www.geologicacarpathica.sk
GEOLOGICA CARPATHICA, OCTOBER 2010, 61, 5, 365—381 doi: 10.2478/v10096-010-0022-3
High resolution stratigraphy of the Jurassic-Cretaceous
boundary interval in the Gresten Klippenbelt (Austria)
ALEXANDER LUKENEDER
1,
*, EVA HALÁSOVÁ
2
, ANDREAS KROH
1
, SUSANNE MAYRHOFER
1
,
PETR PRUNER
3
, DANIELA REHÁKOVÁ
2
, PETR SCHNABL
3
, MARIO SPROVIERI
4
and MICHAEL WAGREICH
5
1
Geological and Paleontological Department, Natural History Museum, Burgring 7, 1010 Vienna, Austria; *alexander.lukeneder@nhm-wien.ac.at
2
Department of Geology and Paleontology, Faculty of Natural Sciences, Comenius University, Mlynská dolina G-1, 842 15 Bratislava,
Slovak Republic; halasova@fns.uniba.sk; rehakova@fns.uniba.sk
3
Institute of Geology, Academy of Sciences of the Czech Republic, v.v.i., Rozvojová 269, 165 00 Praha 6, Lysolaje, Czech Republic
4
Institute for Marine and Coastal Environment (IAMC-CNR), Calata Porta di Massa (Interno Porto di Napoli), 80133 Napoli, Italy
5
Department for Geodynamics and Sedimentology, Center for Earth Sciences, University of Vienna, Althanstrasse 14, 1090 Vienna, Austria
(Manuscript received February 8, 2010; accepted in revised form June 10, 2010)
Abstract: The key objective of investigation of hemipelagic sediments from the Gresten Klippenbelt (Blassenstein For-
mation, Ultrahelvetic paleogeographic realm) was to shed light on environmental changes around the Jurassic-Cretaceous
(J/K) boundary on the northern margin of the Penninic Ocean. This boundary is well exposed in a newly discovered site at
Nutzhof. Around the critical interval including the boundary, this new outcrop bears a rich microplanktonic assemblage
characterized by typical J/K (Tithonian/Berriasian) boundary faunas. The Nutzhof section is located in the Gresten Klippenbelt
(Lower Austria) tectonically wedged into the deep-water sediments of the Rhenodanubian Flysch Zone. In Late Jurassic—
Early Cretaceous time the Penninic Ocean was a side tract of the proto-North Atlantic Oceanic System, intercalated be-
tween the European and the Austroalpine plates. Its opening started during the Early Jurassic, induced by sea floor spread-
ing, followed by Jurassic—Early Cretaceous deepening of the depositional area of the Gresten Klippenbelt. These tectonically
induced paleogeographic changes are mirrored in the lithology and microfauna that record a deepening of the depositional
environment from Tithonian to Berriasian sediments of the Blassenstein Formation at Nutzhof. The main lithological
change is observed in the Upper Tithonian Crassicollaria Zone, in Chron M20N, whereas the J/K boundary can be pre-
cisely fixed at the Crassicollaria—Calpionella boundary, within Chron M19n.2n. The lithological turnover of the deposi-
tion from more siliciclastic pelagic marl-limestone cycles into deep-water pelagic limestones is correlated with the deep-
ening of the southern edge of the European continent at this time. Within the Gresten Klippenbelt Unit, this transition is
reflected by the lithostratigraphic boundary between siliciclastic-bearing marl-limestone sedimentation in the uppermost
Jurassic and lowermost Cretaceous limestone formation, both within the Blassenstein Formation. The cephalopod fauna
(ammonites, belemnites, aptychi) and crinoids from the Blassenstein Formation, correlated with calcareous microfossil
and nannofossil data combined with isotope and paleomagnetic data, indicate the Tithonian to middle Berriasian
(Hybonoticeras hybonotum Zone up to the Subthurmannia occitanica Zone; M17r—M21r). The succession of the Nutzhof
section thus represents deposition of a duration of approximately 7 Myr (ca. 150—143 Ma). The deposition of the lime-
stone, marly limestone and marls in this interval occurred during tectonically unstable conditions reflected by common
allodapic material. Along with the integrated biostratigraphic, geochemical and isotopic analysis, the susceptibility and
gamma-ray measurements were powerful stratigraphic tools and important for the interpretation of the paleogeographic
setting. Two reverse magneto-subzones, Kysuca and Brodno, were detected within magnetozones M20n and M19n, re-
spectively.
Key words: Jurassic/Cretaceous boundary, Penninic Ocean, paleoecology, paleogeography, environmental changes.
Introduction
Jurassic and Lower Cretaceous pelagic sediments are known
to form a major elements of the northernmost tectonic units
of the Gresten Klippenbelt (Cžjžek 1852; Kühn 1962;
Küpper 1962; Gottschling 1965; Decker & Rögl 1988;
Decker 1990; Piller et al. 2004). Preliminary results on a
Jurassic-Cretaceous boundary section of the Gresten Klip-
penbelt were presented including description of new faunas
and localities (Lukeneder 2009; Kroh & Lukeneder 2009;
Pruner et al. 2009; Reháková et al. 2009).
The Gresten Klippenbelt at Nutzhof comprises Upper Ju-
rassic (Tithonian) to Lower Cretaceous sediments belonging
to the Blassenstein Formation. The lower part of the succes-
sion consists of marls, marly limestone and marl-limestone
alternations, whereas the upper part of the Blassenstein For-
mation (Tithonian to Valanginian) is composed of very pure
limestones. The biostratigraphy of the Lower Cretaceous
sediments in the study area is mainly based on microfossils
(Reháková et al. 2009). The first description of the lithology
and stratigraphy of this area was provided by Cžjžek (1852),
followed by Küpper (1962). Biostratigraphic data on the
Blassenstein Formation (Stollberger Schichten of Küpper
1962) near Nutzhof are remarkably scarce (Cžjžek 1852;
Küpper 1962).
The tectonically highly active northern zone of the Penninic
Ocean (the southern margin of the European continent) is
crucial for understanding the formation of the Penninic
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LUKENEDER, HALÁSOVÁ, KROH, MAYRHOFER, PRUNER, REHÁKOVÁ, SCHNABL, SPROVIERI and WAGREICH
Ocean, its subsequent subduction and the following Alpine
history.
Formation of the Penninic Ocean, here defined to include
the Ligurian Basin (sensu Dercourt et al. 1993, 2000; Masse
et al. 2000; Mandic & Lukeneder 2008) and synonymous
with the Alpine Tethys (Stampfli & Borel 2002 and Stampfli
et al. 2002) was initiated in the Late Triassic by rifting and
disjunction of the Austroalpine microcontinent from the
southern European Plate margin (Stampfli & Mosar 1999;
Scotese 2001). It formed an eastern prolongation of the
North Atlantic Rift-System, which affected the final break-
up of the Permo-Triassic supercontinent Pangaea (e.g. Faupl
2003). The formation of the oceanic crust and the sea-floor
spreading lasted from the Middle Jurassic to the Early Creta-
ceous, terminating with the introduction of its southward-di-
rected subduction beneath the northern Austroalpine plate
margin (Faupl & Wagreich 2000; Mandic & Lukeneder
2008). This tectonic phase is reflected by the lithological
change within the Nutzhof section. An increasing deepening,
reflected in the sedimentary succession (e.g. allodapic lime-
stones and microturbidites), in the section at Nutzhof, marks
the opening of the Penninic Ocean. The pelagic carbonate
sedimentation, which started in the Late Jurassic, changes
from siliciclastic-dominated limestone deposition to pure
limestone-dominated. The Penninic Ocean persisted from
the Late Jurassic until close to the end of the Cretaceous.
The paleomagnetic and rock-magnetic study is a continua-
tion of detailed paleontological and magnetostratigraphic
studies of the Jurassic/Cretaceous (J/K) boundary in the
Tethyan Realm (Houša et al. 1999). The section at Brodno
near Žilina, W Slovakia, was the first section investigated
with high-resolution magnetostratigraphy and micropaleon-
tology in the Carpathians (Houša et al. 1999). Magnetostrati-
graphic studies were carried out in the Bosso Valley of
Umbria, Italy (Houša et al. 2004) and the Tatra Mountains,
Poland (Grabowski & Pszczółkowski 2006). The magneto-
stratigraphic investigations published by Pruner et al. (2009)
preliminarily determine the boundaries of magnetozones
M17n to M22r (six reverse and six normal zones). The aim
of these studies was to globally and objectively establish a
correlation between biozones around the J/K boundary in the
Tethyan Realm using global paleomagnetic events and pre-
cisely determine the boundaries of magnetozones M19 and
M20 including narrow reverse subzones. These studies pro-
vided a precise record of polarity changes in the Earth’s
magnetic field and determined their stratigraphic positions
precisely within a biochronostratigraphic zonation.
The Nutzhof locality represents the only known section that
includes the J/K boundary interval in the Gresten Klippenbelt.
The section contains rich assemblages of radiolarians,
calpionellids, saccocomids, nannofossils and in some inter-
vals ammonites. The J/K boundary sediments of the Nutzhof
section provide an excellent succession for quantitative and
integrated methods due to their fossiliferous and undisturbed
bedding for a period of almost 7 million years.
Location and geological setting of Nutzhof
Locality description
The Nutzhof locality is situated in the Gresten Klippenbelt
of Lower Austria (48°04
’49” N, 15°47’36” E), about 20 km
south of Böheimkirchen and 5 km north of Hainfeld (Fig. 1),
600 m above sea level (m a.s.l.) (ÖK 1 : 50,000, sheet 56 St.
Pölten). The outcrop is located in an abandoned quarry in the
south-eastern-most part of the northeast-southwest striking
Gresten Klippenbelt, between Kasberg (785 m a.s.l.) to the
east and the vicinity of the Nutzhof (550 m a.s.l.) to the west.
The quarry is located on the northern side of the Kasberg
ridge and the measured section is exposed on the eastern side
of the quarry.
Geological setting
The Gresten Klippenbelt at Nutzhof is surrounded by
deep-water successions of the Rhenodanubian Flysch Zone.
The Gresten Klippenbelt represents an independent and
scarcely known geological unit. It is tectonically incorporat-
ed in the Flysch Zone as a long, thin, east-west striking marly
and calcareous unit (Fig. 1). Sediments from the Gresten
Klippenbelt are considered to belong to the southern part of
the Helvetic paleogeographic realm. The Gresten Klippen-
belt sediments were deposited on the southern shelf and
Fig. 1. Locality map of Austria with indicated position of the Nutzhof locality in Lower Austria (left). Detailed map of the area around
Nutzhof with outcrop position within the Jurassic—Cretaceous Klippenbelt (right).
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STRATIGRAPHY OF THE JURASSIC-CRETACEOUS GRESTEN KLIPPENBELT (AUSTRIA)
slope of the European continent, on the slope of the Bohemian
Massif at the north-western margin of the Penninic Ocean.
The Nutzhof site consists of two different facies within the
Blassenstein Formation (Lukeneder 2009). The lower part
(Tithonian; 18.0—10.0 m) with dark marl-limestone alterna-
tions and its characteristically intercalated limestone beds, and
the upper part (Tithonian—Berriasian; 10.0—0.0 m) with light
grey, almost pure limestone. Limestone beds display uniform
overturned bedding-plane orientation. The mean strike is
151°± 30° and the mean dip angle 44° ± 22°. The succession is
characterized by a marked lithological and faunal change at
Nu 10.0 which does not coincide with the Jurassic/Cretaceous
boundary at bed Nu 7.0 (Nu for Nutzhof samples). Sediments
occur as wacke-, pack- or mudstones.
The Nutzhof section
The Jurassic-Cretaceous boundary in the Gresten Klippen-
belt
The most recent reports concerning the J/K boundary in-
terval from the Gresten Klippenbelt present preliminary re-
sults (Lukeneder 2009; Kroh & Lukeneder 2009; Pruner &
al. 2009; Reháková et al. 2009) (Fig. 2). Therein first results
have been presented on macro-, micro- and nannofossils.
Tectonic units including the J/K boundary of the Gresten
Klippenbelt were reported by Cžjžek (1852), Kühn (1962),
Küpper (1962), Gottschling (1965), Decker & Rögl (1988),
Decker (1990) and Piller et al. (2004).
Materials and methods
The Jurassic-Cretaceous boundary section at Nutzhof was
studied with an integrated approach. Beds were sampled for
biostratigraphical, paleomagnetic, geochemical (CaCO
3
,
TOC, S) and istotopic (
18
O,
13
C,
87
Sr) data. Focus is di-
rected to an interval of about 18.0 m (Nu 0.0—Nu 18.0) that
was studied in detail (Figs. 2, 3, 4). Macro-, micro- and nanno-
fossil contents were quantitatively investigated (Fig. 4).
Samples were collected at intervals of 0.1 and 0.2 meters for
stable isotopes, total organic carbon (TOC), sulphur (S), cal-
cium carbonate (CaCO
3
), susceptibility and gamma log. The
microfossil content was analysed for calpionellids, radiolari-
ans, saccocomids (thin sections) and insoluble residues.
High resolution studies were combined with grey-scale
quantification, gamma-ray and susceptibility analyses. Sam-
ple numbers, for example Nu 10.0, correspond to the sample
interval at 10.0 m within the log (for all numbers and figures,
Nu = Nutzhof). All samples are stored at the Natural History
Museum of Vienna, in the collection of the Department of
Geology and Paleontology.
Gamma-ray analysis
The gamma log measures the radioactivity of the rock,
which represents a direct function of its clay-mineral content.
Increasing radioactivity reflects the increasing clay content.
Gamma response (counts per second – cps) was measured
using a hand-held standard gamma-ray scintillometer.
Macrofossils
Macrofossil material includes 46 ammonite specimens, 238
lamellaptychi and 82 rhyncholites were examined. Four
brachiopods and three inoceramids as well as a single
belemnite specimen were collected. Ammonites are preserved
as steinkerns or are represented by calcitic aptychi. Shell-
preservation is restricted to organisms with primary skeletal
calcite of belemnite-rostra and brachiopods in addition to rare
inoceramid fragments (calcitic prisms). The ammonite
assemblage contains six different genera: Subplanites,
Haploceras, Phylloceras, Ptychophylloceras, Lytoceras and
Leptotetragonites dominated by the perisphinctid genus
Subplanites (Lukeneder 2009).
Calpionellids and calcareous nannofossils
Quantitative micro- and nannofacies analysis includes study
of calpionellids and calcareous dinoflagellates in 93 thin sec-
tions. The thin sections are deposited in the Natural History
Museum in Vienna; NHMW 2007z0271/0000. Changes in the
distribution of calpionellids and calcareous nannofossils were
studied in detail in order to correlate them with the changes in
nannoplankton associations (Figs. 2, 3 and 4).
Calcareous nannofossils were analysed semiquantitatively
in 19 smear slides, prepared from all lithologies by standard
techniques, using a light polarizing microscope at 1250
magnification. At least 200 specimens were counted in each
slide to record relative abundances and the stratigraphic range
of taxa (Figs. 2, 3). Nannofossil preservation can be character-
ized as moderately to intensely etched by dissolution. The cal-
careous nannofossil zones were adopted from the zonal
scheme proposed by Bralower et al. (1989).
Magnetic components
Paleomagnetic analyses presented in this studies come
from 244 samples, but the preliminary results include only
111 samples (see Pruner et al. 2009). All the samples were
subjected to progressive thermal demagnetization (TD) or
alternating field (AF) demagnetization in 11—12 temperatures
or fields. The individual components were precisely established
using multicomponent analysis of remanence (Kirschvink
1980). Isothermal remanent magnetization (IRM) to satura-
tion was measured to identify magnetically active minerals.
Magnetomineralogical analyses and unblocking temperature
determination show that magnetite and goethite are the main
carriers of remanent magnetization.
Microfossils
Apart from thin sectioning also employed for a study of
calpionellids, an effort was made to obtain three-dimension-
al specimens of the crinoids and other microfossils common-
ly observed in the thin sections (namely foraminifers,
ostracods, rhyncholites, small aptychi, ophiuroid remains,
368
LUKENEDER, HALÁSOVÁ, KROH, MAYRHOFER, PRUNER, REHÁKOVÁ, SCHNABL, SPROVIERI and WAGREICH
Fig. 2. Nutzhof log with occurrence and range of calcareous nannofossils, calcareous dinoflagellates and calpionellids and indicated paleo-
magnetic zonation: normal magnetozones are denoted black, reverse zones in white, and unknown parts in grey.
369
STRATIGRAPHY OF THE JURASSIC-CRETACEOUS GRESTEN KLIPPENBELT (AUSTRIA)
etc.). Bulk samples were collected in closely spaced intervals
in the lower, marly part of the succession (10.0—18.0 m).
Strong lithification hampered dense bulk sampling in the up-
per part of the section (0 to 10.0 m). These beds were analysed
by thin sections only. Traditional washing methods were not
applicable due to strong lithification of the sediment. Partial
disaggregation was achieved by repetitive, combined treat-
ment with hydrogen-superoxide and the tenside Rewoquat
(see Lierl 1992). After cleaning, the microfossils were hand
picked under a microscope. For the present study we used
the sediment fractions larger than 250 µm only.
TC and TOC content
Calcium carbonate contents (CaCO
3
; wt. % bulk rock, TC)
were determined using the carbonate bomb technique. Total
carbon content was determined using a LECO WR-12 analy-
ser. Total organic carbon (TOC) contents were calculated as
the difference between total carbon and carbonate carbon,
assuming that all carbonate is pure calcite. All the chemical
analyses were carried out in the laboratories of the Depart-
ment of Forest Ecology at the University of Vienna.
Stable isotopes
A total of 37 bulk sample stable isotope analyses were
measured by automated continuous flow carbonate prepara-
tion GasBenchII device (Spötl & Vennemann 2003) and
ThermoElectron Delta Plus XP mass spectrometer at the
IAMC-CNR (Naples) isotope geochemistry laboratory.
Acidification of samples was performed at 50 °C. For each
six samples, an internal standard (Carrara Marble with
18
O= —2.43 vs. V-PDB and
13
C= 2.43 vs. V-PDB) was run,
and for each 30 samples, the NBS19 international standard
was measured. Standard deviations of carbon and oxygen
isotope measures were estimated 0.1 and 0.08 ‰, respective-
ly, on the basis of ~ 10 repeated samples.
All the isotope data are reported in per mil (‰) relative to
the V-PDB standard.
87
Sr/
86
Sr isotope data were analysed from 19 bulk-rock
samples of limestones at the Geochronological Laboratory of
the Department of Lithospheric Research, Centre for Earth
Sciences, University of Vienna using strontium separation
by standard methods of ion-exchange chromatography and
isotope ratio measurements on a TIMS (Triton mass spec-
trometer). The measured NBS 987 standard value during
measurements was 0.710256 + /—0.000004 (7 measurements)
and samples were not adjusted to the NBS 987 standard
value of 0.710248.
Data and results
Biostratigraphy and magnetostratigraphy
The stratigraphic investigation of the calcareous microfos-
sils (calpionellids, calcareous dinoflagellates) and nannofos-
sils demonstrate that the Nutzhof section represent the Lower
Tithonian—middle Berriasian. The calcareous dinoflagellate
cyst zonation of Reháková (2000a) was followed. The pres-
ence of the Lower Tithonian Tithonica, Malmica and Semira-
diata cyst Zones is demonstrated. The standard calpionellid
zones and subzones proposed by Reháková (1995) and Rehá-
ková & Michalík (1997) were adopted for the biostratigraphic
subdivision of the section into the Chitinoidella Zone (Boneti
Subzone), the Praetintinnopsella Zone and the Crassicollaria
Zone (Remanei Subzone). These belong to the middle to
Upper Tithonian. The standard Calpionella Zone (Alpina,
Ferasini and Elliptica Subzones) were observed in the overly-
ing Lower Cretaceous (Fig. 2).
The nannofossil zones include the Conusphaera mexicana
mexicana Zone, Microstaurus chiastus and Nannoconus
steinmannii steinmannii Zones. This stratigraphic interval cor-
responds to the Lower Tithonian Hybonoticeras hybonotum
ammonite Zone to the middle Berriasian Subthurmannia
occitanica ammonite Zone, demonstrated in the Nutzhof
section on chronostratigraphic diagnostic cephalopods (Sub-
planites fasciculatiformis, Ptychophylloceras ptychoicum,
Leptotetragonites honnoratianus, Haploceras elimatum,
Hibolithes (gr.) semisulcatus and some lamellaptychi.
The magnetostratigraphic log across the Nutzhof section
includes the M21r to the M17r magnetozones subdivided
into the Kysuca (M20r) and Brodno (M19r) subzones
(Figs. 2, 6). The average sedimentation rate in the Nutzhof
section is ca. 3.7 m/Myr (Fig. 7), but with high dispersion
(from 2—11 m/Myr). The scatter of the sedimentation rate is
similar to Hlboča profile in Slovakia (Grabowski et al.
2010). The main difference between these two sections is in
the thickness of M19 and M20 mangentozones. Nutzhof has
higher sedimentation rate at M19 while Hlboča appears with
higher rates in M20.
Macrofossil content
The macrofossil content is characterized by ammonoids,
aptychi, belemnites, brachiopods, bivalves and echinoderms.
The ammonite fauna comprises six different genera repre-
sented by Lytoceras sutile Oppel, Lytoceras sp., Leptotetra-
gonites honnoratianus (d’Orbigny), Phylloceras sp.,
Ptychophylloceras ptychoicum (Quenstedt), Haploceras
(Haploceras) elimatum (Oppel), Subplanites fasciculatiformis
Lukeneder. The ammonite fauna is dominated by the
perisphinctid-type. Ammonitina is the most common com-
ponent (60 %; Subplanites and Haploceras), followed by the
Phylloceratina (25 %; Ptychophylloceras and Phylloceras),
and the Lytoceratina (15 %; represented by Lytoceras and
Leptotetragonites). The belemnite Hibolithes (gr.) semisul-
catus (Münster) and aptychi (Lamellaptychus) occur. Only
Mediterranean cephalopod elements are present at Nutzhof.
Brachiopods are represented by Triangope, bivalves by inoc-
eramid shells and echinoderms by crinoids (Phyllocrinus
belbekensis Arendt, Balanocrinus sp., Crassicoma? sp. and
Saccocoma tenella (Goldfuss).
The crinoid fauna recovered from the bulk samples of
Nutzhof is typical for Upper Jurassic strata of Central and
Eastern Europe. The low diversity of stalked crinoids, com-
mon in many contemporaneous deposits (Hess et al. 1999),
may be interpreted as a result of the distal position of the sec-
370
LUKENEDER, HALÁSOVÁ, KROH, MAYRHOFER, PRUNER, REHÁKOVÁ, SCHNABL, SPROVIERI and WAGREICH
Fig. 3. Compiled geochemical, isotope and fossil data on the J/K boundary at Nutzhof. Note the change at the predating interval at meter 7
below the J/K boundary.
371
STRATIGRAPHY OF THE JURASSIC-CRETACEOUS GRESTEN KLIPPENBELT (AUSTRIA)
tion, which represents a deep-water facies. The incomplete
size ranges of isocrinid and phyllocrinid ossicles, the lack of
fragile elements and the presence of allodapic material
(Lukeneder 2009) suggest that the majority of the crinoid ma-
terial is allochthonously deposited. Saccocomid fragments, in
contrast, are not sorted and include abundant fragile elements
suggesting that these crinoids are autochthonous.
Of the crinoid material only the saccocomids can be used
for biostratigraphy. Saccocoma tenella is restricted to the
Upper Kimmeridgian—Upper Tithonian. From a biogeo-
graphic point of view the faunal composition indicates con-
nections with contemporaneous units of the northern Tethys
shelf in Eastern Europe.
Microfacies and calcareous microplankton assemblages
The limestones in the section include wackestones, pack-
stones and mudstones. Fine-grained micrite with pelagic
microfossils (calpionellids, calcareous dinoflagellates, radio-
larians) and calcareous nannofossils characterize an open-ma-
rine environments. Rare skeletal debris from fragmented and
disintegrated shells of invertebrates (benthic foraminifers,
echinoderms, molluscs) are derived from shallower environ-
ments. The studied microfacies are typical for basinal settings.
Calpionellids
Calpionellids in the studied samples are generally well-
preserved. Hyaline forms dominate, whereas chitinoidellids
are rare. The chitinoidellid taxonomy of Pop (1997) and
Reháková (2002) is followed here. The group is represented
by Borziella slovenica (Borza), Dobeniella tithonica (Borza)
and Chitinoidella boneti Doben, species typical for the
Boneti Subzone of the Chitinoidella Zone (Figs. 2, 4). The
appearance of first hyaline calpionellid loricas of Praetintin-
nopsella andrusovi Borza and Tintinnopsella remanei Borza
Fig. 4. A – Conusphaera mexicana minor Bown & Cooper; Nu 18.0, NHMW2008z0271/0028. B – Conusphaera mexicana mexicana Bra-
lower et al.; Nu 17.0, NHMW2008z0271/0003. C – Cadosina semiradiata semiradiata Wanner; 17.0, NHMW2008z0271/0003. D – Paras-
tomiosphaera malmica (Borza); Nu 13.0, NHMW2008z0271/0002. E – Calpionella alpina Lorenz and Calpionella grandalpina Nagy;
Nu 9.8, NHMW2008z0271/0011. F – Crassicollaria parvula Remane and Calpionella grandalpina; Nu 9.6, NHMW2008z0271/0012.
G – Calpionella elliptica Cadisch; Nu 3.2, NHMW2008z0271/0014. H – Nannoconus steinmannii steinmannii Kamptner; Nu 4.0,
NHMW2008z0271/0034. I – Nannoconus kamptneri kamptneri Brönnimann; Nu 2.0, NHMW2008z0271/0035. J – Phyllocrinus belbek-
ensis Arendt; Nu 12.3; NHMW 2008z0226/001. K – Balanocrinus sp.; Nu 14.6, NHMW2008z0228/0003. L – Saccocoma tenella (Gold-
fuss); Nu 11.5, NHMW2008z0236/0015. M – Saccocoma tenella (Goldfuss); Nu 13.0, NHMW2008z0236/0012. N – Hibolithes (gr.)
semisulcatus (Münster); Nu 14.3, NHMW2008z0264/0025. O – Subplanites fasciculatiformis Lukeneder; Nu 17.0, NHMW2008z0264/0012.
P – Triangope sp.; Nu 1.0, NHMW2008z0264/0028. Q – Lamellaptychus sp.; Nu 18.0, NHMW2008z0264/0024. Graphic scale bars
equal 1 m for A, B and H, I; 50 m for C—G; 1 mm for J—K, and 10 mm for N—Q.
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LUKENEDER, HALÁSOVÁ, KROH, MAYRHOFER, PRUNER, REHÁKOVÁ, SCHNABL, SPROVIERI and WAGREICH
precede the crassicollarian radiation. Crassicollaria parvula
Remane and Calpionella alpina Lorenz dominate relative to
Crassicollaria massutiniana (Colom), Calpionella grandalpina
Nagy and Tintinnopsella carpathica (Murgeanu & Filipescu)
in the Remanei Subzone of the Crassicollaria Zone. Higher
in the section, crassicollarians abruptly decrease in abun-
dance, being replaced by an interval with radiation of small
spherical forms of Calpionella alpina Lorenz. The diversifi-
cation of a monospecific calpionellid association started in
the overlying Ferasini and Elliptica Subzones of the stan-
dard Calpionella Zone where Calpionella alpina Lorenz is
accompanied by Tintinnopsella carpathica (Murgeanu &
Filipescu), Remaniella ferasini Pop, R. duranddelgai Pop,
R. catalanoi Pop, Calpionella elliptica (Cadisch), Tintinnop-
sella longa (Colom), and Lorenziella hungarica Knauer.
Calcareous dinoflagellates
Calcareous dinoflagellates predominate in the Lower and
Upper Tithonian being represented by Cadosina parvula
Nagy, Carpistomiosphaera borzai (Nagy), Schizosphaerella
minutissima (Colom), Parastomiosphaera malmica (Borza),
Cadosina semiradiata semiradiata Wanner, Cadosina semi-
radiata fusca (Wanner), Carpistomiosphaera tithonica
Nowak, Colomisphaera fortis Řehánek, Colomisphaera
tenuis (Nagy), Colomisphaera carpathica (Borza), and
Stomiosphaerina proxima Řehánek. For the first time the ap-
pearance of Colomisphaera fortis Řehánek precedes the ap-
pearance of Colomisphaera tenuis (Nagy), hampering the
determination of the Tenuis and Fortis dinoflagellate Zones
sensu Řehánek (1992) (Figs. 2, 4).
Calcareous nannofossils
The semiquantitative study (Figs. 2, 3) reveals that only the
taxa Conusphaera spp., Polycostella spp., Nannoconus spp.,
Cyclagelosphaera margerelii Noël, Watznaueria barnesae
(Black) Perch-Nielsen, and W. manivitae Bukry occur in sig-
nificant abundances. Nannofossils indicative of eutrophic
environments such as Zeugrhabdotus erectus (Deflandre) Re-
inhardt, Diazomatholithus lehmannii Noël, and Discorhabdus
ignotus (Górka) Perch-Nielsen occur sporadically.
The calcareous nannofossil assemblage from the basal part
of the Nutzhof section (samples 17, 18, Tithonica dinoflagel-
late Zone) contains the dissolution-resistant nannofossil spe-
cies Conusphaera mexicana mexicana Bralower et al.,
Conusphaera mexicana minor Bown & Cooper, Cyclagelo-
sphaera margerelii, Cyclagelosphaera deflandrei (Manivit)
Roth, Watznaueria barnesae, Watznaueria britannica
(Stradner) Reinhardt, and Watznaueria manivitae. The FO
(first occurrence datum) of Faviconus multicolumnatus
Bralower was recorded. The absence of the nannolith Poly-
costella beckmannii Thierstein allowed us to distinguish the
Conusphaera mexicana mexicana NJ20 Zone; Hexapodor-
habdus cuvillieri Subzone NJ20-A (Roth et al. 1983; emend-
ed Bralower et al. 1989) of the Lower Tithonian.
The calcareous nannofossil assemblages from the samples
Nu 16.0 to Nu 12.0 show dominance of Watznaueria and
Conusphaera. The FOs of Zeugrhabdotus embergeri (Noël)
Perch-Nielsen, Zeugrhabdotus erectus, and Diazomatho-
lithus lehmannii were observed. The FO of the nannolith
Polycostella beckmannii is the most significant marker indi-
cating the base of the Polycostella beckmannii Subzone
NJ20-B of the Conusphaera mexicana mexicana Zone, NJ20
(Roth et al. 1983; emended Bralower et al. 1989). The age of
this Subzone is middle Tithonian. The range of the Poly-
costella beckmannii Subzone NJ20-B fits with dinoflagellate
Malmica and Semiradiata Zones and the lower part of the
Chitinoidella Zone.
The calcareous nannofossils investigated in sample Nu 11
reflect a rather distinct change. The FO of Helenea chiastia
Worsley, Hexalithus noeliae Loeblich & Tappan and the
nannolith species Nannoconus compressus Bralower et al.
are evidence for the base of the Microstaurus chiastius Zone
NJK Bralower et al., 1989 and its Hexalithus noeliae Sub-
zone NJK-A, which is thought to represent the Late Titho-
nian interval. The Subzone coincides with the upper part of
the Chitinoidella Zone.
The calcareous nannofossil assemblages from samples
Nu 9.0 to Nu 6.0 contain dissolution-resistant nannofossil
genera
Conusphaera,
Cyclagelosphaera,
Watznaueria,
Diazomatholithus and Assipetra. The FAD of Nannoconus
wintereri Bralower & Thierstein (1989) was observed (sam-
ple 9.0). Many remains of dissolution-susceptible coccoliths
are present. In the upper part of the studied interval, the abun-
dance of Conusphaera drops. This interval was correlated
with the Microstaurus chiastius Zone NJK, Subzone Rote-
lapillus laffitei NJK-C, determining the J/K boundary interval.
It shows good correlation with the upper part of the Upper Ti-
thonian Crassicollaria Zone and the Calpionella Zone (Alpina
Subzone), which represent the J/K boundary interval.
The interval bearing the calpionellid species of the Lower
Berriasian Calpionella Zone (Ferasini Subzone) (sample
Nu 5.0) shows a distinctive change in the calcareous nanno-
fossil assemblage – the onset of nannoconids (Nannoconus
globulus minor Bralower, Nannoconus steinmannii minor
Deres & Achéritéquy, Nannoconus kamptneri minor Bralower,
Nannoconus cornuta Deres & Achéritéquy). This nannofossil
event indicates the base of the Nannoconus steinmannii minor
Subzone NJK-D (Microstaurus chiastius Zone NJK) Bralower
et al., which belongs to the lowermost Berriasian.
The calcareous nannofossils studied from the sample inter-
val Nu 4.0—Nu 0.0 (correlating with the calpionellid
Calpionella Zone, Elliptica Subzone) record the diversifica-
tion of nannoconids. The FAD of Nannoconus steinmannii
steinmannii Kamptner is recorded at level Nu 2.0. It could re-
flect the explosion in nannoconid abundance (sensu Bralower
et al. 1989: p. 188). Nannoconus globulus minor, Nannoco-
nus kamptneri minor, Nannoconus wintereri, Nannoconus
globulus globulus Deres & Achéritéquy, Nannoconus
steinmannii minor Deres & Achéritéquy, Nannoconus stein-
mannii steinmannii, and Nannoconus kamptneri kamptneri
Brönnimann, Nannoconus spp. indicative of the Nannoconus
steinmannii steinmannii Zone NK-1, Bralower et al. (1989),
which is middle Berriasian in age.
On the basis of calcareous nannofossil distribution, the in-
terval between the FO of Nannoconus wintereri co-occurring
with small nannoconids in bed Nu 9.0 and the FO of Nanno-
373
STRATIGRAPHY OF THE JURASSIC-CRETACEOUS GRESTEN KLIPPENBELT (AUSTRIA)
conus steinmannii minor in bed Nu 5.0 (FAD after Hardenbol
et al. 1998 – 143.92 Ma) is interpreted as the Tithonian-
Berriasian boundary interval (Figs. 2, 3).
Stable isotope data
Oxygen and carbon (O, C)
The bulk carbon-isotope values (Fig. 3) lie between + 0.49
and + 2.10 ‰ corresponding to biogenic calcite precipitated
under open marine conditions during the Jurassic—Creta-
ceous (e.g. Weissert et al. 1985). All
18
O values are be-
tween —1.94 to —5.49 ‰ and appear depleted relative to
diagenetically unaltered marine calcite (e.g. van de Schoot-
brugge et al. 2000, and reference therein). This reflects ele-
vated temperature during burial diagenesis and/or effects of
meteoric diagenesis (Weissert 1989). The carbon isotope sig-
nal is considered of primary importance as a calibration tool
between ammonites and magnetostratigraphy (Hennig et al.
1999), but it should be noted that the absence of covariance
between
18
O and
13
C suggests a limited influence of sec-
ondary diagenesis on the isotope record (Fig. 3).
A positive trend in the
13
C, from the base of the section at
Nu 18.0 up to Nu 14.0, is followed by a decreasing excur-
sion shifting the isotope values to their lowest values
(0.69 ‰) at about Nu 10.0. After that point the
13
C values
stabilize at near constant averages of ~ 1.20 ‰.
Strontium (Sr)
87
Sr/
86
Sr isotope data from the section show a range from
0.707370 + /—0.000004 to 0.707598 + /—0.000004. A gentle
trend from lower values in the lower, Jurassic part of the sec-
tion (Nu 18.0—Nu 12.0: mean 0.707472) to higher values in
the upper part including the J/K boundary and the Creta-
ceous interval (Nu 11.0—Nu 0.0: mean 0.707553) can be rec-
ognized (Fig. 3). A special interval is represented in the
strong increase from Nu 13.0 (lowest isotope value) to
Nu 11.0 (highest isotope value) and probably indicate a local
diagenetic phenomenon. The slight increase of mean stron-
tium isotope ratios in the section is compatible with the gen-
eral increase of strontium isotope ratios from the latest
Jurassic into the earliest Cretaceous as reported by the stron-
tium isotope seawater curve of McArthur et al. (2001) and
McArthur & Howarth (2004). The values measured in the
present study are generally higher by a factor of ca. 0.0002
compared to the values reported by McArthur & Howarth
(2004), who measured Upper Tithonian values around
0.707150 and Berriasian values between 0.707200—0.70725
(see also McArthur et al. 2007) with the Berriasian/Valang-
inian boundary slightly above 0.707300. Thus, the lowest
measured value in the Nutzhof section thus does not fall
within the J/K boundary range of values recorded by
McArthur & Howarth (2004). This confirms a strong diage-
netic overprint upon strontium isotope values. However, the
increase in mean values is within the reported magnitude of
increase expected for the J/K boundary interval, thus being
compatible with the stratigraphy inferred by other methods,
but precluding detailed dating.
Geochemistry
The CaCO
3
(calcium carbonate contents, equivalents calcu-
lated from total inorganic carbon; carbonate bomb) differ
markedly in the lower and upper part of the log. The lower
part shows variations from 89.03 % (Nu 12.0) in limestone
beds to 40.72 % (Nu 13.4) in marl beds, whereas the upper
part displays more constant values ranging from 86.16 %
(Nu 9.6) up to the highest measured value of 97.4 % (Nu 3.6).
As recorded by the biostratigraphic results, the strong
lithological and faunal changes at Nu 12.00 and Nu 10.0 are
3 to 5 meters below the Jurassic/Cretaceous boundary (Bed
Nu 7.0) indicating changes in depositional environment 0.5
to 1 million years before the end of the Jurassic. The interval
from Nu 12.0—10.0 (CaCO
3
89.03—68.97 %; S 0.59—0.45 %;
TOC up to 0.97 %) differs markedly and heralds the environ-
mental change observed (Fig. 3).
Both the CaCO
3
and the S content clearly show a trend to-
wards higher values and stable conditions from bed
Nu 10.00 to Nu 18.00. Unstable conditions are mirrored in
alternating values in the lower part of the log by variations
from 89.03 % CaCO
3
and 0.59 % S (Nu 12.0) in limestone
beds to 40.72 % and 0.30 % (Nu 13.4) in marl beds.
The range is smaller and more constant in the interval
Nu 10.0—18.0 with CaCO
3
values from 86.16 % at Nu 9.6 up
to the maximum value of 97.4 % at Nu 3.6. The total sulphur
content is positively correlated to the CaCO
3
values. The
maximum value is at bed Nu 9.0 with 0.58 % S and its mini-
mum with 0.5 % S in bed Nu 0.0. As confirmed by Hirano
(1993) the sulphur content is a reliable index for oxic-anoxic
conditions of the bottom water and sediment at the time of
preservation.
The weight % TOC values show no positive correlation
with S or CaCO
3
. TOC values oscillate throughout the log.
They vary from 0.001 % to 0.91 % (Nu 11.2) in the lower
part and from 1.07 % (Nu 3.4) to 0.001 % in the upper part.
The above described geochemistry is also reflected in the
results of grey-scale data marking siliciclastic input. The sec-
tion can be subdivided into three parts: a lower part
(Nu 18.0—12.0) with 170—111 (mean 140.5), a middle part
(Nu 12.0—10.0) with 138—90 (mean 114) and an upper part
(Nu 10.0—0.0) with 254—195 (mean 224.5). In combination
with other analyses, the grey-scale factor is a good indicator
for siliciclastic input (clay, not sandstone) in pelagic to
hemipelagic sediments. This indicates the dominance of si-
liciclastic components and allodapic microturbidites within
the dark mid-part. These results corroborate those obtained
from susceptibility and gamma log (increasing values show
higher contents in clay minerals), thin sectioning and micro-
facies analysis.
Susceptibility
Susceptibility measurements at Nutzhof represent a direct
function of the clastic or turbiditic content and associated
mineral spectra (Fig. 3). Higher susceptibility data reflect
higher detritic input of terrigenous material. The paleomag-
netic data given in the magnetostratigraphic profile indicate
a significant jump of remanent magnetization and magnetic
374
LUKENEDER, HALÁSOVÁ, KROH, MAYRHOFER, PRUNER, REHÁKOVÁ, SCHNABL, SPROVIERI and WAGREICH
susceptibility, at Nu 10.0. This change marks the change
from marls and marly limestone to pure limestone. Magneto-
susceptibility measurements allow a subdivision of the
Nutzhof section into three parts or intervals. A general de-
creasing trend throughout the log reflects a decreasing con-
tent of siliciclastic material indicating a decrease in clastic
input to the depositional area at Nutzhof during the Late
Jurassic—Early Cretaceous. Mean values of volume magnetic
susceptibility (k) are shown in Table 1. The k ranges from
—8.6 to 15.6 10
—6
SI for upper interval between 0—10 m of
the section and from 30 to 85.1 10
—6
SI for the lower part
(10.12—18.4 m). The lower part from Nu 18.0—12.0 shows
values from 0.052—0.028 (mean 0.039). Above Nu 12.0 val-
ues range from 0.050—0.026 (mean 0.033). The most marked
change appears at Nu 10.0 from values of 0.050 to 0.010.
The upper interval from Nu 10.0 to 0.0 is characterized by
very low values from 0.012—0.000 (mean 0.004). The J/K
boundary strata itself are not characterized by significant
changes in values.
Gamma log
The radioactivity variation of the studied section is mea-
sured by gamma-ray measures and represents a direct func-
tion of the variation of the clay-mineral content. Hence,
higher radioactivity reflects higher clay contents. Measure-
ments of gamma response (cps) are a powerful tool for inter-
preting the stratigraphy in the outcrop.
Generally measured cps values range between 4 and 30. The
gamma response allows a clear subdivision of the section into
three parts each corresponding to the three identified main
lithological units within the Blassenstein Formation. The gam-
ma response gradually decreases from Nu 18.0 to Nu 0.0,
reaching the highest values at Nu 16.5 and lowest values at
Nu 7.7 and Nu 3.3. Within this gradually decreasing trend, the
biggest excursion is recorded close to bed Nu 10.0. Values
range in the lower interval (Nu 18.0—12.0) from 15—30 cps
(mean 22.53 cps), in the middle interval (Nu 12.0—10.0) from
13—23 cps (mean 19.95 cps), and in the upper interval
(Nu 10.0—0.0) from 4—14 cps (mean 9.07 cps) (Fig. 3).
The gamma response becomes gradually weaker in the up-
per, undisturbed part of the section. The uppermost part of
the section, however, shows an upwards decreasing gamma
response. The curve pattern therefore shows a vertically con-
gruent curve to the susceptibility values.
The decreasing gamma log values together with the charac-
teristic pattern in decreasing susceptibility suggest a more sta-
ble depositional environment from about Nu 10.0 and
upwards, predating the J/K boundary by 3 meters or 0.5 mil-
lion years.
Paleomagnetism
The paleomagnetic study of the section identifies the
boundaries of magnetozones from M17r to M21r and the re-
verse subzones Kysuca and Brodno (M20n.1r and M19n.1r,
respectively). The record of polarity changes in the Earth’s
magnetic field can determine the precise age. The identifica-
tion of the detected polarity zones against the M-sequence of
polarity intervals given by the GPTS (Gradstein et al. 2004)
is the most important topic. The preliminary determination
of boundaries of magnetozones M17n to M22r was the result
from 30 samples of C-component direction (Pruner et al.
2009). The number of polarity zones, namely six normal and
six reverse, is the same number as in preliminary results. The
mean values of the modulus of NRM (Jn) and of volume
magnetic susceptibility (k) for 244 samples of Upper Tithonian
and Lower Berriasian limestones are shown in Table 1. The k
ranges from —8.6 to 15.6 10
—6
SI for the upper interval be-
tween 0—10 m of the section and from 30 to 85.1 10
—6
SI for
the lower part (10.12—18.4 m). The results of AF and TD de-
magnetization procedures are displayed in Pruner et al.
(2009: figs. 3, 4). The A-component is of viscous origin and
is demagnetizable in the temperature range of 20—100 °C (or
AF 0—5 mT). The origin of the B-components, low tempera-
ture (LTC) or low field (LFC) were undoubtedly imprinted,
most probably in the Neogene, after Alpine folding. Both
magnetic polarities are present in C-component (high tem-
perature – HTC or high field – HFC) directions, but the di-
rections are highly scattered (Table 2, Fig. 5). The statistical
Fig. 5. J/K limestones and marls,
directions of N polarity (left) and
R polarity (right) of C-compo-
nents of RM corrected for dip of
strata. Stereographic projection,
full (open) small circles repre-
sent projection onto the lower
(upper) hemisphere. The mean
direction calculated according to
Fisher (1953) is marked by a
small crossed circle, the confi-
dence circle at the 95% probabil-
ity level is circumscribed about
the mean direction.
375
STRATIGRAPHY OF THE JURASSIC-CRETACEOUS GRESTEN KLIPPENBELT (AUSTRIA)
Fig. 6. Magnetostratigraphic profile across the Nutzhof J/K boundary strata, paleomagnetic and lithostratigraphic data. M – NRM in the
natural state; k – value of volume magnetic susceptibility in the natural state; D – declination; I – inclination. Normal (reverse) magne-
tozones are denoted black (white), unknown (grey).
376
LUKENEDER, HALÁSOVÁ, KROH, MAYRHOFER, PRUNER, REHÁKOVÁ, SCHNABL, SPROVIERI and WAGREICH
parameters for component C (total number 220) are influ-
enced by samples close to the boundary of shorter polarity
zones. The mean values of C-component directions are
anomalous, having been affected by counter clockwise paleo-
tectonic rotation. The paleomagnetic data given in the
magnetostratigraphic profile (Fig. 6) indicate a significant
change of remanent magnetization and magnetic susceptibility,
at level Nu 10 due to the significant change in lithology from
marl (Nu 18.0—10.0) to limestone (Nu 10.0—0.0).
Figure 5 presents the results of the magnetostratigraphic
profile with indicated moduli values of natural remanent mag-
netization (Jn), volume magnetic susceptibility values of sam-
ples in the natural state (k), paleomagnetic declination Dp and
inclination Ip (of C-components of remanence inferred by
multi-component analysis). The values of the angular deflec-
tion of the direction of C-components of remanence from the
mean direction, with only normal polarity being taken into
consideration (reverse directions were transformed into nor-
mal directions for the calculation of the mean direction), are
given in the next column. The resulting normal and reverse
magnetozones are indicated in the last column.
Discussion
The high-resolution quantitative analysis of selected organic
groups (calpionellids, radiolarians, saccocomids) indicates
major variations in their abundance and composition (Figs. 2,
3, 4). The Upper Jurassic (Tithonian) depositional setting at
Nutzhof was influenced by the periodic input of biodetritus
from surrounding shallow marine paleoenvironments, whereas
deposition was more constant during the Berriasian and
characterized by pelagic sediments predominantly composed
of planktonic microorganisms (radiolarians, calcareous dino-
flagellates, calpionellids, and nannofossils).
Calcareous dinoflagellates predominate in the Lower and
Upper Tithonian. Their stratigraphic and paleoecological po-
tential has been discussed by Reháková (2000a,b). In the
Nutzhof section, the Lower Tithonian record of calcareous di-
noflagellates shows a distinct change in abundance and com-
position. Forms with radial orientation of calcite crystallites in
their cyst walls dominate in the Tithonica and Malmica Zones,
whereas cadosinid species with oblique arrangement of the
calcite crystallites dominate the Semiradiata Zone. According
to Michalík et al. (2009), coinciding acme peaks of Cadosina
semiradiata semiradiata Wanner and Conusphaera spp. prob-
ably indicate warmer surface waters.
Chitinoidellids are very rare in the Nutzhof section. The
appearance of the first hyaline calpionellid loricas precedes
the crassicollarian radiation. A monospecific calpionellid as-
sociation consisting predominantly of Calpionella alpina
Lorenz characterizes the section. A similar calpionellid evo-
lution and biostratigraphy of the Jurassic-Cretaceous bound-
ary interval was recorded by Remane (1986), Pop (1994),
Reháková (1995), Olóriz et al. (1995), Grün & Blau (1997),
and Andreini et al. (2007). Reháková (in Michalík et al.
2009) demonstrated that the J/K boundary interval can be
characterized by several calpionellid events: the onset, diver-
sification, and extinction of chitinoidellids (middle Titho-
nian); the onset, diversification, and extinction of
crassicollarians (Upper Tithonian); and the onset of the
monospecific Calpionella alpina association at the J/K
boundary. Due to synsedimentary erosion probably originat-
ing during several extensional pulses, which denivelated the
sea bottom, clast-bearing calpionellid biomicrites were doc-
umented along the Upper Jurassic and Lower Cretaceous
(Lower Berriasian) formations in several areas studied
(Michalík et al. 1990, 1995; Grabowski et al. 2010).
The calcareous nannofossil ranges in the Nutzhof section
provides a tool for biostratigraphic subdivision of the J/K
boundary interval. The coccoliths of the family Watznaueri-
aceae and three nannolithic genera Conusphaera, Polycostel-
la, and Nannoconus dominate the assemblages. This is in
accordance with nannofossil studies in other locations at low
latitudes sections across the J/K boundary (Thierstein 1971,
1973, 1975; Erba 1989; Gardin & Manivit 1993; Özkan 1993;
Table 1: Basic magnetic parameters and statistical properties of the physical quantities in the basic groups of samples from the Nutzhof.
Modulus of NRM
J
n
[10
–6
A/m]
Volume magnetic susceptibility
k [10
–6
SI]
Age
Polarity
Number of samples
Mean value
Standard deviation
Mean value
Standard deviation
Early Berriasian
N+R
82
88
39
2.3
3.1
Late Tithonian
N+R
155
165
132
21.4
26.5
Table 2: Mean directions of B (LFC or LTD) and C-components (HFC or HTD) corrected and not corrected for structural tilt.
Structural tilt correction
No structural tilt correction
(in-situ directions)
Mean directions
Mean directions
Age of rocks
C
omp
on
en
t of
rem
an
en
ce
Po
la
ri
ty
Decl. [
o
] Incl.
[
o
]
α
95
[
o
] k Decl. [
o
] Incl.
[
o
]
α
95
[
o
] k
n
L. Tith.+ E.Berr.
B
R
351.7
–55.4
3.1
12.1
10.4
77.5
3.1
11.9
168
L. Tith.+ E.Berr.
C
N
278.0
53.3
7.1
3.2
199.3
–27.3
8.0
2.6
119
L. Tith.+ E.Berr.
C
R
104.1
–46.1
6.4
4.8
19.3
13.2
6.4
4.8
101
L. Tith.+ E.Berr.
C
N*
)
286.1
44.5
4.7
4.0
198.1
–15.0
5.2
3.7
220
377
STRATIGRAPHY OF THE JURASSIC-CRETACEOUS GRESTEN KLIPPENBELT (AUSTRIA)
Tavera et al. 1994; Bornemann et al. 2003; Pszczółkowski &
Myczyński 2004; Tremolada et al. 2006; Halásová in Micha-
lík et al. 2009).
The lowermost occurrences of nannofossils are partly ob-
scured due to poor preservation, but we tentatively identified
the boundaries of zones and subzones based on certain strati-
graphic markers (Polycostella beckmannii, Helenea chiastia,
Hexalithus noeliae, Nannoconus wintereri, Nannoconus
globulus minor, Nannoconus steinmannii minor, Nannoco-
nus kamptneri minor, Nannoconus steinmannii steinmannii,
Nannoconus kamptneri kamptneri, Nannoconus globulus
globulus).
Tremolada et al. (2006) detected that Conusphaera domi-
nates the nannolith assemblage in the upper middle Tithonian
(“Conusphaera world”). This is corroborated by data obtained
in this study. The acme peak of the genus Polycostella in sam-
ples Nu 13.0 and 14.0 coincides with the middle Tithonian
Semiradiata Subzone (Reháková 2000b). Comparison with
the Brodno section (Michalík et al. 2007 and Michalík et al.
2009) indicate that the dominance of the nannolith Polycostel-
la beckmannii occurs somewhat lower in the Chitinoidella
Zone in the Nutzhof section. The first appearance of Helenea
chiastia is also demonstrated to be diachronous, being close to
the base of the calpionellid Crassicollaria Zone in the Brodno
section, but recorded in the uppermost part of the Chitinoidel-
la Zone in the Nutzhof section.
The most distinct nannofossil event is the onset of nanno-
conids which was observed in the interval comprising the
calpionellid Calpionella Zone, Ferasini Subzone (lowermost
Berriasian). This indicates a change in the paleooceano-
graphic regime. From the biostratigraphic point of view, the
upper J/K boundary datum based on nannofossils (Borne-
mann et al. 2003).
The change of saccocomid marl and limestone by overlying
calpionellid limestone in the Upper Tithonian also character-
izes J/K-boundary successions reported from numerous other
localities in Austria (e.g. Kristan-Tollmann 1962; Flügel
1967; Holzer 1968; Holzer & Poltnik 1980; Reháková et al.
1996), Germany (Lackschewitz et al. 1989), Poland (Pszczół-
kowski & Myczyński 2004) and Slovakia (Vašíček et al.
1992). Many of these localities, however, differ lithologically
from the section studied at Nutzhof. In most cases the sacco-
comid-bearing beds are pure, reddish limestone.
Saccocomid limestones have often been interpreted as
Kimmeridgian (e.g. Flügel 1967: p. 35; Sauer et al. 1992:
p. 183; Wessely 2008: p. 210, fig. 5) and have been used as
the marker bed for that stage (Bernouli 1972). Reliable strati-
graphic data is, however, commonly lacking. Based on well-
dated sections, the majority of the recorded saccocomid-
occurrences are of Tithonian age (Nicosia & Parisi 1979;
Keupp & Matyszkiewicz 1997). This is corroborated/support-
ed by the data from the present study.
Summary and conclusions
The studied section at Nutzhof represent a J/K-boundary
succession deposited in a distal slope-setting in the Gresten
Klippenbelt, a part of the Helvetic paleogeographic realm.
The Upper Jurassic to Lower Cretaceous pelagic sediments
represent a major sedimentation cycle.
The significant depositional change from a mixed silici-
clastic/carbonate to a pure carbonate depositional system is
marked by a change from a lower marly cyclic part to an up-
per calcareous part. Accordingly, the lower (Tithonian) mar-
ly part is characterized by dark, laminated pelagic marls and
marly limestones with intercalated turbiditic limestone beds
(e.g. allodapic limestones). The upper part (limestone) repre-
sents a phase of autochthonous pelagic sedimentation char-
acterized by bright, chert- and aptychi-bearing nannoconid
limestone. The macro-invertebrate fauna of the Berriasian
limestone succession is sparse, comprising rare ammonoids,
aptychi, belemnites and brachiopods. The macro-inverte-
brate fauna of the Tithonian marl-limestone succession is
rich in saccocomids accompanied by rare bivalves (inocera-
mids) and partly by abundant ammonites. The microfauna,
in contrast, is abundant, with dominating calpionellids and
radiolarians in the limestone succession and saccocomid
blooms within the marl-limestone succession.
The macrofauna, as already stated, is represented especially
by ammonoids, belemnoids, aptychi and bivalves. The
whole section yielded 46 ammonite individuals/specimens.
Sampling of the sparse ammonites was difficult due to hard-
ite sediments. The ammonite biostratigraphy is integrated
with micro- and nannofossil biostratigraphic data from the
marl-limestone succession and indicates Early Tithonian to
middle Berriasian ages (Hybonoticeras hybonotum Zone up
to the Subthurmannia occitanica Zone). Descendants of
Subplanites have not previously been reported within the
Gresten Klippenbelt. All ammonoids are typical of the Medi-
terranean Province.
The limitation of ammonite biostratigraphy obtained by
the new ammonite findings from Nutzhof has demonstrated
the importance of integrating macrofauna biostratigraphy
with the micro- and nannofossil biostratigraphy. The de-
scribed fauna increases our understanding of ammonite fau-
nas from the area of the Gresten Klippenbelt and the
neighbouring Waschberg Zone during deposition of the Juras-
sic/Cretaceous boundary interval. Both areas were at the time
located on the passive northern margin of the Penninic Ocean.
Magnetostratigraphic, geochemical and isotopes studies
contribute to the understanding of the environmental history
during the Jurassic-Cretaceous boundary interval in a little
known area. Sediment deposition took place during condi-
tions of relatively stable water masses with relatively low
sedimentation rates in an unstable sedimentological environ-
ment. This is reflected by a change in lithology from Nu 11.0
to Nu 13.0 (11 to 13 m). A series of event layers with rede-
posited faunal elements (e.g. phyllocrinids) indicate a trans-
port of sediment from shallower areas in the North. The
depositional area was influenced by the opening of the Pen-
ninic Ocean during the Late Jurassic to Early Cretaceous. A
phase of an earlier Penninic opening, is reflected as a signifi-
cant change in lithology and composition of faunal assem-
blage in the uppermost Tithonian (at Nu 10.0 m).
There is no evidence for redeposition of ammonites, which
are considered autochthonous and parautochthonous pelagic
elements from the open sea. Four crinoid taxa are recorded in
378
LUKENEDER, HALÁSOVÁ, KROH, MAYRHOFER, PRUNER, REHÁKOVÁ, SCHNABL, SPROVIERI and WAGREICH
the Tithonian Blassenstein Formation and comprise Balano-
crinus sp., Saccocoma tenella (Goldfuss), Crassicoma? sp.,
and Phyllocrinus belbekensis Arendt. Only S. tenella is abun-
dant. The other taxa, in particular the benthic isocrinids and
phyllocrinids are rare. Preservation and ossicle size range of
the latter groups indicate their allochthonous origin. The sac-
cocomid remains are restricted to the Tithonian, the saccoco-
mid-rich facies being overlain by calpionellid limestones.
The biostratigraphic study based on the distribution of
calpionellids allowed an identification of the Boneti Subzone
of the Chitinoidella Zone. The J/K boundary is recorded be-
tween the Crassicollaria and Calpionella Zone and is de-
fined by the morphological change of Calpionella alpina
tests. The base of the Crassicollaria Zone approximately co-
incides with the onset of Tintinnopsella remanei Borza and
the base of the standard Calpionella Zone, with the monospe-
cific calpionellid association being dominated by Calpionella
alpina Lorenz. Two further Subzones (Ferasini and Elliptica)
of the standard Calpionella Zone were recognized in radiolari-
an-calpionellid and calpionellid-radiolarian wackestones in
the overlying uppermost part of the section.
The appearance of several important nannofossil genera
allow the identification of the Lower, middle and Upper
Tithonian, and a relatively accurate identification of the
Tithonian-Berriasian boundary, and the definition of the
Lower Berriasian nannofossil zones. Coccoliths of the fami-
ly Watznaueriaceae and nannoliths of the genera Conus-
phaera, Nannoconus and Polycostella dominate the
assemblages. The interval between the FAD of Nannoconus
wintereri co-occurring with small nannoconids in sample
Nu 9 (the uppermost Tithonian) and the FAD of Nannoconus
kamptneri minor in sample Nu 5 (lowermost Berriasian) is
interpreted as the Tithonian-Berriasian boundary interval.
The nannoconid dominance in the lowermost Berriasian,
known as the “Nannoconus world” sensu Tremolada et al.
(2006) is now recorded in the Nutzhof section.
Paleomagnetic data across the J/K boundary strata allow the
construction of a detailed magnetostratigraphic zonation. The
interval between Nu 5 to 10.5 m provides a high-resolution
Fig. 7. Estimated average sedimentation rate diagram around the
J/K boundary at Nutzhof based on magnetostratigraphic and bios-
tratigraphic data.
profile with an almost continuous record of magnetic and
paleomagnetic parameters, that records the critical intervals
with boundaries of the magnetozones M19n—M20n. Accord-
ing to magnetozone M19n and Brodno Subzone, the J/K bound-
ary is identified within the interval between Nu 6.5—7 m.
Significant changes do not occur at the J/K boundary itself.
The step of remanent magnetization and magnetic susceptibil-
ity, at level Nu 10.0, occurs in magnetozone M20n below the
Kysuca Subzone. A similar jump of NRM and susceptibility
lies in the M20n just above the Kysuca Subzone in the Bosso
section. The average sedimentation rate in the Nutzhof sec-
tion is ca. 3.7 m/Myr (Fig. 7), but with high dispersion (from
2—11 m/Myr) differing from the average sedimentation rates
of 2.27 m/Myr recorded in Brodno and 2.88 m/Myr in Puerto
Esca
n
o. Relatively low rates (1 m/Myr) are recorded in the
Bosso Valley, but higher rates (3—11 m/Myr) are reported by
Grabowski & Pszczółkowski (2006) from the Tatra Moun-
tains. No significant change can be noted at or within the J/K
boundary interval. The integration of fossil and magnetostrati-
graphic data demonstrates a duration of approximately 7 mil-
lion years (approximately 150—143 Ma) for the deposition of
the Nutzhof section (Figs. 6 and 7).
The carbon isotope record documents a significant change
in the C-cycle dynamic suggesting a sluggish 3-D dynamic
of the marine system possibly associated with a decrease in
primary productivity. Abrupt oscillations mainly recorded
between the levels 10 and 6 m suggest a significantly unsta-
ble global carbon system during the Jurassic but a change to-
wards balanced conditions in the Cretaceous interval.
Acknowledgments: We are indebted to Hans Egger (Geologi-
cal Survey of Austria) who made us aware of the studied lo-
cality. The study was supported by the Austrian Science Fund
(FWF; Project P20018-N10) and by the Grant Agency of the
Czech Republic (Grant No. GACR 205-07-1365) and Re-
search Plan of the IG AS CR No. CEZ AV0Z30130516. This
is also a contribution to the 506 IGCP UNESCO Project,
APVV-0280-07, APVV-0248-07, APVV- 0465-06, APVT
51-011305 and LPP 0120-09. MW thanks IGCP 555 and the
Austrian Academy of Sciences for financial support. Thanks
go to members of the Kilian Group (Lower Cretaceous Am-
monite Working Group; president Stephane Reboulet, Lyon)
for fruitful discussions on the ammonoid fauna. Technical
support for photography was provided by Alice Schumacher
(Vienna). Franz Topka (Vienna) assisted with the preparation
of ammonoid specimens and Anton Englert (Vienna) prepared
the thin sections. Paleomagnetic analyses were performed by
Daniela Venhodová, Jana Drahotová, and Jiří Petráček. The
software for the evaluation of paleomagnetic measurements
was prepared by Otakar Man (Institute of Geology ASCR
v.v.i.). We thank Luc Bulot (Marseille) and Jacek Grabowski
(Warsaw) for their comments which helped to improve the
quality of the manuscript.
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Appendix
Crossplot of the
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