferred orientation of the zinnwaldite basal planes
with the intensity maximum in the centre of the small circle.
Since QTA of zinnwaldite was not possible due to insuffi-
cient input information, we cannot quantify the basal plane
preferred orientation of zinnwaldite.
QTA of quartz was based on three experimental pole
figures marked with an asterisk (Fig. 6). None of the other
pole figures could be used due to multiple overlaps (see
examples in Fig. 6). However, the results appear to be
reliable, mainly due to the very small RP values (refer to
Leiss et al. (2002) and to discussion in ‘‘LPO evaluation
from neutron diffraction data’’). The c-axis orientations of
quartz form an incomplete small-circle pattern around the
foliation normal with a large opening angle. Correspond-
ingly, the a-axes cluster in poorly defined small circles
around the foliation normal with a large opening angle. The
separated (101) and (011) rhombohedral faces display
girdle distributions sub-parallel to the foliation plane and
cluster-like maxima close to the foliation normal.
With regard to the recalculated pole figures of albite,
the (010) faces display the most pronounced LPO with its
normals sub-parallel to the foliation normal (Fig. 6—
recalculated pole figures). The deviation is about 20. This
is in agreement with the orientation of the cluster-like
(011) intensity maximum of quartz. All the other pole
figures of albite show weaker, girdle-like intensity distri-
butions. The (010) face is the face with the largest surface
area of idiomorphic albite. Hence, it must be discussed
whether the LPO of albite may originate in the same way
as for quartz.
In summary, the most important results of the LPO
analyses are the parallelism of (101) and (011) rhombo-
hedral faces of quartz, (010) faces of albite, magmatic
foliation and sub-horizontal contacts of the granite. The
intensity distributions are more or less symmetrically
arranged with the symmetry axis normal to the assumed
flow plane. Moreover, the supposed basal plane preferred
orientation of zinnwaldite confirms that the macroscopic
magmatic foliation plane observed in the field is also sig-
nificant at a sample scale.
Discussion
Meissen monzonite
The magma of the Meissen monzonite intruded the stress
field of the active dextral strike-slip system of the Elbe
Zone (e.g. Mattern 1996; Linnemann and Schauer 1999)
with high crystal load ([25 vol% phenocrysts), whereas the
Podlesı´ granite stock emplaced in a relatively passive,
transtensional tectonic setting (see also ‘‘Implications for
the regional geology’’). However, the LPO of plagioclase
in the Meissen monzonite is similar to the LPO of albite in
the Podlesı´ dyke granite; this holds true for the type of LPO
and for the orientation of the contour line patterns with
respect to the magmatic foliation. The similar LPO of non-
equidimensional plagioclase crystals in both magmatic
systems suggests that the crystal alignment was caused by
magma flow.
The crystal load of the monzonitic magma during
emplacement was presumably higher than 25 vol.%, as
indicated by the rather large volume fraction of euhedral
amphibole and feldspar phenocrysts. Phenocrysts act as
rigid particles in a viscous fluid and may be aligned if the
crystals own non-equidimensional shapes. This requires
that the phenocrysts crystallised early, which is docu-
mented by different composition and structure compared to
the groundmass minerals, and by internal compositional
zoning (e.g. Davidson et al. 2008). Early crystallisation of
the amphibole and feldspar phenocrysts in the monzonite
magma is indicated by variable core to rim composition,
the occurrence of diopside cores in amphibole grains and
different compositions of groundmass and phenocryst
feldspars (Pfeiffer 1964; Wenzel et al. 1997).
Due to the high crystal load of the monzonitic magma,
the crystals could not freely rotate and were tiled against
each other. As soon as the interaction between the crystals
became predominant, the flow regime changed from lam-
inar to granular flow (e.g. Drake 1990). However, we
suggest that the very pronounced LPOs of K-feldspar and
plagioclase phenocrysts are caused by a combination of
internal shear stress due to magma flow dynamics and
external shear stress due to regional strike-slip tectonics of
the Elbe Zone. The more distinct magmatic foliation at the
intrusion margin of the Meissen Massif compared to the
core of the pluton (e.g. Behr 1968) is a strong indication
that regional shear stress imposed the shear stress caused
by magma dynamics (Vigneresse et al. 1996). Plastically
deformed (elongated) xenoliths with their long axis parallel
to the magmatic foliation plane (Pfeiffer 1964) are other
indicators for superimposition of the internal stress field by
the regional stress field. The primary magmatic flow plane
and the foliation caused by the regional shear tectonics
are parallel to each other, suggesting that the direction of
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Int J Earth Sci (Geol Rundsch) (2011) 100:1515–15321524
magma flow was controlled by the regional shear tectonics
already at the initial stages of the pluton emplacement.
Deformation lamellae, sub-grain formation due to rota-
tion recrystallisation in quartz and strain-related myrmek-
ites are features of solid-state flow (Simpson 1985; Vernon
2000), indicating that the regional shearing continued after
the rheologically critical melt percentage (RCMP) of the
monzonitic magma was exceeded. The RCMP delineates
the boundary between magmatic and tectonic fabrics and is
defined for 65–80% solids (crystals) in the magma (Arzi
1978; van der Molen and Paterson 1979).
Conclusions on the development of the quartz LPO of
the Meissen monzonite are hard to draw, because ‘WIMV’-
derived and ‘components’-derived recalculated c-axes pole
figures show significant differences (Fig. 5). The compo-
nent method reveals a broad great-circle distribution of the
c-axes sub-parallel to the foliation plane, whereas the
WIMV method shows an additional weak c-axis maximum
normal to the foliation plane. According to Pfeiffer (1964),
quartz crystallised at the final stage of magma solidifica-
tion. Microstructural indicators for the late crystallisation
of quartz are as follows : (1) the small grain size and
anhedral shape of the grains filling interstices between
feldspar laths and amphiboles, (2) quartz moulded onto the
crystal phases of adjacent grains, (3) quartz fills the cracks
of broken feldspar phenocrysts and (4) quartz shows
homogeneous CL (early quartz phenocrysts would show
concentric growth zoning in CL, e.g. Mu¨ller et al. 2009).
Thus, the alignment of quartz nuclei and/or small equidi-
mensional quartz crystals due to magmatic flow can be
excluded.
The uniform great-circle distribution of the c-axes sub-
parallel to the foliation plane may result from oriented
quartz nucleation under the influence of an anisotropic
stress field, as predicted by Kamb’s hypothesis (1959).
Based on thermodynamic calculations, Kamb (1959) con-
cluded that the c-axis of quartz tends to align perpendicular
to the maximum principle pressure axis and, thus, sub-
parallel to the foliation plane. Kamb (1959) calculated
small-circle c-axis distributions with the circle axis per-
pendicular to the foliation plane, but the quartz c-axes of
the Meissen monzonite form a uniform great-circle distri-
bution. As mentioned before, the solidifying monzonite
magma was continuously affected by the regional shear
tectonics. After the RCMP was exceeded, the strain parti-
tioned into interstices between the rigid feldspar and
amphibole crystals, where the quartz was still crystallising.
The local stress field could result in oriented quartz growth,
whereby the strongest axis (c-axis of quartz) tended to
align perpendicular to the principle pressure axis as it is
illustrated in Fig. 7a.
Nevertheless, the LPO geometry of the Meissen quartz
does not imply a typical deformational LPO (e.g. Schmid
and Casey 1986), indicating that the solid-state flow fea-
tures observed in quartz are not strong enough to explain a
significant crystallographic re-orientation of quartz. We
cannot entirely exclude that the quartz LPO is partially due
to solid-state flow, such as local recrystallisation at grain
edges and sub-grain formation (Figs. 3b, c). The myr-
mekite formation, being part of the observed solid-state
features, may have influenced the quartz LPO. However,
myrmekites grow in epitaxial continuity with parent crys-
tals (e.g. Stel and Breedveld 1990); thus, the myrmekite
formation had no influence on the bulk LPO of quartz.
The poorly defined quartz c-axis maximum perpendic-
ular to the foliation plane, calculated by the WIMV
method, may reflect a different growth process. The most
probable explanation is epitaxial growth on the strongly
aligned feldspars, whereby quartz nucleated with its c-axis
(basal plane) perpendicular to (010) and/or (110) feldspar
faces (Fig. 7b). This type of epitaxial growth is known, for
example, from graphic feldspar-quartz intergrowth (e.g.
Fenn 1986; Stel 1992) and macroscopic quartz crystal
overgrowths on feldspar (e.g. Akhavan 2010). Particular
LPO developed presumably in pressure shadows between
aligned and tiled feldspar phenocrysts. Nevertheless, the
interpretation of the quartz LPO is rather speculative
because of reflection overlaps in the diffraction pattern and
the low volume fraction of quartz (5 to 6 vol.%) resulting
in a weak diffraction signals. Evidence for a magmatic
lineation could not be obtained from the LPOs.
Podlesı´ dyke granite
Melt inclusion studies by Breiter et al. (1997) revealed that
the dyke granite magma initially contained up to 2.6 wt%
P, 2.2 wt% F and about 7.5 ± 0.8 eq.-wt% water. The
magma chemistry indicates a rather low viscosity of the
dyke granite melt at the time of emplacement (e.g. Ding-
well 1987). In addition, the magma had a low crystal load
of 10 to 15 vol.%, comprising quartz, albite, mica nuclei
and some K-feldspar phenocrysts inherited from the stock
granite magma (Breiter 2002; Breiter et al. 2005). Distinct
compositional zoning of K-feldspar phenocrysts and dif-
ferent chemistry compared to the groundmass K-feldspar
document crystallisation during an early stage of magma
evolution (Breiter 2002).
After emplacement, the pressure of dissolved H2O
within the dyke exceeded the lithostatic pressure and the
cohesion of surrounding rocks, leading to fracturing and
brecciation in the apical part of the 7-meter-thick dyke
where the sample originates (Breiter et al. 2005). The
sudden drop of pressure during degassing caused rapid
crystallisation of the strongly under-cooled melt. Triggered
by microseismicity and filter pressing, more granite magma
moved into contact-parallel spaces generated by the
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Int J Earth Sci (Geol Rundsch) (2011) 100:1515–1532 1525
escaped volatiles and magma portions. This process repe-
ated several times, resulting in the formation of layered
structures defining a magmatic foliation and unidirectional
solidification fabrics (Breiter et al. 2005). Thus, the indi-
vidual layers of low-viscosity dyke granite magma were
rapidly transformed into highly viscous crystal mush. The
rather high crystallisation rate enabled freezing of the flow
fabrics.
The pronounced LPO and SPO of the euhedral to sub-
hedral albite plates characterised by the rotation of the
(010) face of albite parallel to the magmatic foliation can
be explained by laminar magmatic flow. At low strain,
crystal loads below 20% and large bulk volume, the
magma behaves as a viscous body, in which particles rotate
independently and the flow is laminar (e.g. Vigneresse
et al. 1996). This finding is in accordance with the postu-
lated basal plane preferred orientation of zinnwaldite par-
allel to the magmatic foliation, and with observations by
Ta´borska´ and Breiter (1998) who described a marked sub-
horizontal magnetic foliation of primary (magmatic) origin
in the Podlesı´ dyke granite. The c-axis distribution shows a
distinct maximum in the N–S direction parallel to the strike
of the reference joint plane 351/83, which is interpreted
as a magmatic lineation.
In contrast to albite, K-feldspar shows no LPO at all. As
mentioned earlier, the investigated sample contains minor
perthitic, partially dissolved K-feldspar phenocrysts and
abundant non-perthitic anhedral groundmass K-feldspar.
Shape anisotropy of the platy K-feldspar phenocrysts in the
dyke granite is apparently too small to form a distinct flow-
related LPO.
The weak LPO of ‘snowball’ quartz, which is charac-
terised by small-circle c-axis and a-axis distributions
with a large opening angle around the foliation normal,
approximately fits the LPO geometry in the flattening
field of the local strain field (e.g., Schmid and Casey 1986).
The opening angle of the two small girdles formed by the
c-axes in the pole figure is approximately 120–140
(Fig. 6). This angle corresponds to the angle between the
rhombohedral faces.
Quartz LPOs showing small-circle c-axis distributions
were already observed for a number of late-Variscan and
post-kinematic granites of the Bohemian Massif (Maros-
check 1933; Behr 1967; 1968; Watznauer and Behr 1966;
Mierzejewski 1968). Mostly, these granites are weakly
porphyritic, medium- to coarse-grained, with K-feldspar
and quartz phenocrysts embedded in a finer-grained
groundmass. Watznauer and Behr (1966) distinguished
between the c-axes LPO of high-quartz (early-magmatic
phenocrysts) and low-quartz (groundmass quartz) forming
small-circle distributions with small and large opening
angles, respectively. The c-axes LPO of high-quartz is less
pronounced than the LPO observed for low-quartz in the
same rock. The c-axis opening angle of the quartz LPO of
the Podlesı´ granite corresponds to the low-quartz LPO
pattern, which is in agreement with the observed
low-quartz habit of the ‘snowball’ quartz. According to
Watznauer and Behr (1966), the axis of the open circles is
mostly parallel to the magmatic lineation, sometimes
perpendicular to the magmatic lineation and foliation (e.g.,
Berbersdorf granite, Granulite Massif, Germany). The
latter geometry corresponds to the LPO geometry of the
Podlesı´ granite.
Maroscheck (1933) suggested that the quartz LPO in the
Mauthausen granite of the South Bohemian Massif is
caused by the alignment of crystal nuclei in a crystal mush
during magmatic flow (‘‘Keimregelung’’). However, he
could not explain the mechanism leading to preferred
Fig. 7 Schematic illustrations of supposed processes resulting in
quartz LPOs detected in the Meissen monzonite (a and b) and Podlesı´
granite (c). a Oriented high-quartz nucleation and growth under the
influence of an anisotropic stress field according to Kamb’s hypoth-
esis (1959). b Epitaxial growth of high-quartz (black) on aligned
feldspar (grey), whereby quartz nucleated with its c-axis (basal plane)
perpendicular to (010) and/or (110) feldspar faces. c Adherence of the
rhombohedral faces of trigonal quartz to the (010) faces of aligned
feldspar. Due to shape anisotropy of their attachments, quartz crystals
were passively aligned during magma flow. The quartz of the Podlesı´
granite crystallised as trigonal low-quartz. For explanations, see text
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Int J Earth Sci (Geol Rundsch) (2011) 100:1515–15321526
orientation of the more or less isotropic quartz nuclei.
Watznauer and Behr (1966) and Behr (1968) suggested that
the quartz LPOs are either due to the alignment of crystal
nuclei by magmatic flow forced by the internal stress of
intruding magma and/or the LPOs represent a stable
state of thermodynamic equilibrium according to Kamb’s
theory (1959). The authors exclude regional shearing and
twinning as possible causes for the small-circle c-axis
distribution.
The alignment of the (101) and (011) rhombohedral
faces of ‘snowball’ quartz in the Podlesı´ dyke granite
parallel to the magmatic foliation (Fig. 6) implies both the
processes described by Watznauer and Behr (1966) and
Behr (1968): (1) ‘snowball’ quartz alignment due to mag-
matic flow and/or (2) oriented crystal growth under stress
according to the Kamb’s hypothesis (1959). The Podlesı´
quartz does not exhibit recrystallisation, grain-size reduc-
tion, sub-grain formation, myrmekites, etc., which are
evident for solid-state flow (Vernon (2000). Hence, solid-
state flow as re-orientation mechanism can be excluded.
Alignment due to magmatic flow is difficult to understand
because the quartz crystals are a more or less isotropic.
However, the surface of the rhombohedral faces is larger
than the surface of the prism faces, as visualised by SEM-
CL imaging (Fig. 3e). Thus, the rotation of crystals with
one rhombohedral face parallel to the magmatic flow plane
may explain the LPO to some extent. The ‘snowball’
quartz is commonly attached with its rhombohedral faces
to the (010) faces of aligned albite prisms (Figs. 3e, f) and
to the (001) face of mica flakes (Fig. 3e). However, quartz
did not use the crystals of other minerals as nuclei, because
it usually forms double-ended crystals (Fig. 3e). Moreover,
quartz germinates with the c-axis perpendicular to feld-
spar and mica faces, which is not supported by the LPO
geometry (see also discussion earlier). Therefore, it is
suggested that the rhombohedral faces of the ‘snowball’
quartz adhered to the (010) faces of the strongly aligned
albite and to the (001) faces of zinnwaldite during growth.
Due to shape anisotropy of their attachments, quartz
crystals were passively aligned during magma flow.
Alternatively, the quartz LPO can be the result of oriented
growth on faces of aligned albite and zinnwaldite grains.
However, such type of oriented epitaxial growth has not
been reported.
Implications for the regional geology
The Meissen monzonite and Podlesı´ granite intruded the
Saxothuringian Erzgebirge at different geotectonic events
post-dating the Variscan metamorphic peak at approxi-
mately 340 Ma (e.g. Romer et al. 2003). The Meissen
monzonite intruded at 334 ± 3 Ma, when large-scale
strike-slip processes, the final events of the Variscan
orogeny and formation of Pangaea took place (e.g. Kroner
et al. 2007). The Podlesı´ granite intruded at 311 ± 1 Ma
as the youngest intrusion of the Eibenstock–Nejdek plu-
ton during orogenic uplift, extension and basement
exhumation.
The Meissen Massif intruded an area of extension (pull-
apart structure) within the schist belt of the Elbe Zone
during ongoing dextral shear (Mattern 1996; Kroner et al.
2007). The strain caused by the strike-slip movements lead
to alignment of the magmatic foliation parallel to the shear
direction at the NE and SW margin of the monzonite
intrusion (Fig. 8). The magmatic foliation is sub-parallel to
the s1-foliation of the host rocks at the NE and SW contact.
The core of the intrusion is characterised by a concentric
structure of the magmatic foliation, which seems to be less
unaffected by the regional shear strain. Similar conclusions
can be drawn from the orientation of the magmatic linea-
tion. At the NE and SW margins of the intrusion, the
magmatic lineation preferentially strikes NW to N, whereas
in the core the lineation forms a radial pattern. Thus, the
magmatic structures are, to some extent, mechanically
coupled to the host rock structures according to the clas-
sification of Paterson et al. (1998).
The shear tectonics completed prior to intrusion of the
Meissen ‘Hauptgranit’, the Meissen ‘Riesensteingranit’ and
the Markersbach granite (30 km SE from the sample local-
ity) into the Elbe Zone at 323.4 ± 1 Ma, 323.6 ± 1 Ma and
327 ± 4 Ma (Sharp et al. 1997; Hofmann et al. 2009). This
is evident from the less-developed magmatic foliation of
the particular granites, which is discordant to the host rock
structures. Furthermore, they cross-cut the tectonic struc-
tures related to the dextral strike-slip event (Behr 1964;
Hofmann et al. 2009). Thus, the intrusion of the Meissen
monzonite is an important geological time marker during
Variscan orogenesis.
The Eibenstock–Nejdek pluton, the mother pluton of the
Podlesı´ intrusion, consists of stacked laccolith-like intru-
sions building up an approximately 10-km-thick pluton,
indicated by seismic reflection data and the gravity
anomalies (Bankwitz and Bankwitz 1994; Behr et al. 1994;
Blecha et al. 2009). The tongue-shaped Podlesı´ granite
stock resembles the generally laccolith-like intrusion style
of the Eibenstock–Nejdek pluton, as indicated by field data,
drill core data and sub-horizontal orientation of the mag-
matic foliation.
In contrast to the Meissen monzonite, the Podlesı´ granite
stock emplaced in a rather passive, transtensional tectonic
setting. No macroscale indications for a deforma-
tion-related intrusion were found. The magmatic structures
(foliation and lineation) of the Podlesı´ granite and the
Eibenstock–Nejdek pluton are discordant to the s1-foliation
of the host rocks (Fig. 9a). It seems that the magmatic
structures are completely decoupled from the ductile
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Int J Earth Sci (Geol Rundsch) (2011) 100:1515–1532 1527
structures of the host rocks. However, in the northern part
of the NW–SE-striking pluton the magmatic lineation
strikes consistently NW–SE (Behr 1968), which possibly
indicates weak syn-intrusive influence of the external stress
field. Behr (1968) pointed out that the magmatic lineation
is similar for the different intrusion phases of the pluton.
The magmatic lineation of the Podlesı´ dyke granite plunges
4 northward and corresponds to the regional lineation
pattern of the pluton. The strike of the Eibenstock–Nejdek
pluton and its magmatic lineation are parallel to the strike
of the Gera-Ja´chymov-Zone (GJZ; Fig. 9b). The GJZ is a
NW–SE-striking, 7- to 14-km-wide and 250-km-long fault
system, which penetrates and borders the eastern part of the
Eibenstock–Nejdek pluton. It is predominantly character-
ised by vertical shear movements (dip-slip) during and
after pluton emplacement, extends down to the Moho
(e.g. Bankwitz et al. 1993; Behr et al. 1994; Blecha et al.
2009) and is still active (R. Wittenburg, pers. comm.). The
Podlesı´ granite is situated in the centre of the GJZ.
The crustal magmas of the Eibenstock–Nejdek pluton and
the related Podlesı´ granite stock presumably utilised the
faults of the GJZ for magma ascent (Blecha et al. 2009),
Fig. 8 a Simplified geological
map of the Meissen Massif
showing the deformation fabrics
of the syn-kinematic intrusive
rocks (magmatic foliation and
lineation) and their host
(s1 foliation). Compiled from
Behr (1968) and Eilers et al.
(2000). The Meissen Massif
intruded a pull-apart structure
during ongoing dextral strike-
slip tectonics in the Elbe Zone.
The insets show recalculated
pole figures of K-feldspar and
oligoclase from the sample 1
locality in relation to Earth
coordinates. Distinct maxima of
the (010) faces indicate a strong,
sub-horizontal alignment of
both feldspars defining the
magmatic foliation.
b Simplified geological map of
the Meissen Massif showing the
brittle structures. Modified after
Eilers et al. (2000)
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Int J Earth Sci (Geol Rundsch) (2011) 100:1515–15321528
Fig. 9 a Simplified geological
map of the northern part of the
Eibenstock–Nejdek pluton
showing the deformation fabrics
of the post-kinematic intrusive
rocks (magmatic foliation and
lineation) and their host
(s1 foliation). Compiled from
Behr (1968) and Hoth et al.
(1995). The insets show
recalculated pole figures of
albite and quartz of the Podlesı´
dyke granite in relation to Earth
coordinates. The distinct
maximum of the albite (010)
faces indicates sub-horizontal
alignment of the crystals
defining the magmatic foliation.
The quartz (011) rhombs are
partially parallel, partially
perpendicular to the horizontal
(=foliation) plane. b Simplified
geological map of the northern
part of the Eibenstock–Nejdek
pluton showing the brittle
structures. Modified after Hoth
et al. (1995)
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Int J Earth Sci (Geol Rundsch) (2011) 100:1515–1532 1529
which may explain the parallelism of the pluton axis and
GJZ. It is concluded that the emplacement of magmas of
the Eibenstock–Nejdek pluton can be interpreted as pow-
erful press-in of crystal-loaded magma into the upper crust.
The LPO geometry of the Podlesı´ quartz indicating flat-
tening strain supports this conclusion.
Conclusions
In this study, polyphase LPO analysis by means of neutron
diffraction was successfully applied to fine- to medium-
grained granitic rocks. The following conclusions regard-
ing the LPO development in the Meissen monzonite and
the Podlesı´ dyke granite can be drawn.
The late-Variscan Meissen monzonite, which syn-kine-
matically intruded the strike-slip stress field of the Elbe
Zone, shows pronounced LPOs of K-feldspar and plagio-
clase, as well as a weak LPO of amphibole due to alignment
of the oblate phenocrysts during magmatic flow. The LPO
of amphibole is less pronounced, because the shape
anisotropy is not as strong as the shape anisotropy of the
feldspars. Quartz shows a weak but distinct LPO charac-
terised by a three-fold maximum distribution, which is
symmetrical with respect to the foliation plane/flow plane.
The LPO is untypical for a deformational LPO, indicating
that solid-state deformation processes leading to recrystal-
lisation and sub-grain formation were too weak to cause
significant crystallographic re-orientation of quartz. The
most probable interpretation of the uniform great-circle
c-axis distribution is oriented quartz nucleation and growth
under the influence of an anisotropic stress field, whereby
the c-axes of quartz tend to align sub-parallel to the foliation
plane. Epitaxic growth of quartz on aligned feldspar
phenocrysts may explain the poorly defined c-axis maxi-
mum perpendicular to the foliation plane.
The Podlesı´ dyke granite representing a post-kine-
matic late-Variscan granite exhibits a pronounced LPO
of albite and zinnwaldite, which is characterised by
parallelism of the (010) face and the flow plane. The
crystal alignment is explained by laminar magmatic flow.
K-feldspar shows no LPO at all, because it crystallised
as a late phase from the residual melt, as indicated by
the P-rich rims (Breiter 2002). The weak quartz LPO of
the Podlesı´ dyke granite is characterised by a small-cir-
cle c-axis distribution with a large opening angle around
the foliation normal. This LPO pattern approximately
corresponds to the LPO geometry in the flattening field
of the local strain field. Due to the absence of typical
deformation features, the quartz LPO is interpreted as the
result of magmatic flow. During magmatic flow quartz
adhered with the rhombohedral facies to the (010) faces
of aligned albite and to the (001) faces of zinnwaldite.
Due to shape anisotropy of the attachments, quartz
crystals were passively aligned by magmatic flow.
Magmatic flow is the dominant process causing LPO in
the syn-kinematic Meissen monzonite and in the post-
kinematic Podlesı´ granite. In the case of the Meissen
monzonite, regional strike-slip shearing superimposes the
magmatic flow fabric but does not result in a typical
deformational LPO. Oriented crystal growth of late min-
erals during final magma solidification seems to be a sig-
nificant process contributing to the LPO development, in
particular in rocks that are characterised by pronounced
flow alignment of non-equidimensional phenocrysts.
The results also show that neutron diffraction is suitable
to determine the mineral LPOs on polyphase and coarse-
grained rocks. Especially the SKAT neutron diffractometer
at Dubna offers the necessary preconditions, above all high
resolution and the opportunity to investigate very large
sample volumes. Assuming optimal experimental condi-
tions, even distinct LPOs of minor minerals with volume
fractions down to 5% can be quantified.
Acknowledgments We thank P. Bankwitz, R. Boyd and I. Henderson
for their critical comments and assistance with the presentation. We
appreciated the constructive reviews by Ron Vernon and Scott Paterson,
which improved the quality of the manuscript considerably. The study
was supported by the Deutsche Forschungsgemeinschaft through grant
MU 1717/2-1, the Natural History Museum of London, and the
Geological Survey of Norway. Bernd Leiss is grateful for the financial
support of the German Federal Ministry of Education and Research
(BMBF 03DU0GO1-8).
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