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, OCTOBER 2012, 63, 5, 365—382 doi: 10.2478/v10096-012-0029-z
Provenance analysis of the Permo-Carboniferous fluvial
sandstones of the southern part of the Boskovice Basin and
the Zöbing Area (Czech Republic, Austria): implications for
paleogeographical reconstructions of the post-Variscan
collapse basins
SLAVOMÍR NEHYBA
1
, REINHARD ROETZEL
2
and LUBOMÍR MAŠTERA
3
1
Institute of Geological Sciences, Faculty of Science, Masaryk University, Kotlářská 2, CZ- 611 37 Brno, Czech Republic; slavek@sci.muni.cz
2
Geological Survey, Neulinggasse 38, A-1030 Wien, Austria; reinhard.roetzel@geologie.ac.at
3
Zeyerova 1435/12, 616 00 Brno-Žabovřesky, Czech Republic; Mastera.L@seznam.cz
(Manuscript received November 2, 2011; accepted in revised form April 2, 2012)
Abstract: The provenance analyses of Permo-Carboniferous fluvial sandstones of the southern part of the Boskovice
Basin and the Zöbing area are based on a wide spectrum of analytical techniques (petrography, heavy mineral assemblages,
chemistry of garnet, rutile and spinel, zircon study, major and trace elements). The studied sandstones are poorly sorted
and reveal a relatively immature composition implying short distance transport, rapid deposition, a high-relief source area,
mainly physical weathering and the minor role of chemical weathering. Different source areas for the Boskovice Basin and
the Zöbing area were proved. The Zöbing material was predominantly derived from crystalline units, mainly formed by
metamorphic complexes, although the portions of magmatic and volcanic material were significant. The source area is
supposed to be located in the Moldanubian Unit. The Boskovice Basin deposits, on the other hand, seem to be mainly
derived from metamorphic complexes, corresponding especially to the Moravian Unit, with a relatively wider spectrum of
metamorphites, together with the derivation of the detritus from pre-existing sedimentary rocks (especially from Moravo-
Silesian Paleozoic deposits/Drahany Culm unit). The transport direction in the basin was more complex, both from the
west and east. These results did not confirm the possibility of communication between the Boskovice Basin and the Zöbing
area during the Late Paleozoic. The existence of “colinear” marginally offset half grabens with predominant transversal
sources is here hypothesized. The general heavy mineral evolution in time does not indicate the successive exhumation of
a simple structured orogen but may be interpreted as differences in the extent of the source areas.
Key words: Permo-Carboniferous, terrestrial deposits, provenance, axial vs transverse sources.
Introduction
Studies of the provenance of clastic sediments in sedimentary
basins are important in paleogeographical and tectonic recon-
structions. The composition of clastic sediment is controlled
by a broad range of parameters starting with the composition
of source rocks, processes such as weathering, abrasion, hy-
drodynamic sorting, mixing during transportation, diagenetic
processes, etc. (Johnson 1993; Cox & Lowe 1995; Eynatten
2004). Integrated (modal analysis of sandstones, heavy min-
eral and bulk chemical analyses) methods of provenance
study of the sedimentary infill of collapse-type grabens are
used for constraining tectonic uplift and unroofing episodes in
orogenic belts (Adhikari & Wagreich 2011), evaluating the
transport distance, climate and weathering effects and relief
(Pettijohn et al. 1987).
Additionally, in order to use provenance analysis in the
paleogeographical reconstruction of ancient continental ba-
sins, one should understand the facies architecture and the
distribution of depositional environments in the basin. An
axial river or rivers are in general most important for redistri-
bution of the sedimentary material in a continental half gra-
ben. Rivers are often situated in the topographically lowest
part of a basin, which again is situated above the zone of the
maximum subsidence near the footwall block. The distribu-
tion of facies and transport direction in continental, exten-
sional basins are largely controlled by the tilt of the basin
floor (Bridge & Leeder 1979; Alexander et al. 1994; Mackey
& Bridge 1995; Mack & Leeder 1999; Gawthorpe & Leeder
2000; Peakal et al. 2000; Gawthorpe et al. 2003). This situa-
tion may be modified by variables in differential erosion of
the rock types in the source areas, headward growth of drain-
ages, fault segregation, or vertical or lateral fault propagation
(Leeder & Jackson 1993; Mack & Stout 2005).
The continental Permo-Carboniferous basins of the Bohe-
mian Massif record a long history of post-Variscan exten-
sional collapse from the Westphalian up to the Early Triassic
(Kalvoda et al. 2008; Martínek et al. 2009). The erosional
remnants of these deposits provide speculations regarding
the original paleogeographic extent of the basins. The purpose
of this study is to use chemical and petrographical approaches
for: i) confirming or denying supposed communication dur-
ing the deposition of the currently isolated Permo-Carbonif-
erous deposits of the Boskovice Basin (Moravia, Czech
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Republic) and the Zöbing Upper Paleozoic (Lower Austria,
Austria), ii) an improved determination of the source areas
and its evolution, and, iii) identification of the paleogeo-
graphical, climatic and tectonic events responsible for the
material supply.
Regional geological setting
The Boskovice Basin
The elongated asymmetrical Boskovice Basin (BB) is
striking in a SSW-NNE direction, filled with Permo-Carbon-
iferous deposits. The current width of the basin is only 5 to
12 km and the length approximately 90 km (Fig. 1). The BB
is situated along an important SSW-NNE trending dextral
strike slip structure, separating the principal geological units
of the Bohemian Massif namely the Moldanubian Unit, the
Moravian Unit, the Letovice and Zábřeh Crystalline Com-
plexes to the west and the Brno Massif and Moravo-Silesian
Paleozoic deposits (Culm facies) to the east (Čepek 1946;
Jaroš 1961). The BB can be classified as an extensional ba-
sin (half graben) with several stages of development. The en-
tire thickness of the sedimentary infill is estimated at
5700 m; the maximum present-day thickness of the sediment
fill in the BB, however, is assumed to be less than 3000 m
Fig. 1. Schematic geological maps of
the investigated areas in the Czech Re-
public and Austria. A – Boskovice
Basin, B – Zöbing area.
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(Šimůnek & Martínek 2008). The tectonic (NW-SE exten-
sion, dextral strike-slip reactivation along the NW oriented
fault) and the climatic processes (a general but not gradual
trend from the tropical humid paleoclimate in the Carbonif-
erous, through humid to semi-arid conditions with several
climatic fluctuations in the Permian) were the principal lead-
ing factors of the filling of the BB (Mikuláš & Martínek
2006; Šimůnek & Martínek 2008). The BB basin was also
transversally segmented by NW-SE trending faults/eleva-
tions into “subbasins”. The northern Letovice subbasin
(Lower Autunian – Middle Autunian) is younger than the
southern Rosice-Oslavany subbasin (Stephanian C – Lower
Autunian) according to Havlena (1964) or Jaroš & Malý (in
Pešek et al. 2001). The opening of the Rosice-Oslavany sub-
basin to the south and a relation to the Early Paleozoic de-
posits in the surroundings of Zöbing in Lower Austria is
widely assumed (Jaroš & Mísař 1967).
A strongly asymmetric distribution of the sedimentary fa-
cies and the continental depositional environments is typical
for the BB (Fig. 2). Breccias and conglomerates initiated the
deposition in the entire basin. In the eastern part the coarse-
grained deposition continued throughout the entire basin
succession with the facially monotonous Rokytná conglom-
erates comprising pebbles from easterly located geological
units (wackes, arkoses, shales, limestones, conglomerates,
rarely magmatic or metamorphic rocks). The lowest litho-
stratigraphic unit on the western limb of the basin is the so
called Basal Red-Brown Formation (Stephanian C) with the
Balinka conglomerates at its base. Pebbles from generally
westerly situated crystalline units (mica schists, gneisses,
quartzites, marbles, amphibolites, granulites, serpentine,
magmatic rocks, etc.) are most common in these conglomer-
ates. The Basal Red-Brown Formation is a product of alluvial
and fluvial deposition (Jaroš & Malý 2001). The succession
grades upwards into the Rosice-Oslavany Formation (Stepha-
nian C – lower Autunian/Asselian) with a coal seam com-
plex (Šimůnek & Martínek 2008; Štramberk et al. 2008).
The Rosice-Oslavany Formation is subdivided into the Lower
Grey Member, Middle Red-Brown Member and Upper Grey
Member. The sedimentary infill is represented by an alterna-
tion of shales, sandy shales, siltstones, fine- to coarse sand-
stones and rarely also of thin conglomerate layers. Three
coal seams were identified within the Lower Grey Member.
Mastalerz & Nehyba (1992) described the deposits of an
anastomosing fluvial system with abundant avulsion in the
Lower Grey Member. Episodic overfill of the channels and
overbank deposition (channel belts, crevasses) were typical
processes. Both episodic (one phase) and multi-storey chan-
nel fill were recognized along with collapses of the channel
banks. A bituminous shale horizon was described within the
Upper Grey Member with an abundant flora and fauna con-
tent. This horizon belongs to the Acanthodes gracilis Bio-
zone (Štamberk et al. 2008). Mastalerz & Nehyba (1997)
recognized that the lacustrine sequence within the Upper
Grey Member is composed of a transgressive, open-lake and
regressive segment. Evidence of frequent lake level fluctua-
tions, subaerial exposure and small-scale shallowing-up mo-
tifs was recognized. The following Padochov Formation
(Autunian/Asselian) represents a complex of brown arkosic
sandstones, arkoses and conglomerates (Jaroš 1961; Malý
1993; Pešek et al. 2001; Šimůnek & Martínek 2008). Exten-
sive fluvial channels with variations in sediment and fluvial
discharge and sediment load are assumed.
The next two upper formations namely the Veverská Bítýška
Formation (Autunian/Asselian) and the Letovice Formation
(Early Sakmarian—Late Sakmarian) are only developed in the
middle and northern part of the BB. They are represented by
cyclic fluvial and fluvio-lacustrine deposits with several fos-
siliferous horizons (Pešek et al. 2001; Zajíc 2002; Zajíc &
Štramberk 2004; Šimůnek & Martínek 2008).
Fig. 2. Lithostratigraphic correlation of the Upper Carboniferous—Permian sediments in the Boskovice Basin (modified after Šimůnek &
Martínek 2008) and the Zöbing area (Vasícek 1991a).
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Zöbing area
In the surroundings of Zöbing a more than 1000 m thick
succession of Upper Carboniferous to Permian sediments oc-
cur in a wedge-shaped distribution about 6.5 km long and
maximally 2.3 km broad. They mainly crop out at the
Heiligenstein east to southeast of Zöbing and reach as far as
Diendorf and Olbersdorf in the northeast (Fig. 1). These de-
posits of the Zöbing Paleozoic (ZP) have been well known
since the 19
th
century (cf. Holger 1842; Partsch 1843, 1844;
Cžjžek 1849, 1853; Ettingshausen 1852; Stur 1870; Suess
1912; Waldmann 1922; Vohryzka 1958; Schermann 1971).
The last detailed mapping was done by Vasícek (1974, 1975),
who also defined the Zöbing Formation and divided it in sev-
eral members (Vasícek 1991a; cf. Vasícek 1977, 1983, 1991b;
Vasícek & Steininger 1996). From the Zöbing Formation re-
mains of plants were described by Berger (1951), Vasícek
(1977, 1991a,b, 1983) and Vasícek & Steininger (1996) (cf.
Tenchov 1980; Cichocki et al. 1991). Bachmayer & Vasícek
(1967) described remains of insects, Flügel (1960) non-marine
molluscs and Schindler & Hampe (1996) remains of fish. How-
ever, until now no detailed sedimentological study was done.
The sediments of the Zöbing Formation are tectonically
tilted together with the crystalline basement (mainly granulite
and ultrabasits) and preserved in a tectonic half graben be-
tween the Diendorf fault in the northwest and the Falkenberg
fault in the southeast (Waldmann 1922; cf. Fuchs et al. 1984,
Fig. 1). Today in the surroundings of the Permo-Carboniferous
sediments, crystalline rocks of the Moldanubian Unit (granu-
lite, Gföhl gneiss, mica schists, amphibolite) occur. North of
the ZP granites, Biteš gneiss and mica-schists of the Moravian
unit are also located close to the Paleozoic sediments.
In the succession of the Zöbing Formation a trisection of
the sediments can be observed (Fig. 2). Above the crystalline
basement the Zöbing Formation starts in the southwest with
a succession about 300 m thick of alternating silt- and sand-
stones, which can be divided into four members.
The lowermost Leopoldacker Siltstone Member mainly
consist of dark grey, fine-grained, laminated silt- and sand-
stones with small coal seams and a high amount of organic
remains. In coaly shales and coal-streaks close to the base a
well preserved flora with Late Carboniferous ferns and horse-
tails occurs (Vasícek 1983, 1991a,b; Vasícek & Steininger
1996). Siltstones contain freshwater bivalves (Flügel 1960)
and in dark grey carbonate nodules (coal balls) freshwater
gastropods, ostracods and small fish teeth and fish scales
(Schindler & Hampe 1996) were found.
The above following ochre-brown, thin-bedded and slightly
calcareous silt- to sandstones of the Rockenbauer Sandstone
Member pass over into varve-like carbonaceous shales
(“Brandschiefer”). The sediments often contain resedimented
clay- and sandstone-pebbles and remains of conifers (Vasícek
1983, 1991a,b; Vasícek & Steininger 1996). Besides ostra-
cods, teeth and coprolites of fish and a fragment of an insect
wing were found in this member (Schindler & Hampe 1996).
In the Kalterbachgraben Sandstone/Siltstone Member
above, an alternation of massive layers of arkoses and sand-
stones with dark grey, laminated silt- to sandstones can be ob-
served (Vasícek 1983, 1991a,b; Vasícek & Steininger 1996).
In this alternation dark, laminated limestones, reddish silt-
stones, a coal seam, and a thin layer of rhyolitic tuff (Schindler
& Hampe 1996) are intercalated. Fossils were only found in a
single limestone bed, from where Schindler & Hampe (1996)
described many ostracods and few fish teeth.
The topmost member of the basal succession is the Kamp-
brücke Siltstone Member, which mainly consists of layered
siltstones alternating in longer intervals with arkoses and
sandstones and two fossil-bearing horizons. In the lower fos-
siliferous horizon a rich flora with ferns and horsetails
(Vasícek 1974, 1977, 1983) occurs, whereas the higher hori-
zon contains remains of conifers, freshwater bivalves and in-
sect wings (Bachmayer & Vasícek 1967; Vasícek 1991b).
The second, about 700 m thick middle part of the Zöbing
Formation is the Heiligenstein Arkose Member, which con-
sists of an alternation of banks of arkoses, sandstones and con-
glomerates. The grain size of this member increases towards
the top, where the Heiligenstein Conglomerate Layers com-
prise mainly granulite, additionally also quartz, quartzite, gra-
nitic gneisses, amphibolites, marble, Gföhl gneiss and clasts
of rhyolite (Waldmann 1922; Vohryzka 1958; Schermann
1971; Vasícek 1977, 1991b). Boulders in these conglomerates
reach sizes up to 1 m in diameter.
Above the Heiligenstein Arkose Member the third, about
400 m thick upper part of the Zöbing Formation starts with
the Lamm Siltstone/Arkose Member. It shows an alternation of
reddish-brown siltstones, sandstones and arkoses. In finer
parts of the succession intercalations of dark grey silicified
limestones can be observed (Vasícek 1983, 1991a,b; Vasícek
& Steininger 1996). From pelitic sediments Vasícek (1991b)
describes imprints of raindrops. In the uppermost part of the
Zöbing Formation the Geißberg Sandstone Member occurs. It
is a varied series of red and grey claystones in alternation
with arkoses and sandstones (Vasícek 1983, 1991a,b;
Vasícek & Steininger 1996). No biostratigraphic data are
available until now from the Lamm Siltstone/Arkose Mem-
ber and the Geißberg Sandstone Member.
The sediments of the Leopoldacker Siltstone Member at
the base of the Zöbing Formation are dated by the seed fern
Alethopteris zeilleri and similar forms to the Late Carbonife-
rous (Stephanian) (Vasícek 1977, 1983, 1991a; Vasícek &
Steininger 1996). In the above following Rockenbauer Sand-
stone Member and Kampbrücke Siltstone Member callipterids
like the seed fern Autunia conferta, the conifer Ernestioden-
dron filiciformis and fructifications of horsetails (Calamo-
stachys dumasii) already point to an Early Permian (Autunian)
age (Schindler & Hampe 1996; Vasícek & Steininger 1996).
Volcanoclasts from rhyolite in the Heiligenstein Arkose
Member are correlated with the volcanism in the Middle Per-
mian “Saalic orogenic phase” (Vasícek 1977, 1983, 1991a,b;
Vasícek & Steininger 1996).
For the basal, fine-grained part of the Zöbing Formation
Schindler & Hampe (1996) assume that the depositional en-
vironment was shallow eutrophic lakes with a vegetation-
rich riparian zone or stagnating oxbow lakes close to a
fluvial environment. With the beginning of the Kalterbach-
graben Sandstone/Siltstone Member a clear climatic and en-
vironmental turn looms. The arkoses and conglomerates of
the Kalterbachgraben Sandstone/Siltstone Member and the
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Heiligenstein Arkose Member are interpreted as periodic
flash-flood deposits in arid alluvial environments of the Per-
mian (Vasícek 1991a,b).
Methods
The presented results are based on the study of the profile
along the Oslava River between Oslavany and Ivančice, where
deposits of the Basal Red-Brown Formation, Rosice-Osla-
vany Formation, Padochov Formation, and Rokytná con-
glomerates (the Rosice-Oslavany subbasin of the BB) were
investigated. In the broader surroundings of Zöbing Upper Pa-
leozoic deposits are accessible in several small outcrops. The
studied outcrops belong to the Rockenbauer Sandstone Mem-
ber, Kalterbachgraben Sandstone/Siltstone Member, Heiligen-
stein Arkose Member, and Lamm Siltstone/Arkose Member
(Vasícek 1991a; cf. Fig. 1).
All the outcrops and sections were logged, the depositional
environment and its evolution was evaluated (Nehyba et al. in
prep.). Samples for provenance analyses were only selected
from sandstone bedforms (dunes) of fluvial channels. Ten sam-
ples were selected from the BB and thirteen from the ZP. The
framework grains were point counted in thin sections according
to the standard method (Dickinson & Suczek 1979; Zuffa 1980,
1985; Dickinson 1985; Ingersoll 1990). The entire rock
geochemistry was evaluated in the ACME laboratories Van-
couver, Canada (10 analyses of the BB, 15 analyses of the ZP).
Heavy minerals were quantified by counting method under
the polarizing microscope in the grain-size fraction 0.063—
0.125 mm (8 samples from the BB, 13 samples from the ZP).
The opaque minerals were not considered in the calculation.
Detailed studies of the zircon characteristics were carried out
on samples with enhanced occurrence of this mineral. The
outer morphology, colour, presence of older cores, inclusions
and zoning were evaluated in the entire zircon spectra (291
zircons from the BB and 223 from the ZP). Only the euhedral
or subhedral zircons were considered in the study of typology
(29 grains from the BB and 43 grains form the ZP) and elon-
gation (89 grains from the BB and 81 grains from the ZP). The
electron microprobe analysis of garnet, rutile and spinel were
evaluated with a CAMECA SX electron microprobe analyser
(Faculty of Science, Masaryk University, Brno, Czech Repub-
lic). Data from 276 analysed garnet grains for the ZP and from
133 for the BB, as well as from 100 analysed rutiles for the ZP
and from 67 for the BB were available. The analyses of 22
spinels for the BB and 10 for the ZP were obtained.
Results
Petrography
Sandstones from both the BB and the ZP are in general
coarse- to medium-grained, often texturally immature, poorly
sorted with a certain admixture of granules. The sandy grains
are often angular and sub-angular, whereas small pebbles are
usually rounded. The amount of the matrix is limited (Fig. 3)
and is mostly of the coating type. Sericite, chlorite and clas-
tic micas were recognized in the matrix. Cement, which of-
ten intensively colours the matrix, is formed by carbonates
and amorphous Fe oxi-hydroxides. The studied samples oc-
cupy the wacke field to a predominant extent; some of them
being arkoses, whereas subwackes are rare (Petránek 1963;
Kukal 1986) (Fig. 3).
The sandstones from the ZP contain a significant amount
of both monomineral and aggregate quartz. The anhedral
quartz grains suggest an origin from granitoids. Cataclasis of
the quartz grains resembles a source from muscovitic quartz-
ites or mica schists. In all probability coarse subhedral feld-
spar grains with microperthites and plagioclases originated
from cataclased granitoids. The clasts of fine grained acidic
plutonites, fine-grained gneisses, granulites, and feldspar
phenocrysts were determined regularly, whereas quartzites
were rare. The partly reworked clasts of glasses or volcanites
with micropoikilitic structures represent the acidic volcanic
source. The source of micas (both biotite and muscovite) is
probably mainly connected with mylonites or cataclasites,
rarely with granitoids. Garnet, cordierite, rutile, tourmaline
and zircon were identified as accessory minerals.
A broader spectrum of detrital grains was recognized within
sandstones of the BB. Monomineral and aggregate quartz
dominates and originate from granitoids, cataclasites and my-
lonites. The content of feldspar is generally lower than in the
ZP, but relatively coarse grains of plagioclases are common.
Their source is connected with granodiorites or diorites.
Argillizated acidic volcanic glasses, felsites or grains with flu-
idal structures represent the most common volcanic derivates.
Grains of quartzites, fine-grained slates or even mica schists
are more common in the BB than in the ZP. Grains of silty
shales originate in all probability from the Lower Carbonifer-
ous “Culmian“ rocks. The content of micas (both biotite and
Fig. 3. Classification ternary diagram (according to Petránek 1963;
Kukal 1986) of the studied sandstones. M = matrix (%), F = plagio-
clase + K-feldspar (%), U = unstable rock fragments (%), Q = quartz
(%), S = stable rock fragments (%).
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Table 1: Framework mineral data of studied sandstones (BB – Bos-
kovice Basin, ZP – Zöbing area).
Fig. 4. Discrimination ternary diagrams (according to Dickinson
1985, 1990; Ingersoll 1990) of the studied sandstones. (Q = Q
m
+ Q
p
,
Q
m
– monocrystalline quartz, Q
p
– polycrystalline quartz;
F = plagioclase + K-feldspar; L = L
v
+ L
s
+ L
m
, L
v
– volcanic lithic
fragments, L
s
– sedimentary lithic fragments, L
m
– metamorphic
lithic fragments; L
t
= L + Q
p
).
muscovite) varies to a great extent and is generally lower in
the BB than in the ZP. The presence of carbonate cement is
more frequent. Garnet, tourmaline, rutile and zircon form the
most common accessory minerals. The remnants of clasts of
organic material were regularly observed.
On the Q
m
—F—L
t
(Fig. 4A) discrimination diagram, the
majority of the samples from the ZP occupy the continental
block field, whereas the samples from the BB reveal a mixture
of the granitoid detritus with remnants of acidic volcanism
and metamorphosed sediment origin. Differences in the
provenance of the ZP and the BB are supported by the posi-
tion of the samples in the diagram L
m
—L
v
—L
s
, (Fig. 4B, In-
gersoll 1990) and Q—F—L (Fig. 4C, Dickinson 1985, 1990).
Framework mineral data are presented in Table 1. The sand-
stones of the ZP plot in the field of the basement uplift of the
stable craton, on the other hand the BB sandstones plot in the
recycled orogen and the dissected volcanic arc fields
(Fig. 4C). The mixing of material from the crystalline base-
ment (metamorphic and plutonic rocks) with volcanogenic
and recycled sedimentary rocks typifies the BB.
Heavy mineral studies
The heavy mineral ratios apatite:tourmaline (ATi),
garnet:zircon (GZi), TiO
2
-group:zircon (RZi) and the ZTR
(zircon+tourmaline+rutile) index have been used (cf. Morton
& Halsworth 1994). The ZTR index is widely accepted as a
criterion for the mineralogical “maturity” of heavy mineral
assemblages (Hubert 1962; Morton & Hallsworth 1994).
Garnet, zircon, and rutile represent the most common heavy
minerals in the studied deposits, being relatively stable in di-
agenesis and having a wide compositional range, so as to be
further evaluated in detail along with spinel.
Heavy mineral assemblages and mineral ratios
The heavy mineral assemblages differ significantly between
various lithostratigraphic units of the BB and the ZP but also
between individual beds of the single units. Garnet (46.2 %)
Sample Q
m
F L
t
L
m
L
v
L
s
Q
t
L
BB
1 55.7 22.1 22.2 68.1
19.7 12.2 55.7 22.2
BB 2
62.7 32.7 4.6 23.7 48.3 28
62.7 4.6
BB
3 42.1 36.8 21.1 50.3
18.8 30.9 42.1 21.1
BB 4
60
21.3 18.7 70.3 29.7 31.4 60
18.7
BB 5
78.4 9.3 12.3 36.3 6.7 57
78.4 12.3
BB 6
63.8 29.9 6.3 51.1 48.9
0
63.8 6.3
BB
7 68.8 20.4 10.8 80.7
19.3 0 68.8 10.8
BB 9
62.1 18.3 19.6 22.4 42.6 35
62.1 19.6
BB
10 68.8 20.4 10.8 80.7
19.3 0 68.8 10.8
BB 11
62.1 18.3 19.6 22.4 42.6 35
62.1 19.6
ZP 1
87.3 8.9 3.8 87.8 12.2
0
87.3 3.8
ZP 2
63.6 32.3 4.1 46
54
0
63.6 4.1
ZP 3
65
28.3 6.7 30.5 56.3 13.2 65
6.7
ZP 4
56
36.3 7.7 8.8 91.2
0
56
7.7
ZP 5
39
51.2 9.8 22.1 77.9
0
39
9.8
ZP 6
51.2 42.5 6.3 6.9 93.1
0
51.2 6.3
ZP 7
50.4 41.5 8.1 20.8 79.2
0
50.4 8.1
ZP 8
63.8 26.7 9.5 9.5 90.5
0
63.8 9.5
ZP 9
49.9 36.5 14.6 74.9 25.1
0
48.9 14.6
ZP 10
44.3 44.6 11.1 89.8 10.2
0
44.3 11.1
ZP 11
53.1 36.5 9.4 4.3 95.7
0
53.1 9.4
ZP
12 44.1 45.1 10.8 0 100 0 44.1 10.8
ZP 13
53.1 36.3 10.4 7.5 92.5
0
53.1 10.4
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and zircon (22.1 %) predominate in the transparent heavy
mineral spectra of the Basal Red-Brown Formation of the BB.
Further minerals (monazite, kyanite, rutile, tourmaline, stauro-
lite, apatite, zoisite, amphibole, and spinel) represent only a
small percentage. The ATi-ratio is 20.8, the GZi-ratio 67.6,
the RZi-ratio 14.7 and the ZTR index 29.7. A high content of
kyanite (62.4 %) and epidote (28.9 %) together with an acces-
sory occurrence of rutile, zircon, staurolite, tourmaline and
spinel were determined in certain heavy mineral spectra of the
Rosice-Oslavany Formation. There the RZi-ratio is 80.6 and
the ZTR index 9.0. In further samples from this formation zir-
con (78.9 %) strongly predominates with a subordinate occur-
rence of apatite, rutile, tourmaline, kyanite, and spinel. Here
the ATi-ratio is 24.4, the RZi-ratio 92.9 and the ZTR index
94.7. Zircon (22.3—41 %), garnet (12.5—25.6 %), apatite
(17.4—24.5 %) and kyanite (11.8—16.7 %) predominate in the
heavy mineral spectra of the Padochov Formation. Rutile,
tourmaline, staurolite, epidote, monazite, titanite, spinel, and
andalusite were also recognized and usually have a few per-
cent. The ATi-ratio is 82.9—95.0, the GZi-ratio 11.1—53.4, the
RZi-ratio 5.3—17.5, and the ZTR index 28.9—53.3. In sandstone
beds within the Rokytná conglomerates zircon (30.8—35.8 %),
garnet (15.6—54.6 %) and apatite (15.6 %) dominate. Signifi-
cantly less common were rutile, zoisite, amphibole, kyanite,
epidote, monazite, staurolite, andalusite, titanite, and spinel.
The ATi-ratio is 100, the GZi-ratio 30.4—64, the RZi-ratio
9.9—18.8, and the ZTR index 32.4—44.1.
In the Rockenbauer Sandstone Member of the ZP rutile
(72.1 %) and zircon (14.7 %) dominate. Additional heavy
minerals (apatite, titanite, zoisite, epidote, monazite, garnet,
staurolite, tourmaline, and andalusite) form several percent at
a maximum. The ATi-ratio is 33.3, the GZi-ratio 19.7, the
RZi-ratio 84.0, and the ZTR index 87.8. Two heavy mineral
assemblages were determined within the Kalterbachgraben
Sandstone/Siltstone Member. An association with predomi-
nance of garnet (69—81.6 %), rutile (10.9—15.2 %) and zircon
(5.5—16.1 %) and occurrences of kyanite, apatite, titanite, and
monazite prevail in the majority of the samples. The ATi-ratio
is 100, the GZi-ratio 81.1—96.9, the RZi-ratio 40.4—84.1, and
the ZTR index 15.8—27.0. Zircon (39 %), rutile (16.9 %) and
garnet (16.9 %) predominate in the second association of this
member with the occurrences of apatite, andalusite, tourma-
line, epidote, kyanite, and amphibole. The ATi-ratio is 79.7,
the GZi-ratio 30.2, the RZi-ratio 47.2, and the ZTR index
75.1. Two associations were also determined in the samples
from the Heiligenstein Arkose Member. The first one is char-
acterized by a predominance of garnet (78.6—85.0 %), with oc-
Siltstone/Arkose Member. Additional heavy minerals (apa-
tite, rutile, kyanite, and zircon) consist of only several per-
cent. The ATi-ratio is 100, the GZi-ratio 99.0, the RZi-ratio
82.0, and the ZTR index 5.0.
The amount of heavy mineral analyses is insufficient thus
we can only speculate about the general evolution of the
heavy mineral assemblages. The situation seems to be less
complicated in the ZP. Basal deposits (Rockenbauer Sand-
stone Member, Kalterbachgraben Sandstone/Siltstone Mem-
ber) are typified by a strong predominance of rutile and
zircon, show low ATi and GZi-ratios, a high RZi-ratio and
ZTR index. The middle part of the succession (Heiligenstein
Arkose Member) is typically characterized by the presence of
garnet, but also of rutile, zircon and apatite. The ATi is 100,
the GZi-ratio 81.1—96.9, the RZi-ratio 40.4—84.1, and the ZTR
index 15.8—27.0. The ATi and GZi-ratios are higher and the
RZi-ratio and ZTR index lower than in the basal parts of the
succession. Garnet strongly predominates in the upper part of
the succession (Lamm Siltstone/Arkose Member). The ATi,
GZi and RZi-ratios are the highest in the succession and the
ZTR index is particularly low.
In the BB the basal deposits are characterized by a strong
predominance of garnet and zircon, low ATi and RZi-ratios,
a high GZi-ratio and a medium ZTR index. For the middle
part of the succession (Rosice-Oslavany Formation) the pres-
ence of varied heavy mineral spectra in different samples
with an important presence of kyanite, epidote in some sam-
ples and a strong predominance of zircon are typical. The
ATi-ratio is low, the RZi-ratio is high and the ZTR index
varies significantly. Zircon, garnet, apatite and also kyanite
dominate in the upper parts of the succession (Padochov For-
mation and Rokytná conglomerates). The heavy mineral as-
semblages differ particularly in terms of the relative content of
garnet and kyanite. The ATi ratio is high; GZi and Rzi ratios
and ZTR index vary.
Rutile
The concentration of the main diagnostic elements (Fe,
Nb, Cr, and Zr) varies significantly in the studied samples.
Data from the ZP have revealed that the concentration of Nb
varies between 182 and 7340 ppm (average 2082 ppm), the
concentrations of Cr vary between 4 and 4050 ppm (average
1011 ppm), of Zr between 170 and 8410 ppm (average
3183 ppm), and the value of logCr/Nb is mostly negative
(87.5 %). The data from the BB reveal that the concentration
of Nb varies between 129 and 8538 ppm (average 1565 ppm),
Fig. 5. Discrimination plot Cr vs. Nb of investigated rutiles.
currence of rutile, apatite, zircon, staurolite, mona-
zite, zoisite, and kyanite. The ATi-ratio is 100, the
GZi-ratio 97.8—98.9, the RZi-ratio 70.6—83.0, and
the ZTR index 3.2—8.8. The second one is typified
by a predominance of garnet (30.7—63.3 %), rutile
(11.2—19.8 %), and also apatite (6.6—22.2 %) and
zircon (6.6—33.2 %), and occurrences of stauroli-
te, monazite, zoisite, tourmaline, epidote, an-
dalusite and kyanite. The ATi-ratio is 83.5—100,
the GZi-ratio 52.0—88.5, the RZi-ratio 33.0—69.3,
and the ZTR index 19.2—46.8. Garnet (84.9 %)
predominates in the heavy minerals of the Lamm
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of Cr between 3 and 5080 ppm (average 510 ppm), of Zr be-
tween 15 and 8330 ppm (average 1291 ppm), and the value of
logCr/Nb is also mostly negative (85.1 %). The discriminate
plot Cr vs. Nb is presented in Fig. 5. Rutiles from the BB re-
veal higher variations in the concentrations of diagnostic ele-
ments than rutiles from the ZP.
The Zr-in-rutile thermometry was applied for metapelitic
zircons only (for a stable rutile-quartz-zircon assemblage cf.
Zack et al. 2004a,b; Meinhold et al. 2008). The results indi-
cate that 94.7 % of metapelitic rutiles from the ZP belong to
granulite metamorphic facies and 5.3 % to the amphibolite/
eclogite facies. In the BB the metapelitic rutiles of granulite
metamorphic facies form 53.6 %, the rutiles of the amphibo-
lite/eclogite facies 32.1 % and 14.3 % belong to the green-
schist/blueschist facies.
Garnet
The results of the analyses of detrital garnet chemistry are
presented in the Table 2 and Fig. 6A,B. The garnet composi-
tion is different for the ZP and the BB. The garnet composi-
tion of all lithostratigraphic members of the ZP (Fig. 6B) was
surprisingly monotonous. Almandine absolutely predominates
as pyrope-almandines make 93.5 % of the spectra. Almand-
ines form 2.2 %, grossular-pyrope-almandines 1.4 %, spessar-
tine-almandines form 1.4 %, grossular-almandines form
0.7 %, while pyrope-andradite-almandine and grossular were
exceptional. The spectra of garnets are much wider in the BB
(Fig. 6A), where 14 types of garnet were determined. Pyrope-
almandines predominate forming 50.4 %, grossular-almand-
ines form 16.7 % and pyrope-grossular-almandines were
determined in 11.3 % of the studied grains.
Zircon
In the BB subrounded and rounded zircons in all studied
samples amounted to 49.8 %, whereas the subhedral ones
formed 45.7 % and the euhedral zircons constituted 4.4 %. In
the ZP subrounded and rounded zircons in all studied samples
amounted to 47.9 % whereas, subhedral ones made 42.7 %
and euhedral zircons constituted 9.4 %. Certain differences in
the shape of zircons were recognized between deposits of vari-
ous members of the ZP. The highest occurrence of euhedral
zircons was observed in the Heiligenstein Arkose Member.
Zircons with a pale colour shade predominate in the BB
with 66.6 %. The colourless zircons constitute 23.6 % of the
spectra. Zircons with a brown colour form 5.8 %, opaque
ones 3.4 %, and pink zircons are very rare (0.7 %). Zircons
with a pale colour shade also predominate in the ZP forming
Table 2: Garnet types of the studied deposits of the Boskovice Ba-
sin (BB) and Zöbing area (ZP) (ALM – almandine, GRS – gros-
sular, PRP – pyrope, SPS – spessartine, AND – andradite).
Fig. 6. Ternary diagram of the chemistry of detrital garnets (Morton
1985). A – analysis from Boskovice Basin, B – analysis from
Zöbing area (ALM – almandine, GRS – grossular, PRP – py-
rope, SPS – spessartine).
Fig. 7. Histograms of zircon elongation.
Garnet type
ZP
BB
ALM
(82–90)
2.2 %
5.3 %
ALM
(49–83)
–PRP
(11–48)
93.5 %
50.4 %
ALM
(69)
–PRP
(18)
–SPS
(12)
–
0.8 %
ALM
(62–64)
–PRP
(18–25)
–GRS
(10–15)
1.9 %
2.3 %
ALM
(58)
–GRS
(22)
–SPS
(16)
–
0.8 %
ALM
(60–67)
–GRS
(19–34)
0.7 %
16.7 %
ALM
(63–68)
–GRS
(12–20)
–PRP
(10–16)
–
11.3
%
ALM
(50–83)
–SPS
(14–42)
1.4 %
4.5 %
ALM
(71–72)
–SPS
(13–15)
–PRP
(10–11)
–
2.3 %
ALM
(42–56)
–SPS
(21–27)
–GRS
(15–21)
–PRP
(13–15)
–
1.6 %
GRS
(66–89)
–AND
(11–31)
0.4 %
1.5 %
GRS
(74)
–PRP
(13)
–AND
(12)
–
0.8 %
GRS
(50)
–ALM
(41)
–
0.8 %
PRP
(40)
–AND
(36)
–ALM
(20)
–
0.8 %
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48.4 % while colourless zircons constitute 42.2 % of the
spectra. Zircons with a brown colour form 7.6 %, opaque
ones 0.4 % and pink zircons 1.3 %.
The proportion of zoned zircons in the BB samples is
19.8 % while older cores occur in zircons to an amount of
14.7 %. These zircon characteristics are significantly less
common in the ZP where zoned zircons form maximally
9.7 % and zircons with older cores 4.7 %. All the studied zir-
cons show inclusions.
The average value of the elongation (the relationship be-
tween the length and width of the crystals) for the BB sam-
ples was 2.18 and for the ZP 2.33. The histograms of
elongation are presented in Fig. 7. Zircons with elongation
above 2.0 predominate with 65.2 % in the BB and 69.7 in the
ZP. Zircons with an elongation of more than 3 are supposed
to reflect a magmatic/volcanic origin (Zimmerle 1979) and/
or only limited transport. The presence of such zircons is
very limited in the BB with 5.6 %, whereas it is significantly
higher in the ZP with 19.1 %.
The parental magmas of the studied zircons had a hybrid
character (close to the anatectic origin) in accordance with
the position of the “typology mean point” (Pupin 1980,
1985). The predominance of the typological subtypes S18 of
Pupin (1980) can be observed in the BB and of S17 and S12
in the ZP (Fig. 8A,B).
Spinel
The microprobe study reveals a strong predominance
(86.4 % in the BB and 70 % in the ZP) of spinels with a high
content of Cr ( > 2500 ppm). These spinels can be classified
as chromian ones which are a typical mineral for peridotites
and basalts (Pober & Faupl 1988) reflecting a source from
mafic/ultramafic rocks. Plotting TiO
2
against Al
2
O
3
(Fig. 9)
for spinels points to a volcanic source, which also suggests
the relatively high TiO
2
concentrations (Kamenetsky et al.
2001; Zimmermann & Spalletti 2009).
Major element geochemistry
The major element composition is presented in Table 3. In
the studied samples the positive inter-relationship between
Al
2
O
3
and
TiO
2
is well developed (Fig. 10A). The trends in
Al
2
O
3
and
TiO
2
contents are
not consistent and indicate ei-
ther different provenance or weathering and depositional his-
tory for the deposits of the ZP and the BB (Young & Nesbitt
1998; Passchier & Whitehead 2006). The studied deposits
reveal relatively low Al
2
O
3
and
TiO
2
values, characteristic
for granulites and granitoids (Passchier & Whitehead 2006).
Significant enrichment in Al with respect to average crystal-
line rocks (due to weathering) was not determined (Passchier
& Whitehead 2006). Several samples from the ZP and the
BB are relatively enriched in Al
2
O
3
(more than 12 %) proba-
bly caused by the matrix rich in kaolinite. The Ti : Al ratio
for the studied samples varies between 0.02 to 0.06 (average
0.04) for the BB and 0.01—0.07 (average 0.03) for the ZP.
Relatively low TiO
2
and Al
2
O
3
concentrations can be partly
explained by grain-size effect (Young & Nesbit 1998; Paschier
2004). In contrast to Al and Ti, which occur mainly in phyl-
losilicates concentrated in a finer mud fraction, Zr-bearing
minerals generally concentrate in the fine sand fraction.
A plot of TiO
2
/Zr—Zr/Al
2
O
3
(Fig. 10B) illustrates, that the
data follow completely different patterns and point to a differ-
ent provenance for the BB and the ZP samples (Passchier &
Whitehead 2006).
The value of the ratio K
2
O/Na
2
O (Roser & Korsch 1986)
for the studied sediments from the BB varies between 0.48
and 2.07 (average 1.28) and for the ZP between 0.32 and 3.3
(average 1.23). Such relatively low values reflect a deriva-
tion from the mainly primary sources and a highly varied
Fig. 8. Typology of zircons in the
Pupin-diagram (Pupin 1980).
Fig. 9. Discrimination plot of TiO
2
vs. Al
2
O
3
for investigated spinels.
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role of recycled sedimentary sources (McLennan et al. 1993;
Bock et al. 1998). Higher ratios (above 1) can reflect a deri-
vation from the recycled sedimentary sources with an ex-
tended weathering history (Roser & Korsch 1986). Similarly,
the K
2
O/Al
2
O
3
ratio can be used to estimate the degree of re-
cycling (Cox & Lowe 1995; Passchier 2004). Its value is be-
tween 0.14 and 0.44 for the BB and between 0.09 and 0.37
for the ZP. The relatively low ratios could indicate a source
from quartz-rich rocks and significant variations of the ratio
point to a variation in the content of recycled sediments.
Typically, samples from the basal depositional units of both
occurrences (i.e. Rockenbauer Sandstone Member and Basal
Red-Brown Formation) reveal the lowest value of recycling.
However, because of the relatively easy affection of the alkali
elements during weathering and diagenesis, the use of alkali
elements could be problematic.
The studied samples are sedimentary rocks from heteroge-
neous source rocks and have undergone sorting during trans-
portation in fluvial channels. The weathering indices could
reflect variations in parent rock composition rather than the
degree of weathering (Borghes & Huh 2007). The chemical
index of alteration is commonly used (CIA index – Nesbitt
& Young 1982), although due to the highly varying carbon-
ate content and absence of CO
2
data, a precise correction for
the carbonate CaO was difficult. After correcting for P
2
O
5
(apatite), the value of CaO is consequently accepted, if the
mole fraction of CaO Na
2
O. However, if CaO Na
2
O, it
was assumed, that the moles of CaO = Na
2
O (McLennan et
al. 1993). The CIA index ranges between 58 and 81 (aver-
age 63.4) for the BB and between 61 and 77 (average 67.4) for
the ZP. The CIA index of sediments is, in general, about 50 in
the case of first cycle sediments predominantly derived from
physically weathered igneous rocks, and tends to increase as
chemical weathering intensifies (Nesbitt & Young 1982). The
variations in the CIA index reflect differences in the propor-
tion of the content of weathered/recycled material. The effect
of chemical weathering depends on (1) intensity (controlled
primarily by the climate and vegetation) and (2) weathering
time. The second effect includes a complex set of factors, of
which the physiography is particularly important (Johnsson
1993; Le Pera et al. 2001). Higher CIA values may indicate
more intense chemical weathering in more humid conditions
or weathering in a sub-humid condition, whereas lower CIA
values can be attributed to an influx of less weathered detri-
tus under semi-arid conditions.
The studied sediments were plotted on the Al
2
O
3
—
(CaO + Na
2
O)—K
2
O diagram (Fig. 10C), (called A-CN-K in
the following text). The trends in A-CN-K
are
not consistent
for the ZP and the BB. The samples from the BB are ar-
ranged almost parallel to the A-CN axis and follow a trend of
increasing Al
2
O
3
(and slightly also K
2
O) with decreasing
CaO + Na
2
O. The elongated distribution reflects the varied
role of the weathering trend/clay minerals and can be associ-
ated with grain size variations (Corcoran 2005). The samples
from the ZP are more concentrated in the upper part of the
diagram near the feldspar join. Such a distribution indicates
a prevailing physical weathering and the low role of chemi-
cal weathering. The compositional variations between the
BB and the ZP reveal that the source rocks should be differ-
ent. Some deviations from the “ideal weathering trend” to-
wards an illite composition and similarly a subhorizontal
distribution of the samples can possibly be interpreted as a
result of an increase in K during diagenesis (Fedo et al.
1995; Bock et al. 1998; Ohta 2008). Alternatively, these pat-
terns may indicate the mixing of a moderately weathered
source with an unweathered one (McLennan et al. 1993).
Sample
SiO
2
Al
2
0
3
Fe
2
O
3
MgO CaO Na
2
O K
2
O TiO
2
P
2
O
5
MnO Cr
2
O
3
LOI
BB 1
73.93
10.46
2.1
0.86
3.55
3.02
1.45
0.24
0.09
0.1
0.013
4.1
BB 2
72.26
12.5
3.97
0.85
0.43
2.32
3.25
0.69
0.14
0.09
0.031
3.2
BB 3
78.82
11.21
0.52
0.15
0.29
2.39
4.94
0.16
0.13
0.01
0.007
1.2
BB 4
67.02
9.76
1.85
1.85
4.88
2.08
2.49
0.24
0.07
0.1
0.034
7.5
BB 5
75.36
10.97
1.72
0.97
1.64
2.93
3.27
0.24
0.11
0.03
0.012
2.6
BB 6
62.47
13.9
4.61
3.05
2.87
2.97
3.29
0.63
0.19
0.05
0.017
5.7
BB 7
65.7
13
4.6
1.88
3.12
2.21
2.62
0.63
0.14
0.08
0.01
5.8
BB 8
30.41
9.5
3.22
2.84
25.3
1.19
2.26
0.43
0.16
0.18
0.013
24.3
BB 9
62.13
11.11
3.99
1.35
7.51
2.19
2.46
0.51
0.1
0.1
0.009
8.4
BB 10
71.99
9.95
2.6
1.06
4.14
1.99
2.45
0.36
0.09
0.07
0.007
5.2
ZP 1
78.72
10.75
1.45
0.52
0.27
2.41
3.83
0.2
0.11
0.01
0.006
1.6
ZP 2
75.1
11.66
2.92
1.19
0.35
2.49
3.33
0.32
0.13
0.07
0.018
2.3
ZP 3
75.9
11.14
2.2
1.14
1.09
2.94
3.11
0.29
0.22
0.03
0.009
1.8
ZP 4
67.38
14.1
4.07
2.56
1.15
2.04
2.96
0.52
0.15
0.04
0.011
4.9
ZP 5
76.44
11.86
1.53
0.78
0.22
2.88
4.34
0.18
0.12
0.03
0.014
1.4
ZP 6
69.45
13.58
3.49
1.99
0.59
3.86
3.01
0.4
0.17
0.05
0.012
3.3
ZP 7
79.76
9.04
3.29
0.77
0.41
0.53
1.75
0.56
0.13
0.06
0.033
3.6
ZP 8
77.64
9.53
4.15
1.39
0.33
2.52
0.81
0.55
0.1
0.02
0.033
2.8
ZP 9
75.21
12.23
2.11
0.84
0.35
2.68
4.22
0.28
0.15
0.03
0.011
1.8
ZP 10
73.8
12.44
2.92
1.25
0.34
2.36
3.77
0.34
0.15
0.11
0.01
2.4
ZP 11
79.31
10.18
1.33
0.35
0.11
2.15
3.66
0.24
0.07
0.01
0.006
2.5
ZP 12
78.63
9.18
1.54
0.32
1.68
2.7
1.79
0.12
0.09
0.18
0.004
3.7
ZP 13
75.35
10.91
3.84
1.53
0.53
2.56
1.06
0.37
0.19
0.02
0.043
3.5
ZP 14
74.62
11
4.16
1.66
0.53
2.45
1.11
0.35
0.18
0.02
0.041
3.8
ZP 15
73.87
11.62
3.85
1.67
0.49
2.19
1.44
0.4
0.16
0.04
0.036
4.2
Table 3: The major element composition (%) of the studied samples (BB – Boskovice Basin, ZP – Zöbing area).
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Fig. 10. Discrimination plots of major element geochemistry. A –
TiO
2
vs.
Al
2
O
3
, B – TiO
2
/Zr vs. Zr/Al
2
O
3
, C – ternary diagram
Al
2
O
3
—(CaO + Na
2
O)—K
2
O, D – SiO
2
vs.
TiO
2
, E – SiO
2
/Al
2
O
3
vs. Na
2
O/K
2
O, F – classification diagram (Herron 1988), G – dis-
crimination diagram of tectonic setting (Roser & Korsch 1988).
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With no extra input of detritus the sediment recycling re-
sults in a negative correlation of SiO
2
and TiO
2
(Gu et al.
2002). Such a trend can be generally followed for the sam-
ples both from the ZP and the BB. Whereas in the ideal case
(Cox & Lowe 1995; Corcoran 2005) the overlying sequence/
formation should contain more quartz (i.e. SiO
2
), less feld-
spar and clays (lower content of TiO
2
, Al
2
O
3
and MgO) in
the studied cases the distribution is more complex (Fig. 10d).
This can be connected with several factors: a) variations in
fluvial discharge when a higher energy fluvial environment
inhibited the removal of finer-grained feldspar, clay and
heavy minerals richer in TiO
2
relatively to SiO
2
;
or b) by a
renewed uplift and erosion of the source area during the dep-
ositional history. Erosion of the high relief profile would
have resulted in the deposition of the stronger weathered
portion first (Youngston et al. 1998).
Ohta (2008) has demonstrated that the SiO
2
/Al
2
O
3
and
Na
2
O/K
2
O ratios are highly susceptible to the effect of hy-
draulic sorting and grain-size fractionation. On the SiO
2
/
Al
2
O
3
—Na
2
O/K
2
O diagram (Fig. 10E) two compositional
trends can be observed, in which the geochemical variability
induced by hydraulic sorting is expressed by the range and ex-
tent of these trends. The majority of samples (especially from
the BB) are arranged horizontally and derived from the quartz-
rich recycled sedimentary provenance. Certain samples (from
the Kalterbachgraben Sandstone/Siltstone Member of the ZP
and the Basal Red-Brown Formation of the BB) are arranged
obliquely and reveal an increased content of the material de-
rived from the crystalline/igneous provenances.
According to the diagram of Herron (1988), which utilizes
the major oxides, the studied sandstones (Fig. 10F) can be
classified as lithic arenites or arkoses, only a few of them as
wackes. In terms of tectonic setting (Fig. 10G), the studied
samples plot in the majority in the active continental margin
field, while a number of them are in the passive margin
(Roser & Korsch 1988). Such an interpretation of the tectonic
settings can be affected by the mobility of K and Na, particu-
larly during the weathering of feldspar.
Trace element geochemistry
The trace element composition is presented in Table 4. In
order to determine the tectonic setting associated with the
deposits, the samples were plotted on a Th-Zr/10-Sc and
La-Th-Sc ternary diagram (Bhatia & Crook 1986;
Fig. 11A,B). The different positions of the samples from the
BB and the ZP are visible. Whereas samples from the BB lie
out of the discrimination fields the samples from the ZP can
be found in the continental volcanic arc field (McLennan et
al. 1993; Bahlburg 1998). The Th/Sc ratios of the studied
formations of the BB vary between 0.82 and 5.6 (average
1.78) and for the ZP between 0.61 and 2.63 (average 1.52).
The Zr/Sc ratio of the studied formations of the BB varies
between 6.23 and 76.34 (average 23.24) and for the ZP be-
tween 10.00 and 39.95 (average 24.31). The samples show
the Th/Sc and Zr/Sc values (Fig. 11C) along the trend from
the mantle to the upper continental crust composition
(McLennan et al. 1993), the predominant provenance from
the upper continental crust, a relatively low and highly varied
role of the reworking and significant compositional hetero-
geneity in the source areas. The highest values of the factors
were recognized in the BB in the sample from the Rosice-
Oslavany Formation close to the coal seams whereas in the
ZP they come from the Kalterbachgraben Sandstone/Silt-
stone Member. Variations in the role of tectonics (slope, areal
Sample
Ni Th Sc La Rb Nb Zr V Ba Be Co
BB 1
24
6.1
6
13.9
60
4.8
85.3
39
144
1
6.2
BB 2
74.2
50.8
9
81.8
113.9
18.1
687.1
50
485
2
13.8
BB 3
8.8
9.5
3
12.5
154.7
5.1
86.8
14
944
2
2.4
BB 4
67.4
6.5
9
21.2
93.2
4.9
107.5
56
287
1
10.7
BB 5
40.5
9.4
5
17.6
106.5
4.7
88.3
30
541
1
4.5
BB 6
80.7
13.9
11
27.8
152
12.2
192.9
65
475
2
13.3
BB 7
30.4 12.4 12 26.2 106.4 10.2 201.8 76 500 3 10.9
BB 8
64.2
8.2
10
28.6
124.7
9.2
68.3
53
244
2
12.6
BB 9
26.7
9.8
10
32.1
101.5
9.1
179.2
64
405
2
7.4
BB 10
19.8
7.9
6
20.4
90.2
6.5
145.2
42
412
1
5.2
ZP 1
18.6
8
4
20.3
131.5
4.6
112.7
19
708
1
3.3
ZP 2
45.4
17.5
8
20.2
113.4
8.1
154.4
36
676
1
7.7
ZP 3
34.8
7.8
6
21.8
108.6
6.2
132.8
30
635
0.5
5.1
ZP 4
28.8
14.5
9
31.9
134.8
11
202.7
53
370
2
8.8
ZP 5
34.3
5.6
4
14.6
120
3.5
110.5
13
994
0.5
4.3
ZP 6
74.1
12.9
8
24.1
98.9
9.6
138.6
44
533
2
9.4
ZP 7
117.8
7.3
7
18.9
61.2
10.6
288.4
41
134
0.5
10.8
ZP 8
103.2
5.7
8
16.2
28.5
10.3
177.6
38
192
0.5
12.3
ZP 9
30.2
7.5
5
21.3
136.4
6.1
88.4
35
957
1
4.4
ZP 10
42.5
13.5
6
30.3
144
8.4
239.7
38
741
2
6.2
ZP 11
12.7
10.5
4
19.6
134.2
5.6
128.4
25
465
0.5
2.9
ZP 12
14.9
4.9
2
10.4
62
3.8
76.6
15
277
0.5
2.4
ZP 13
105.6
5.5
9
19.5
44.9
8.1
119
55
155
1
10.3
ZP 14
114.2
5.3
9
17
46.8
7.4
126.2
56
167
1
11.3
ZP 15
112.7
6.9
10
19.4
61
9.1
100
60
177
0.5
17.4
Table 4: The trace element composition (ppm) of the studied samples (BB – Boskovice basin, ZP – Zöbing area).
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Fig. 11. Discrimination plots of trace element geochemistry. A – Th-Zr/10-Sc ternary diagram, B – La—Th—Sc ternary diagram, C – Th/Sc
vs. Zr/Sc, D – Cr vs. Al
2
O
3
, E – Cr vs. TiO
2
, F – Ba vs. K
2
O.
extent, etc.) during the evolution of the basin are assumed to
be responsible for the variations in the value of these factors.
The Cr values of the studied formations of the BB vary from
47.8 to 232.6 ppm and for the ZP from 41 to 280.5 ppm. The
elevated content of the Cr (Cr above 150 ppm) was deter-
mined in the BB in samples from the Rosice-Oslavany For-
mation close to the coal seams whereas in the ZP it was from
the Kalterbachgraben Sandstone/Siltstone Member and the
Rockenbauer Sandstone Member. Samples from the upper
parts of the stratigraphic successions in both basins reveal a
generally lower content of Cr. An input from the mafic sources
would also result in an enrichment of Ni and V. The abun-
dances of Ni of the studied formations of the BB vary from
19.8 to 80.7 ppm and for the ZP from 18.6 to 117.8 ppm. The
V values of the studied formations of the BB vary from 14 to
76 ppm and for the ZP from 15 to 60 ppm. Elevated abun-
dances of Ni (i.e. Ni over 100 ppm) and the highest abundances
of V were determined for samples from the Kalterbachgraben
Sandstone/Siltstone Member and Rockenbauer Sandstone
Member. The Cr/Ni ratio for the BB is 1.44—3.45 and for the ZP
1.1—3.23. The elevated Cr and Ni abundances with low Cr/Ni
ratios (between 1.3—1.5) were suggested as having been indic-
ative of mafic/ultramafic rocks in the source area (Bock et al.
1998; Sensarma et al. 2008). Low Cr/Ni ratios were recog-
nized only in two samples from the Padochov Formation and
in one sample from the Heiligenstein Arkose Member. These
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results and also the high Y/Ni ratios (above 11.8 for the BB
and 18.7 for the ZP) point to the limited significance of a maf-
ic and ultramafic contribution to these deposits (McLennan et
al. 1993).
A poor correlation and different trends exist between Al
2
O
3
and TiO
2
with Cr (Fig. 11D,E), signifying differences in their
provenance. The different position of samples of the BB from
the Rosice-Oslavany Formation and of the ZP from the Kalter-
bachgraben Sandstone/Siltstone Member and Rockenbauer
Sandstone Member is remarkable.
The immobile Ba shows a particularly strong positive cor-
relation with K
2
O in both of the sample suites (Fig. 11F).
The differences in the provenance of the two catchments, de-
termined above, are discernible in the K
2
O-Ba distribution.
Variations in fluvial discharge (fluvial channel vs. crevasse
channel) are responsible for an increase in the contribution
of K-feldspar ± biotite increase in both the Ba and K contents
in the different samples from the same formation or member
(Padochov Formation and Kalterbachgraben Sandstone/Silt-
stone Member).
The Zr/Th ratio is another measure of the degree of recy-
cling. Its values vary from 8.3 to 18.4 for the BB, which is
close to the upper crustal average of 17.76. The Zr/Th ratio
for the ZP varies from 12.2 to 39.5. Such an enriched value
(above the UCC) results from the low values of both Th and
Zr (in comparison with the BB) especially from the lower Th
concentrations. Th is commonly abundant in heavy minerals
like monazite, zircon, titanite, the minerals of the epidote
group and clay minerals. The results point to different prove-
nance and the lower role of recycling in the ZP since the con-
centrations of the heavy minerals during recycling would
accordingly lead to an increase in Zr and Th abundances in
the respective deposits (Zimmermann & Bahlburg 2003).
Discussion
Clear differences in the composition of the detrital materi-
al of the fluvial sandstones of the BB and the ZP were identi-
fied in all the employed analytical techniques (petrography,
heavy mineral studies, geochemistry of both major and trace
elements) and indicate different source areas. Therefore the
assumed communication between the BB and the ZP during
the Late Paleozoic (Jaroš & Mísař 1967) is unlikely. The tra-
ditional model of a single narrow half graben occupied by an
axial drainage with transport to the south (Malý 1993) is also
questionable. The existence of “colinear” marginally offset
half grabens with predominant transversal sources can be as-
sumed.
Improved determination of the source areas and their evo-
lution was the second target of the study. The predominance
of quartz as well as certain amounts of plagioclase and alkali
feldspar reflects the derivation of detritus from the pre-exist-
ing sedimentary rocks (especially in the BB) and granitic
rocks exposed in the source area (particularly in the ZP).
Polycrystalline quartz grains are an additional indicator of
the metamorphic source. The preservation and transport of
feldspar, particularly of less stable plagioclase, are indicators
of limited chemical weathering conditions (Einsele 1992).
All the geochemical indicators would indicate the derivation
from mainly primary sources (particularly in the case of the
ZP) and the highly varied role of recycled sedimentary
sources (particularly in the case of the BB). The most signifi-
cant differences in the source areas are predominantly in the
sedimentary rocks, volcanics and recycling.
The significant presence of garnet and the occurrence of stau-
rolite mainly indicate mica schist complexes as sources. The
monotonous spectra of the garnet composition indicate a first
cycle detritus and the predominant garnet provenance from
metamorphic rocks such as gneisses, (amphibole + biotite)
schists and granulites in the ZP. The wide spectrum of garnet
composition in the BB indicates either a more complex source
area (gneisses, amphibole+biotite schists, granulites, calc-sili-
cate rocks or marbles, eclogites) or reflects the redeposition of
an older sedimentary cover close to the basin. A comparison
with data from greywackes of the Drahany Culm Unit (Otava
et al. 2000; Čopjaková 2007) reveals important similarities
(a wide spectrum of garnet composition, extremely similar
garnet types). The erosion and redeposition of the older Culm
deposits is also documented by the occurrences of Culm peb-
bles within the conglomerates of the BB.
ZTR minerals are common in acidic to intermediate mag-
matic rocks as well as in mature siliciclastic sediments and
certain metamorphic rocks (Eynatten & Gaupp 1999). More-
over, high ZTR values commonly characterize relatively old
sandstones, because extensive diagenetic dissolution reduces
the mode of less stable minerals (Garzanti & Andó 2007).
The predominant provenance of rutile from metapelitic rocks
(mica schists, paragneisses, felsitic granulites) both in the ZP
(62.5 %) and the BB (50.8 %) is evident. Approximately
38.8 % of the rutiles from the BB originate from metamafic
rocks (eclogites, mafic granulites) whereas only 14.1 % of
such provenance was recognized in the ZP. Approximately
21 % of the studied rutile from the ZP in all probability orig-
inated from magmatic rocks (pegmatites?), but only about
6 % are of such provenance in the BB. Approximately 2.4 %
or 4.4 % of the rutile could not be discriminated in relation
to the source rocks.
The spectra of zircons of the BB show a higher content of
rounded and subrounded zircons, a lower value of elonga-
tion, a lower content of “highly” elongated zircons, a higher
content of zoned zircons, zircons with older cores and
opaque zircons than in the ZP. All this would indicate the in-
creased role of recycled detritus and metamorphic rocks in
the provenance of the BB and the increased role of magmatic
and volcanic rocks in the source area of the ZP. The parental
magma of magmatic zircons for the ZP had a slightly higher
alkaline content (Al
2
O
3
vs. Na
2
O + K
2
O) than for the BB
(differences in the composition of granitoids were also con-
firmed by petrography). Direct identification of the source of
the zircons lacks sufficient data from the possible prove-
nance rocks. Niedermayr (1967) has documented the elonga-
tion of zircons for the Gföhl gneiss between 1.8 and 2.3 and
for the granulites of St. Leonhard between 1.5 and 1.7.
Hoppe (1966) has revealed the elongation in the granulites
of St. Leonhard of about 2.
Apatite may be derived from biotite-rich rocks but is a
common accessory mineral in almost all igneous and a num-
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ber of metamorphic rocks (Adhikari & Wagreich 2011). Epi-
dote was derived from the low-grade metamorphic series.
Kyanite indicates the presence of high-pressure metamor-
phic rocks. The presence of andalusite also reveals the prov-
enance from a higher-T metamorphic facies. Spinels indicate
the existence of basic/ultrabasic rocks in the source area.
Whereas Moravian and adjacent Moravo-Silesian Paleozoic
deposits (Culm facies) represent the predominant source area
for the studied part of the BB, the Moldanubian Unit was the
predominant source area for the ZP. This implies for the BB
a complex transport direction both from the west and east. In
the Zöbing area the main part of the Moldanubian Unit is
west of the ZP but today it is also bordering it in the east. But
the Moldanubian rocks east of the ZP are displaced by the
Diendorf fault system and it is very doubtful, if this was al-
ready the case in the Late Paleozoic. Therefore a transport
direction for the ZP cannot be clearly determined.
The amount of analyses is limited thus we can only specu-
late as to the general evolution in the source area. A local
source from weathered crystalline rocks can be assumed for
the basal successions both in the BB and the ZP. A wider
provenance, less weathered detritus, the predominance of
mica schist complexes and the minor role of reworking and
floodplain modifications can be assumed for additional parts
of the succession in the ZP. A wider provenance, variations in
the input of the first cycles of detritus from the wide spectra of
metamorphic rocks and the recycled detritus (older sedimen-
tary rocks) as well as floodplain modifications can be assumed
for the additional parts of the succession of the BB, in all
probability with the rising importance of the source from the
older (Culm) deposits upwards. The provenance evolution
over time does not indicate the successive exhumation of a
simple structured (lower- to higher grade metamorphic
source) orogen but may be interpreted as differences in expan-
sion in the source areas. The source areas seem to be largely
stable during the depositional history, reflecting the tectonic
history and the resulting depositional phases.
Identification of the paleogeographical, climatic and tec-
tonic events responsible for the material supply was the last
and most complicated target of the study. Sedimentological
studies, identification of the depositional environment, its
evolution, along with the identification of the ruling factors
of deposition (i.e. tectonics and climatic processes) should
be compared with changes in petrography and geochemistry
in order to fulfil such a target.
The studied sandstones are poorly sorted and reveal a rela-
tively immature composition implying a short transport dis-
tance and rapid deposition. The high content of micas can be
interpreted in a similar manner, as the detrital muscovite
rarely survives multiple depositional cycles. The higher pro-
portion of unstable lithic components and the moderately
high feldspar content indicate a high-relief source area. The
prevailing physical weathering and the low role of chemical
weathering can be confirmed by geochemistry. Wide fluctu-
ations of mineral percentages and indices indicate local
sources such as an adjacent alluvial fan, which is in accor-
dance with the interpreted depositional environments. These
types of fluctuations are regarded as typical for post-orogenic
sedimentary basin fills such as the extensional collapse gra-
bens. They can also reflect the hydraulic conditions during
deposition (Morton 1985).
The role of climatic variations in the formation of a heavy
mineral suite is probable. The significantly lower contents of
apatite were determined in the Stephanian deposits whereas
Autunian deposits are characterized by a higher content. Wide
variations in the ATi ratios suggest that the ratio are likely to
be, at least in part, a function of weathering during alluvial
storage (dissolved by contact with acidic waters) (Morton &
Hallsworth 1999; Hallsworth & Chisholm 2008; Adhikari &
Wagreich 2011). A possible burial of deposits below 3.5 km
calls into question the validity of the GZi, ATi and MZi indices.
Conclusions
The erosional remnants of the continental Permo-Carbon-
iferous deposits of the Boskovice Basin in Moravia and the
Zöbing Upper Paleozoic in Lower Austria have recorded the
paleogeographic, tectonic and climatic post-Variscan history
of the Bohemian Massif. A wide spectrum of methods of
provenance analyses of the fluvial sandstones (petrography,
heavy mineral assemblages, chemistry of garnet, rutile and
spinel, zircon study, major and trace elements) were used to
confirm or deny the generally supposed and published com-
munication of these at present isolated Permo-Carboniferous
deposits and for better determination of the source areas and
their evolution.
The results would indicate different source areas for the
studied rocks of both basins. The detritus of the Upper Paleo-
zoic deposits in the Zöbing area was predominantly derived
from primary sources formed by crystalline rocks. The role
of metamorphites (particularly metapelitic rocks – mica
schists, paragneisses, felsitic granulites) was predominant
along with the importance of the presence of magmatic and
volcanic rocks. The source area is predominantly located in
the Moldanubian Unit.
The source from the primary crystalline units (magmatic
and metamorphic rocks) with a relatively wider range of meta-
morphites, along with the derivation of the detritus from pre-
existing sedimentary rocks (in particular Moravo-Silesian
Paleozoic deposits) has been demonstrated for the analysed
part of Boskovice Basin. The metapelitic rocks (mica schists,
paragneisses, felsitic granulites) predominate in addition to
the importance of the metamafics (eclogites, mafic granulites).
The Moravian Unit and the adjacent Drahany Culm unit repre-
sent the predominant source areas while the transport direction
was complex (both from the west and east).
The general provenance evolution over time may be inter-
preted as differences in expansion in the source areas. The
basal successions both in the Boskovice Basin and the
Zöbing area are typified by material from the local/adjacent
sources whereas the wider provenance and variations in the
role of the primary and recycled detritus are assumed for the
further parts of the successions.
The assumed communication between the southern part of
the Boskovice Basin and the Zöbing area during the Late
Paleozoic and the existence of a single narrow half graben oc-
cupied by axial drainage (with transport from north to south,
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cf. Jaroš & Mísař 1967) is improbable. An existence of “colin-
ear” marginally offset half grabens with predominated trans-
versal sources can be assumed. The examined fluvial
sandstones reveal short transport distance, rapid deposition,
high-relief source area, and prevailed physical weathering and
a minor role of chemical weathering. Wide fluctuations of the
mineral percentages and indices indicate local sources such as
an adjacent alluvial fan, which is in accordance with the inter-
preted depositional environments. The type of fluctuations is
regarded as typical for post-orogenic sedimentary basin fills
such as those found in extensional collapse grabens.
Acknowledgments: The authors wish to thank the Grant
Agency of the Czech Republic, which kindly sponsored the
costs of the analytical data and part of the field work with the
Project No. 205/09/1257. The second part of the field work
was generously sponsored by the Geological Survey of Aus-
tria. We are grateful to Fritz F. Steininger for his help during
field work and stratigraphic issues. The authors would like to
thank D. Puglisi and an unknown reviewer for their critical
and stimulating comments, which greatly helped improve
the manuscript.
References
Adhikari B.R. & Wagreich M. 2011: Provenance evolution of col-
lapse graben fill in the Himalaya – The Miocene to Quaternary
Thakkola-Mustang Graben (Nepal). Sed. Geol. 233, 1—14.
Alexander J., Bridge J.S., Leeder M.R., Collier R.E. & Gawthorpe
R.I. 1994: Holocene meander-belt evolution in an active exten-
sional basin, SW Montana, USA. J. Sed. Res. B64, 542—559.
Bachmayer F. & Vasicek W. 1967: Insektenreste aus dem Perm von
Zöbing bei Krems in Niederösterreich. Ann. Naturhist. Mus.
Wien, 71, 13—18 (in German).
Bahlburg H. 1998: The geochemistry and provenance of Ordovician
turbidites in the Argentinian Puna. In: Pankhurst R.J. & Rapela
C.W. (Eds.): The Proto-Andean Margin of Gondwana. Geol.
Soc. London, Spec. Publ. 142, 127—142.
Berger W. 1951: Neue Pflanzenfunde aus dem Rotliegenden von
Zöbing (Niederösterreich). Anz. Österr. Akad. Wiss., Math.-
Naturwiss. Kl. 88/11, 288—295.
Bhatia M.R. & Crook A.W. 1986: Trace element characteristics of
graywackes and tectonic setting discrimination of sedimentary
basins. Contr. Mineral. Petrology 92, 181—193.
Bock B., McLennan S.M. & Hanson G.N. 1998: Geochemistry and
provenance of the Middle Ordovician Austin Glen Mb. (Nor-
manskill Formation) and the Taconian Orogeny in New En-
gland. Sedimentology 45, 635—655.
Borges J. & Huh Y. 2007: Petrography and chemistry of the bed
sediments of the Red River in China and Vietnam: Provenance
and chemical weathering. Sed. Geol. 194, 155—168.
Bridge J.S. & Leeder M.R. 1979: A simulation model of alluvial
stratigraphy. Sedimentology 26, 617—644.
Cichocki O., Popovtschak M., Szameit E. & Vasicek W. 1991: Ex-
cursion A, 22. September 1991: Northern Lower Austria. In:
Kovar-Eder J. (Ed.): Palaeovegetational development of Europe.
Pan-European Palaeobotanical Conference, Wien, Field-Guide,
5—22.
Corcoran P.L. 2005: Recycling and chemical weathering in tectoni-
cally controlled Mesozoic-Cenozoic basins of New Zealand.
Sedimentology 52, 757—774.
Cox R. & Lowe D.R. 1995: A conceptual review of regional-scale
controls on the composition of clastic sediment and the co-evo-
lution of continental blocks and their sediment cover. J. Sed.
Res. A65, 1, 548—558.
Čopjaková R. 2007: Evidence of changes of provenance in the pse-
fitic and psammitic fraction of deposits of Myslejovice Forma-
tion. [Odraz změn provenience v psefitické a psamitické frakci
sedimentů myslejovického souvrství.] PhD Thesis, Faculty of
Science, MU Brno, 1—81 (in Czech).
Čepek L. 1946: The tectonics of the Boskovice Furrow. [Tektonika
boskovické brázdy.] Věst. Stát. Geol. Úst. Rep. Československé
20, 1—6, 128—130 (in Czech).
Cžjžek J. 1849: Geognostische Karte der Umgebungen von Krems
und vom Manhardsberge. Maßstab. 1 : 72,000. Wien.
Cžjžek J. 1853: Erläuterungen zur geologischen Karte der Umge-
bungen von Krems und vom Manhartsberg. Sit.-Ber. K. Akad.
Wiss., Math.-Naturwiss . Kl., Beilage 7, 1—77.
Dickinson W.R. 1985: Interpreting provenance relations from detri-
tal modes of sandstones. In: Zuffa G.G. (Ed.): Provenance of
Arenites. D. Reidel Publication Co., 333—361.
Dickinson W.R. 1990: Clastic petrofacies. In: Miall A.D. (Ed.):
Principles of sedimentary basin analysis. Springer Verlag,
New York, 1—668.
Dickinson W.R. & Suczek Ch.A. 1979: Plate tectonics and sandstone
composition. Amer. Assoc. Petrol. Geol. Bull. 63, 2164—2182.
Einsele G. 1992: Sedimentary basis. Springer Verlag, Berlin, 1—648.
Ettingshausen C.v. 1852: Beitrag zur näheren Kenntniss der Flora der
Wealdenperiode. Abh. K.-Kön. Geol. Reichsanst. 1/3, 1—32.
Eynatten H. von & Gaupp R. 1999: Provenance of Cretaceous syno-
rogenic sandstones in the Eastern Alps: constraints from
framework petrography, heavy mineral analysis, and mineral
chemistry. Sed. Geol. 124, 81—111.
Eynatten H. von 2004: Statistical modelling of compositional trends
in sediments. Sed. Geol. 171, 79—89.
Fedo C.M., Nesbitt H.W. & Young G.M. 1995: Unravelling the ef-
fects of potassium metasomatism in sedimentary rocks and pa-
leosoils, with implications for paleoweathering conditions and
provenance. In: Price J.R. & Velbel M.A. (Eds.): Chemical
weathering indices applied to weathering profiles developed on
heterogeneous felsic metamorphic parent rocks. Chem. Geol.
202, 397—416.
Flügel E. 1960: Nichtmarine Muscheln aus dem Jungpaläozoikum
von Zöbing (Niederösterreich). Verh. Geol. Bundesanst. 1960/1,
78—82.
Fuchs W., Grill R., Matura A. & Vasicek W. 1984: Geologische
Karte der Republik Österreich 1 : 50,000. 38 Krems. Geol.
Bundesanst.
Garzanti E. & Andó S. 2007: Heavy mineral concentration in mod-
ern sands: implications for provenance interpretation. In:
Mange M.A. & Wright D.T. (Eds.): Heavy minerals in use.
Developments in Sedimentology 58, 517—545.
Gawthorpe R.L. & Leeder M.R. 2000: Tectono-sedimentary evolu-
tion of active extensional basins. Basin Res. 12, 195—218.
Gawthorpe R.L., Hardy S. & Ritchie B. 2003: Numerical modelling
of depositional sequences in half-graben rift basins. Sedimen-
tology 50, 169—185.
Gu X.X., Liu J.M., Zheng M.H., Tang J.X. & Qi L. 2002: Provenance
and tectonic setting of the Proterozoic turbidites in Hunan, South
China: geochemical evidence. J. Sed. Res. 72, 393—407.
Hallsworth C.R. & Chisholm J.I. 2008: Provenance of late Carbon-
iferous sandstones in the Pennine Basin (UK) from combined
heavy mineral, garnet geochemistry and paleocurrent studies.
Sed. Geol. 203, 196—212.
Havlena V. 1964: The geology of coal deposits. [Geologie uhelných
ložisek.] II. Nakl. Čes. Akad. Věd, Praha, 1—437 (in Czech).
Herron M.M. 1988: Geochemical classification of terrigenous sands
and shales from core and log data. J. Sed. Petrology 58, 820—829.
381
PROVENANCE OF PERMO-CARBONIFEROUS FLUVIAL SANDSTONES
GEOLOGICA CARPATHICA
GEOLOGICA CARPATHICA
GEOLOGICA CARPATHICA
GEOLOGICA CARPATHICA
GEOLOGICA CARPATHICA, 2012, 63, 5, 365—382
Holger Ph. A. Ritter von 1842: Geognostische Karte des Kreises ob
dem Manhartsberge in Oesterreich unter der Ens, nebst einer
kurzen Beschreibung der daselbst vorkommenden Felsarten.
1—44, 1 Geol. Map (1841).
Hoppe G. 1966: Zirkone aus Granuliten. Ber. Dtsch. Gesell. Geol.
Wiss. R. B 11/1, 47—81.
Hubert J.F. 1962: A zircon-tourmaline-rutile maturity index and the
interdependence of the composition of heavy mineral assem-
blages with the gross composition and texture of sandstones. J.
Sed. Petrology 32/3, 440—450.
Ingersoll W.R. 1990: Actualistic sandstone petrofacies: Discrimi-
nating modern and ancient source rocks. Geology 18, 737—736.
Jaroš J. 1961: The geological evolution of the southern part of the
Boskovice Furrow. [Geologický vývoj jižní části Boskovické
brázdy.] Acta Ac. Sci. Czechoslovenicae Basis Brunensis 32/12,
545—569 (in Czech).
Jaroš J. & Mísař Z. 1967: The problem of the deep-seated fault of the
Boskovice Furrow. [Problém hlubinného zlomu boskovické
brázdy.] Sbor. Geol. Věd, Geol. 12, 131—147 (in Czech).
Johnsson M.J. 1993: The system controlling the composition of
clastic sediments. In: Johnsson M.J. & Basu A. (Eds.): Pro-
cesses controlling the composition of clastic sediments. Geol.
Soc. Amer., Spec. Pap. 284, 1—19.
Kalvoda J., Bábek O., Fatka O., Leichmann J., Melichar R., Nehyba
S. & Špaček P. 2008: Brunovistulian terrane (Bohemian Mas-
sif, Central Europe) from late Proterozoic to late Paleozoic: a
review. Int. J. Earth Sci. 97, 497—517.
Kamenetsky V.S., Crawford A.J. & Meffre S. 2001: Factors con-
trolling chemistry of magmatic spinel: an empirical study of
associated olivine, Cr-spinel and melt inclusions from primi-
tive rocks. J. Petrology 42, 655—672.
Kukal Z. 1986: Manual of practical sediment nomenclature and
classification. [Návod k pojmenování a klasifikaci sedimentů.]
Czech Geol. Surv., Praha, 1—80 (in Czech).
Le Pera E., Arribas J., Critelli S. & Tortosa A. 2001: The effects of
source rocks and chemical weathering on the petrogenesis of
siliciclastic sands from the Neto River (Calabria, Italy): impli-
cations for provenance studies. Sedimentology 48, 357—378.
Leeder M.R. & Jackson J. 1993: The interaction between normal
faulting and drainage in active extensional basins, with exam-
ples from the western United States and central Greece. Basin
Res. 5, 79—102.
Mack G.H. & Stout D.M. 2005: Unconventional distribution of fa-
cies in a continental rift basin: the Pliocene-Pleistocene Man-
gas Basin, south-western New Mexico, USA. Sedimentology
52, 1187—1205.
Mack G.H. & Leeder M.R. 1999: Climatic and tectonic controls on
alluvial-fan and axial-fluvial sedimentation in the Plio-Pleis-
tocene Paleomas half graben, southern Rio Grande Rift. J. Sed.
Res. 69, 635—652.
Mackey S.D. & Bridge J.S. 1995: Three-dimensional model of allu-
vial stratigraphy: theory and application. J. Sed. Res. 65, 7—31.
Malý L. 1993: Formation of the Permo-Carboniferous depositional
basin of Boskovice Furrow and evolution of the Upper
Stephanian deposition in the Rosice-Oslavany sub-basin. [For-
mování sedimentační pánve permokarbonu boskovické brázdy a
vývoj svrchnostefanské sedimentace v rosicko-oslavanské pánvi.]
In: Přichystal A., Obstová V. & Suk M. (Eds.): Geologie Moravy
a Slezska. MZM Brno, 87—99 (in Czech).
Martínek K., Šimůnek Z., Drábková J., Zajíc J. & Nehyba S. 2009:
Carboniferous/Permian boundary in the continental basins of
the Bohemian Massif (Czech Republic): sedimentary environ-
ments and biota. Abstracts of IAS Meeting, Alghero, 265.
Mastalerz K. & Nehyba S. 1992: Paleogeography and paleoflows in
the SW part of the Boskovice basin during Stephanian/Autunian.
Seminarium Sedymentologiczne, Poznaň, 128—129 (in Polish).
Mastalerz K. & Nehyba S. 1997: Comparison of Rotliegende lacustrine
depositional sequences from the Intrasudetic, North-Sudetic and
Boskovice basin (Central Europe). Geol. Sudetica 30, 21—57.
McLennan S.M., Heming S.R., McDaniel D.K. & Hanson G.N.
1993: Geochemical approaches to sedimentation, provenance,
and tectonics. In: Johnsson M.J. & Basu A. (Eds.): Processes
controlling the composition of clastic sediments. Geol. Soc.
Amer., Spec. Pap. 284, 1—19.
Meinhold G., Anders B., Kostopoulos D. & Reischmann T. 2008:
Rutile chemistry and thermometry as provenance indicator: An
example from Chios Island, Greece. Sed. Geol. 203, 98—111.
Mikuláš R. & Martínek K. 2006: Ichnology of the non-marine de-
posits of the Boskovice basin (Carboniferous—Permian, Czech
Republic). Bull. Geosci. 81, 81—91.
Morton A.C. 1985: Heavy minerals in provenance studies. In: Zuffa
G.G. (Ed.): Provenance of Arenites. D. Reidel Publication Co.,
249—277.
Morton A.C. & Hallsworth C.R. 1999: Processes controlling the
composition of heavy mineral assemblages in sandstones. Sed.
Geol. 124, 3—29.
Nesbitt H.W. & Young G.M. 1982: Early Proterozoic climates and
plate motions inferred from major element chemistry of lutites.
Nature 299, 21, 715—717.
Niedermayr G. 1967: Die akzessorischen Gemengteile von Gföhler
Gneis, Granitgneis und Granulit im niederösterreichischen
Waldviertel. Ann. Naturhist. Mus. Wien 70, 19—27.
Ohta T. 2008: Measuring and adjusting the weathering and hydrau-
lic sorting effects for rigorous provenance analyses of sedi-
mentary rocks: a case study from the Jurassic Ashikita Group,
south-west Japan. Sedimentology 55, 1687—1701.
Otava J., Sulovský P. & Čopjaková R. 2000: Changes of provenance
of wackes of the Drahany Kulmian: a statistic evidence. [Změny
provenience drob drahanského kulmu: statistické posouzení.]
Geol. Výzk. na Moravě a ve Slezsku v r. 1999, 94—98 (in Czech).
Partsch P. 1843: Geognostische Karte des Beckens von Wien und der
Gebirge, die dasselbe umgeben – oder – Erster Entwurf einer
geognostischen Karte von Österreich unter der Enns mit Theilen
von Steiermark, Ungern, Mähren, Böhmen und Österreich ob
der Enns. K. K. Hof- u. Staats-Aerearial-Druckerei.
Partsch P. 1844: Erläuternde Bemerkungen zur geognostischen
Karte des Beckens von Wien und der Gebirge, die dasselbe
umgeben. 1—24.
Passchier S. 2004: Variability in geochemical provenance and
weathering history of Sirius group strata, Transantarctic
Mountains: implications for Antarctic glacial history. J. Sed.
Res. 74, 5, 607—619.
Passchier S. & Whitehead J.M. 2006: Anomalous geochemical
provenance and weathering history of Plio-Pleistocene glacio-
marine fjord strata, Bardin Bluffs Formation, East Antarctica.
Sedimentology 53, 929—942.
Peakal J., Leeder M.R., Best J. & Ashworth P. 2000: River response
to lateral ground tilting: a synthesis and some implications for
the modelling of alluvial architecture in extensional basins.
Basin Res. 12, 413—424.
Pešek J., Holub V., Jaroš J., Malý L., Martínek K., Prouza V., Spudil
J. & Tásler R. 2001: Geology and deposits of Upper Palaeozoic
limnic basins of the Czech Republic. [Geologie a ložiska
svrchnopaleozoických limnických pánví České republiky.]
Český Geologický Ústav Praha, 1—244 (in Czech).
Petránek J. 1963: Sedimentary rocks. [Usazené horniny.] Czech
Academy of Sciences, Praha, 1—717 (in Czech).
Pettijohn F.J., Potter P.E. & Siever R. 1987: Sand and sandstone.
Springer-Verlag, Berlin, 1—533.
Pober E. & Faupl P. 1988: The chemistry of detrial chromian
spinels and its implications for the geodynamic evolution of
the Eastern Alps. Geol. Rdsch. 77, 3, 641—670.
382
NEHYBA, ROETZEL and MAŠTERA
GEOLOGICA CARPATHICA
GEOLOGICA CARPATHICA
GEOLOGICA CARPATHICA
GEOLOGICA CARPATHICA
GEOLOGICA CARPATHICA, 2012, 63, 5, 365—382
Pupin J.P. 1980: Zircon and granite petrology. Contr. Mineral. Pe-
trology 73, 207—220.
Pupin J.P. 1985: Magmatic zoning of hercynian granitoids in France
based on zircon typology. Schweiz. Mineral. Petrogr. Mitt. 65,
29—56.
Roser B.P. & Korsch R.J. 1986: Determination of tectonic setting of
sandstone-mudstone suites using SiO
2
content and K
2
O/Na
2
O
ratio. J. Geol. 94, 635—650.
Roser B.P. & Korsch R.J. 1988: Provenance signatures of sand-
stone—mudstone suites determined using discrimination func-
tion analysis of major-element data. Chem. Geol. 67, 119—139.
Schermann O. 1971: Bericht über die Neukartierung des Perms bei
Zöbing (Blätter 21 und 38). Verh. Geol. Bundesanst. 1971/4,
A67—A68.
Schindler T. & Hampe O. 1996: Eine erste Fischfauna (Chondrich-
thyes, Acanthodii, Osteichthyes) aus dem Permokarbon Nied-
erösterreichs (Zöbing, NE Krems) mit paläoökologischen und
biostratigraphischen Anmerkungen. Beitr. Paläont. 21, 93—103.
Sensarma S., Rajamani V. & Tripathi J.K. 2008: Petrography and
geochemical characteristics of the sediments of the small River
Hemavati, Southern India: Implications for provenance and
weathering processes. Sed. Geol. 205, 111—125.
Stur D. 1870: Beiträge zur Kenntniss der Dyas- und Steinkohlenfor-
mation im Banate. Jb. K.-Kön. Geol. Reichsanst. 20, 2, 185—200.
Suess F.E. 1912: Die moravischen Fenster und ihre Beziehung zum
Grundgebirge des Hohen Gesenkes. Denkschr. K. Akad. Wiss.,
Math.-Naturwiss. Kl. 88, 541—631.
Šimůnek Z. & Martínek K. 2008: Study of Late Carboniferous and
Early Permian plant assemblages from the Boskovice Basin,
Czech Republic. Rev. Palaeobot. Palynol. 152, 237—269.
Štramberk S., Zajíc S., Martínek K. & Prouza V. 2008: Excursion
guide – Krkonoše Piemont basin and Boskovice graben – Fau-
nas and palaeoenvironments of the Late Palaeozoic. Spec.
Publ. to 5th Symposium on Permo-Carboniferous Faunas, Mu-
seum of Eastern Bohemia at Hradec Králové, 7—11.
Tenchov Y.G. 1980: Die paläozoische Megaflora von Österreich.
Eine Übersicht. Verh. Geol. Bundesanst. 1980/2, 161—174.
Vasícek W. 1974: Bericht 1973 über Aufnahmen im Perm von
Zöbing auf den Kartenblättern Horn (21) und Krems (38).
Verh. Geol. Bundesanst. 1974/4, A114—A115.
Vasícek W. 1975: Blatt 21, Horn. Geologische Aufnahme (Paläozoi-
kum). Verh. Geol. Bundesanst. 1975/1, A25—A26 (in German).
Vasícek W. 1977: Perm von Zöbing. Arbeitstagung Geol. Bunde-
sanst., Waldviertel, 15.—20. Mai 1977, 16—18, 69—72.
Vasícek W. 1983: 280 Millionen Jahre alte Spuren der Steinkohlen-
wälder von Zöbing. Katalogreihe des Krahuletz-Museums 4,
15—50.
Vasícek W. 1991a: Das Jungpaläozoikum von Zöbing. In: Roetzel R.
(Ed.): Geologie am Ostrand der Böhmischen Masse in Niederös-
terreich. Schwerpunkt Blatt 21 Horn. Arbeitstagung Geol.
Bundesanst., Eggenburg 16.—20. 9. 1991, 98—101.
Vasícek W. 1991b: Das Jungpaläozoikum von Zöbing. In: Nagel D.
& Rabeder G. (Eds.): Exkursionen im Jungpaläozoikum und
Mesozoikum Österreichs. Exkursionsführer Österr. Paläont.
Gesell., 1—2.
Vasícek W. & Steininger F.F. 1996: Jungpaläozoikum von Zöbing.
In: Steininger F.F. (Ed.): Erdgeschichte des Waldviertels.
Schr. Waldviertler Heimatbundes 38, 62—72.
Vohryzka K. 1958: Geologie und radiometrische Verhältnisse in
den jungpaläozoischen Sedimenten von Zöbing, N.-Ö. Verh.
Geol. Bundesanst. 1958/2, 182—187.
Waldmann L. 1922: Das Südende der Thayakuppel. Jb. Geol.
Bundesanst. 72/3—4, 183—204.
Young G.M. & Nesbitt H.W. 1998: Processes controlling the distri-
bution of Ti and Al in weathering profiles, siliciclastic sedi-
ments and sedimentary rocks. J. Sed. Res. 68, 3, 448—455.
Youngston J.H., Craw D., Landis C.A. & Schmitt K.R. 1998: Redefi-
nition and interpretation of late Miocene Pleistocene terrestrial
stratigraphy, Central Otago, New Zealand. New Zealand J. Geol.
Geophys. 41, 51—68.
Zack T., Eynatten H. von & Kronz A. 2004a: Rutile geochemistry
and its potential use in quantitative provenance studies. Sed.
Geol. 171, 37—58.
Zack T., Moraes R. & Kronz A. 2004b: Temperature dependence of
Zr in rutile: empirical calibration of a rutile thermometer. Contr.
Mineral. Petrology 148, 471—488.
Zajíc J. 2002: Vertebrate biozonation of the limnic Permo-Carbon-
iferous deposits of the Czech Republic in the light of the last
fossil finds. Workshop “Oberkarbon-Untertrias in Zentraleu-
ropa: Prozesse und ihr Timing” TU Bergakademie Freiberg,
37—38.
Zajíc J. & Štamberk S. 2004: Selected important fossiliferous hori-
zon of the Boskovice Basin in the light of the new zoopaleon-
tological data. Acta Musei Reginae Hradecensis S.A., Hradec
Králové 30, 5—15.
Zimmermann U. & Bahlburg H. 2003: Provenance analysis and tec-
tonic setting of the Ordovician clastic deposits in the southern
Puna Basin, NW Argentina. Sedimentology 50, 1079—1104.
Zimmermann U. & Spalletti L.A. 2009: Provenance of the Lower
Paleozoic Balcarce Formation (Tandilia System, Buenos Aires
province, Argentina): Implications for paleogeographic recon-
struction of SW Gondwana. Sed. Geol. 219, 7—23.
Zimmerle W. 1979: Accessory zircon from rhyolite, Yellowstone
National Park (Wyoming, U.S.A.). Z. Dtsch. Geol. Gesell. 130,
361—369.
Zuffa G.G. 1980: Hybrid arenites: Their composition and classifica-
tion. J. Sed. Petrology 50, 21—29.
Zuffa G.G. 1985: Optical analyse of arenites: influence of metodol-
ogy on compositional results. In: Zuffa G.G. (Ed.): Provenance
of arenites. D. Reidel Publishing Copany, Dordrecht, 333—361.