GeolCarp_Vol61_No4_309

www.geologicacarpathica.sk

GEOLOGICA CARPATHICA, AUGUST 2010, 61, 4, 309—326 doi: 10.2478/v10096-010-0018-z

Introduction

The  Jurassic/Cretaceous  (J/K)  boundary  interval  offers  good
correlation possibilities for marine sections in the Tethyan re-
gion because of the established (micro- and nanno-) biostratig-
raphy,  C-isotope  stratigraphy  and  magnetostratigraphy.  The
magnetic zones are relatively easy to identify, due to the spe-
cific  pattern  of  two  long  normal  magnetozones  (M20n  and
M19n), containing short reversed polarity subzones (M20n1r
and  M19n1r),  named  by  Houša  et  al.  (1996,  1999)  as  the
Kysuca  and  the  Brodno  respectively.  Microbiostratigraphic
callibration  of  Late  Tithonian/Berriasian  magnetozones  was
successfully performed in south Tethyan sections of the Apen-
nines  and  Southern  Alps  (Channell  et  al.  1987;  Channell  &
Grandesso  1987;  Ogg  et  al.  1991).  Detailed  magnetostrati-

graphic studies in the Apennines, Tatra Mts and Transdanu-
bian Mts were published recently (Houša et al. 2004; Speranza
et al. 2005; Grabowski & Pszczółkowski 2006; Grabowski et
al. 2010) and pilot results were reported from the Eastern Alps
(Pruner et al. 2009). The Brodno section in the Pieniny
Klippen Belt (PKB) is currently proposed as the J/K regional
stratotype in the Carpathians (Michalík et al. 2009).

As the integrated bio- and magnetostratigraphic frame-

work  of  the  J/K  boundary  interval  is  now  well  known,  the
magnetic  method  becomes  a  tool  in  identification  of  paleo-
environmental changes on a global or regional scale, akin to
those  in  Quaternary  loess  sequences  (e.g.  Heller  &  Evans
1995) or Middle—Upper Devonian shallow water carbonates
(e.g. Jackson et al. 1993; Hladil et al. 2006; Nawrocki et al.
2008).  Grabowski  &  Pszczółkowski  (2006)  and  Grabowski

Magneto-, and isotope stratigraphy around the Jurassic/
Cretaceous boundary in the Vysoká Unit (Malé Karpaty

Mountains, Slovakia): correlations and tectonic implications

JACEK GRABOWSKI

, JOZEF MICHALÍK

, ANDRZEJ PSZCZÓŁKOWSKI

and OTÍLIA LINTNEROVÁ

Polish Geological Institute, National Research Institute, Rakowiecka 4, 00 975 Warszawa, Poland; jacek.grabowski@pgi.gov.pl

Geological Institute, Slovak Academy of Sciences, Dúbravská cesta 9, P.O. Box 106, 840 05 Bratislava, Slovak Republic;

jozef.michalik@savba.sk

Institute of Geological Sciences, Polish Academy of Sciences, Research Centre in Warsaw, Twarda 51/55, 00-818 Warszawa, Poland;

apszczol@twarda.pan.pl

Department of Economic Geology, Faculty of Science, Comenius University, Mlynská dolina G, 842 15 Bratislava, Slovak Republic;

lintnerova@fns.uniba.sk

(Manuscript received January 22, 2010; accepted in revised form April 19, 2010)

Abstract: Magneto- and isotope stratigraphic studies in the Vysoká Nappe (Hlboča section, Fatric Unit, Malé Karpaty
Mts, Slovakia) were performed. A generally decreasing

C isotope curve is interpreted as a primary trend from the

Late Oxfordian (3.3 ‰ V-PDB) to the Late Tithonian (1.8—1.4 ‰ V-PDB). Data from the Tithonian part of the Tegernsee
Formation probably reflect “local” basin processes connected with the breccia formation in the latest Tithonian/earliest
Berriasian and/or with possible diagenetic overprint. The C-isotope record of the Berriasian Padlá Voda Formation is
more homogeneous (1.4—1.8 ‰ V-PDB) and assumed to be primary. Magnetostratigraphic investigations were focused
on the Jurassic/Cretaceous (J/K) boundary strata. Upper Tithonian nodular limestones of the Tegernsee Formation
differ substantially from Lower Berriasian calpionellid limestones of the Padlá Voda Formation in rock magnetic prop-
erties. Hematite is present in the Tegernsee Formation, while magnetite is the only magnetic mineral of the Padlá Voda
Formation. Additionally, the latter formation contains superparamagnetic magnetite, which significantly influences its
magnetic susceptibility. Correlation of normal and reversed magnetic intervals with the Late Tithonian global polarity
time scale was supported by microfossil stratigraphy. M21n to M20n magnetozones were distinguished, including the
short reversed Kysuca (M20n1r) Subzone within M20n. Interpretation of Lower Berriasian magnetostratigraphy was
more complex due to presence of breccia horizons and a stratigraphic gap at the J/K boundary in the lower part of the
Padlá Voda Formation embracing M19r and most of M19n magnetozones. This formation was also partially affected by
remagnetization. Detailed correlation between the isotope- and magnetic stratigraphy of the Tithonian—Berriasian in-
terval between Hlboča and Brodno sections is also complex due to J/K stratigraphical gap within the Hlboča section.
The primary B component accounts for counter-clockwise rotation of the Vysoká Unit with a magnitude of ca. 50°.
Since the paleodeclination of Paleogene and Karpatian—Eggenburgian rocks in the area is similar, the rotation must have
taken place after Early Miocene. The paleoinclinations of several Upper Tithonian—Berriasian sections of the Central
Western Carpathians and western part of the Pieniny Klippen Belt are consistent and indicate paleolatitude of 27—30°N.

Key words: J/K boundary, Western Carpathians, paleomagnetism, magnetostratigraphy, magnetic susceptibility, stable
isotopes, microfossil stratigraphy.

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STRATIGRAPHY OF THE JURASSIC/CRETACEOUS BOUNDARY IN THE VYSOKÁ UNIT (SLOVAKIA)

et al. (2010) attempted to link petromagnetic properties of
formations in the Tatra Mts (Poland) and central part of the
Transdanubian Mts (Hungary) with changing sedimentary
conditions.

Isotopic research in the J/K boundary sequences in various

parts of the world (but mainly in the Tethyan area) confirmed
a correlative shape of the

C curve, reflecting relationship

between  global  oceanic  and  atmospheric  conditions  and  the
extent  of  production  and  deposition  of  organic  matter  in
oceanic  sediments  (Scholle  &  Arthur  1980;  Weissert  et  al.
1985; Weissert & Channell 1989; Price et al. 2000; Gröcke et
al.  2003;  Michalík  et  al.  2009,  and  many  others).  The

record in carbonates is becoming an important stratigraphic
tool, because it integrates information on evolution both in the
organic and inorganic part of the carbon cycle. As the total
range of fluctuations usually does not exceed 1 or 2 ‰ (excep-
tionally 2 to 3 ‰), the significance of isotopic curve changes
is interpretable in biostratigraphically or magnetostratigraphi-
cally well characterized sections.

In this paper, new paleomagnetic, magnetostratigraphic,

magnetic  susceptibility  and  stable  isotope  data  from  the
Hlboča section (Vysoká Nappe, Malé Karpaty Mts) are pre-
sented. This section was biostratigraphically correlated with
the regional J/K stratotype section at Brodno and with other
magnetostratigraphically  studied  sections  in  the  Western
Carpathians.  The  global  vs.  diagenetic  trend  of  the  Oxford-
ian—Berriasian  C-isotope  curve  in  the  Hlboča  section  was
discussed.  Magnetostratigraphic,  biostratigraphic  and  iso-
tope stratigraphic scales were compared. The significance of
paleomagnetic results for sedimentary and paleotectonic re-
constructions  of  the  Central  Western  Carpathians  was  also
briefly discussed.

Geological setting

The Malé Karpaty Mts form the westernmost part of the

Central  Western  Carpathians  close  to  the  junction  with  the
Northern  Calcareous  Alps  (Fig. 1).  Its  structure  joins  ele-
ments of the Alpine and Carpathian architecture. The lower-
most  unit  exposed  is  the  Borinka  Unit  of  Ultra-Tatric
appurtenance,  covered  by  the  thick  Tatric  Bratislava  grani-
toid nappe with its Mesozoic sedimentary cover (Fig. 1). The
Alpine  superficial  nappe  system  lies  above  it.  Its  basal  part
belongs  to  the  Vysoká  Nappe,  derived  from  the  northern,
marginal  part  of  the  Fatric  Domain,  where  slope  and  ridge
facies  prevailed  (Plašienka  et  al.  1997).  Thrusting  of  the
Vysoká  Nappe  over  Tatric  Mesozoic  cover  and  crystalline
basement  (Mahe   1987)  might  have  taken  place  around  the
Turonian/Coniacian boundary (Plašienka et al. 1991). High-
er tectonic units are represented by the Hronic nappe system
(the Jablonica, Havranica and Veterlin Nappes).

The Hlboča section is located in the Vysoká Nappe, in the

NE part of the Malé Karpaty Mts, in a half-blind karstic val-
ley (with the only small waterfall in the area called the Padlá
Voda) close to the Smolenice village, ca. 50 km to the NNE
from Bratislava (Fig. 1). The closure of the valley is formed
by steep rock walls called the Mníchove Diery (“Monk’s
holes”); they comprise almost complete Upper Jurassic—

Lower Cretaceous sequence, dipping monoclinally to the
NW (Borza & Michalík 1987b).

Sampling and methods of study

A total of 106 samples have been taken from the sequence

in 0.5 m (in the upper part of section in 1 meter) intervals for
thin  sectioning  and  microfacies  study.  Allochems  (clastic
grains,  calcareous  and  siliceous  plankton  tests,  shell  frag-
ments of benthic organisms) and micrite have been evaluated
under optical microscope in percent using the optical charts
of Bacelle & Bosellini (1965). The data obtained have been
applied  in  graphic  representation  of  mutual  changes,  illus-
trating  transport  and  sedimentation  changes  during  eustatic
sea level fluctuations (Michalík 2007).

Fourty-seven limestone beds were sampled for magneto-

stratigraphic  study.  Samples  were  taken  either  with  a  gaso-
line  powered  drill  (38  beds)  or  as  hand  samples  (9  beds).
Sampling resolution was higher within the Tegernsee Forma-
tion: approximately three samples per one meter were taken.
For comparison, in the difficult conditions of the Padlá Voda
Formation,  forming  steep  walls  of  the  karstic  valley,  only
lower  resolution  sampling  (one  sample  per  one  meter)  was
performed. Most of the sampled beds (36) were also studied
in thin sections for microfossil stratigraphy.

Standard cylindrical specimens 2.2 cm high and 2.5 cm in

diameter were prepared from drill cores and hand samples. Pa-
leomagnetic  experiments  were  performed  in  the  Paleomag-
netic  Laboratory  of  the  Polish  Geological  Institute.  Natural
remanent magnetization (NRM) was measured with the JR6a
spinner magnetometer and the KLY2 kappabridge was used
for  magnetic  susceptibility  measurements.  Specimens  were
demagnetized  exclusively  by  the  thermal  method  using  a
MMTD1  oven.  The  results  of  measurements  were  further
processed using the Remasoft software (Chadima & Hrouda
2006). A fold test was applied using the method of Watson
&  Enkin  (1993).  Rock  magnetic  investigations  comprised
measurements  of  isothermal  remanent  magnetization  (IRM)
applied along the Z axis in the field of 1 T, and then antipar-
allel in the field of 100 mT (using a MMPM pulse magnetiz-
er). The S parameter calculated as a ratio of IRM intensities
applied  in  both  fields  was  indicative  for  proportions  of  low
and high coercivity minerals. In samples from selected beds,
stepwise  acquisition  of  the  IRM  (in  the  maximum  field  of
1.4 T) was performed, followed by thermal demagnetization
of three axes IRM acquired in the fields of 1.4 T, 0.4 T and
0.1 T (Lowrie 1990). Low and high frequency susceptibility
of  selected  beds  was  studied  by  means  of  the  Bartington
MS2 susceptibility meter to estimate the contribution of the
very fine (close to superparamagnetic state – SP) magnetic
fraction (Forster et al. 1994).

Carbon and oxygen isotope analyses were carried out on 47

bulk carbonate samples from the Oxfordian- to Lower Berria-
sian part of the Hlboča section using the Finnigan MAT-2
mass spectrometer. The values are reported in terms of the
Vienna-PDB (V-PDB) in the standard

δ notation in ‰, with a

precision of ± 0.01 ‰. The total organic (TOC) and inorganic
carbonate content (TIC) was measured on the C-MAT 550.

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GRABOWSKI, MICHALÍK, PSZCZÓŁKOWSKI and LINTNEROVÁ

TIC values were recalculated to the CaCO

content in order

to assess the carbonate content of the samples.

Lithology, sequence stratigraphy and isotope data

The lower part of the section sampled (between 25 and

34 m, see Fig. 2) is formed by reddish and pink nodular lime-
stones  attributed  to  the  Tegernsee  Formation  (Borza  &
Michalík 1987a,b; Vašíček et al. 1994; probable equivalent of
the  Czorsztyn  Limestone  Formation  of  Birkenmajer  1977;
Lefeld et al. 1985). The limestones are irregularly, sometimes
thin  lenticularly,  or  even  schistose  bedded,  with  layers  of
intraclasts. The clasts are formed by pale rosa micrite, the ma-
trix consists of reddish brown more marly micrite. Ammonite
and belemnite fragments are relatively common, but they have
been heavily corroded and broken prior to deposition.

The amount of allochems fluctuates in the more or less

regular deepening upward cycles. Seven such cycles have

been recognized in the Tegernsee Formation. Their lowstand
part contains more clastic quartz; an increase of fragments of
benthic organisms in biomicrosparite to biomicrite is observed
during shallowing upward. The representation of biomicrite
accompanied by amount of planktonic tests increases to-
wards highstand (Fig. 2).

Generally, the Padlá Voda Formation consists of thick

(poorly)-bedded  grey  calpionellid  limestones.  However,  the
boundary  of  the  Tegernsee-  and  the  Padlá  Voda  Formations
coincides  with  (several)  limestone  breccia  beds  between  32
and 35 m of the section (Borza & Michalík 1987b; Michalík et
al. 1990, 1995). The stratigraphic extent and thickness of brec-
cias appears as a true problem within the section, as the brec-
cia is hardly visible on the weathered surface of rock, and is
clearly recognizable only on large polished slabs (Fig. 3). The
limestone  extraclasts  attain  10—30 mm,  rarely  up  to  70 mm,
they  were  derived  from  underlying  Tithonian  and  lowermost
Berriasian  strata.  The  erosion  of  12 m  of  the  uppermost
Tithonian  limestone  sequence  was  postulated  by  Borza  &

Fig. 2. Lithology, distribution of allochems in microfacies, CaCO

content, TOC, isotopes of O and C in the Hlboča section.

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STRATIGRAPHY OF THE JURASSIC/CRETACEOUS BOUNDARY IN THE VYSOKÁ UNIT (SLOVAKIA)

Michalík 1987b (see also Michalík et al. 1995). It probably
originated during several extensional pulses, which denivelat-
ed the sea bottom (as in the Upper Valanginian Nozdrovice
Breccia in more distal parts of the Fatric Zliechov Basin, see
Michalík 2007). The higher part of the Padlá Voda Formation
consists of massive limestone with large (up to 25 cm in diam-
eter) cherts. A marly bedded interval with weak silicification
occurs near the top of the sequence. The Padlá Voda Forma-
tion is covered by the bedded to schistose marly Hlboč Forma-
tion (Valanginian—Hauterivian) at 57 m of the section.

Geochemical analyses illustrate a small increase in carbon-

ate content in each eustatic cycle from lowstand to highstand,
correlatable with periodically fluctuating carbonate micro-
and nannoplankton bioclasts (Fig. 2). On the other hand, the
accumulation rate of organic carbon in the Hlboča section was
very low, comparable to the Brodno section, or other sections
studied (Weissert & Channell 1989; Michalík et al. 2009).

The

C curve shows a decreasing trend from Oxfordian

values often above 3 ‰ to Berriasian values below 2 ‰

(Fig. 2). A similar trend was documented else-
where and it is interpreted as a global trend
(Jenkyns & Clayton 1986; Weissert & Channel
1989; Jenkyns 1996; Price & Rogov 2009).

The influence of diagenetic and post-sedi-

mentary processes was tested using

C and

O plots of bulk samples (Fig. 4). Values of

C and

O from the lower, Oxfordian—

Kimmeridgian part of the section (

C > 2) do

not show a positive covariance (Fig. 4a).
Therefore, these limestones were not modified
during diagenesis or deep burial (e.g. Föllmi et
al. 2006; Duchamp-Alfonse et al. 2007).

The elongated shape of the Tithonian data

cluster (18—32 m) from the Tegernsee Forma-
tion  seems  to  indicate  a  relatively  high  posi-
tive  correlation  (Fig. 4b)  –  which  could  be
regarded  as  evidence  for  diagenetic  transfor-
mation of the limestone bed studied. However,
when  the  sample  with  the  most  extreme

value (29.5: + 0.87 ‰) is removed from the
set, the degree of covariance decreases. More-
over,

O value change is less distinct than

the change in

C in this sample (Figs. 2, 4),

which is striking if we assume higher diage-
netic “sensitivity” of the oxygen isotope.
Therefore, the

C composition of the 30.5 m

sample could have been affected by local con-
ditions  in  the  basin  indicated  by  sedimentary
breccia occurrence. It is a matter of discussion,
whether  the  above  mentioned  extensional
pulses,  which  triggered  erosion,  redeposition
and mixing of sediment could have resulted in
local

C value decrease both in the water

column and in the carbonate deposited. On the
other side, physical changes evoked by sedi-
ment mixing could have produced different di-
agenetic

C ratio formed in sediment.

The more compact cluster of data from the

Berriasian Padlá Voda Formation (33—55) re-

Fig. 3. Hlboča Valley – the Mníchove Diery section. a – Beds 29—35 around the J/K
boundary; b – Macrophotography of the brecciated limestone at the base of the
Padlá Voda Formation.

veals a negative trend and rather co-variance of

C and

O values (Figs. 2 and 4c). Although diagenetic overprint

cannot be excluded, the level of co-variation is lower than in
the  Tithonian  set.  The  uppermost  sample  (55.5 m)  from
transitional  beds  between  the  Padlá  Voda-  and  the  Hlboč
Formations  shows  the  most  negative  values  of  both  isotope
ratios.  From  the  point  of  view  of  diagenetic  overprint  of
Berriasian  samples  this  datum  represents  a  rather  extreme
value and it may be excluded from the graphic plot.

Regular fluctuation of

O values in the Berriasian Padlá

Voda Formation resembles similar cyclic changes in calcare-
ous plankton content and the general sequence stratigraphic
arrangement of these beds (Tremolada et al. 2006). Although
the most negative

O peaks are associated with sequence

boundaries, connection with meteoric diagenesis (Weissert
& Mohr 1996) in these deeper water conditions seems
improbable.

For comparison, crossplots of

C and

O values from

the Brodno section which embraces a similar stratigraphic

314

GRABOWSKI, MICHALÍK, PSZCZÓŁKOWSKI and LINTNEROVÁ

interval  do  not  show  any  co-variation  (Fig. 4d).  Therefore,
primary  isotopic  ratios  were  preserved  (Michalík  et  al.
2009). Either slight diagenetic modification of both oxygen
and carbon isotopic values, or a significant local overprint in
the Hlboča section should be included in the interpretation of
deviation from the global trend (Weissert & Channell 1989;
Marshall  1992;  Morante  &  Hallam  1996;  Weissert & Mohr
1996; Price & Rogov 2009, etc.).

Microbiostratigraphy

Biostratigraphy of Upper Jurassic—Lower Cretaceous forma-

tions  in  the  Mníchove  Diery  section  have  been  performed  by
Michalík  et  al.  (1990),  Reháková  &  Michalík  (1992),  or  by
Vašíček  et  al.  (1994).  Michalík  et  al.  (1990)  reported  six
Kimmeridgian  to  Early  Berriasian  microfossil  zones  (Pop
1976,  1986,  1994;  Remane  et  al.  1986).  The  Moluccana-,
Malmica-, Chitinoidella- and Crassicollaria Zones were distin-
guished  in  the  Tegernsee  Formation.  The  boundary  between
the  Tegernsee-  and  the  Padlá  Voda  Formations  has  been  put
below  the  Early  Berriasian  Calpionella  alpina  Subzone.  The
Calpionella  Standard  Zone,  subdivided  into  the  Alpina-  and
the Remaniella Subzones, was identified in the lower part of
the Padlá Voda Formation.

Current biostratigraphic study of the Hlboča (Mníchove

Diery) section was integrated with sampling for magneto-
stratigraphic investigations. It was based on 36 samples taken
from the Tithonian—Middle Berriasian limestones (Fig. 5). In

this  part  of  the  section,  Chitinoidella-,  Crassicollaria-  and
Calpionella  biozones  have  been  recognized.  However,  the
studied  section  is  not  complete,  as  a  breccia  occurs  at  the
boundary  between  the  Crassicollaria  and  Calpionella  Zones
(= Tithonian/Berriasian boundary).

The interval examined starts in the middle part of the

Tegernsee  Formation.  The  typical  red  nodular  limestone  de-
scribed  by  Michalík  et  al.  (1990)  is  rich  in  Saccocoma  ossi-
cles.  The  25-3  sample  consists  of  Globochaete-Saccocoma
biomicrite, containing rare Borziella slovenica (Borza) merely
visible  in  thin  section.  This  sample  belongs  to  the  Early
Tithonian Dobeni Subzone of the Chitinoidella Zone (Fig. 5).
Better  preserved  chitinoidellids  occur  in  the  25-8  sample:
Daciella  svinitensis  Pop,  D.  cf.  svinitensis  Pop,  Daciella
almajensis Pop, D. banatica Pop, Daciella danubica Pop, and
Borziella  slovenica  (Borza).  In  other  samples,  scarce
chitinoidellids like Dobeniella sp. cf. D. cubensis (Furrazola-
Bermúdez), Daciella banatica Pop, D. rumanica Pop and also
Borziella slovenica (Borza) occur.

The boundary of Dobeni/Boneti Subzones is located be-

tween  samples  No. 26  and  26-8  (Fig. 5).  Almajella  cristo-
balensis  (Furrazola-Bermúdez),  Dobeniella  colomi  (Borza)
and Dobeniella cf. cubensis (Furrazola-Bermúdez) have been
recorded in the sample 26-8. Saccocoma—Globochaete biomi-
crite (27-1) contains frequent Chitinoidella sp. (cf. Ch. boneti
Doben),  “Chitinoidella”  pinarensis  (Furrazola-Bermúdez  &
Kreisel),  Dobeniella  sp.,  Borziella  slovenica  (Borza),
Dobeniella bermudezi (Furrazola-Bermúdez) and Carpathella
rumanica  Pop.  This  assemblage  is  correlated  with  the  Late

Fig. 4. Crossplot of carbon and oxygen isotopic data: a – Total Oxfordian—Berriasian data; b – Tithonian part of the Tegernsee Formation;
c – Berriasian Padlá Voda Formation from the Hlboča section; d – Total data from the Brodno section.

315

STRATIGRAPHY OF THE JURASSIC/CRETACEOUS BOUNDARY IN THE VYSOKÁ UNIT (SLOVAKIA)

Fig. 5. Distribution of identified microfossils in the Hlboča section sequence.

Tithonian Boneti Subzone in the upper part of the Chitinoidel-
la Zone. Up section, chitinoidellids are still present, although
poorly  preserved.  Borziella  slovenica  (Borza)  and  Longicol-
laria dobeni (Borza) have been recognized in the 27-4 sample
(Fig. 5). This assemblage is characteristic rather of the Dobeni
Subzone (Reháková 2002), but according to Pop (1996, 1997)
both  taxa  occur  throughout  the  Chitinoidella  and  Praetintin-
nopsella Zones. Unidentified chitinoidellids also occur in the
27-7 and 30-5 samples (also in the bed 31 according to Rehá-
ková  &  Michalík  1992),  whereas  fully  hyaline  calpionellids
are  found  in  31-3.  Therefore,  the  boundary  of  Chitinoidella/
Crassicollaria  Zones  is  located  below  the  latter  sample,  per-
haps close to the contact of the red nodular limestone with red-
dish to light grey biomicrites (Fig. 5). According to Michalík
et  al.  (1990,  text—fig. 2),  the  Chitinoidella/Praetintinnopsella
zonal  boundary  is  located  between  beds 31  and  32.  The
Praetintinnopsella  Zone  was  not  recognized  in  our  study,
nevertheless  this  zone  has  been  reported  by  Michalík  et  al.

(1990) and Reháková & Michalík (1992) from a limestone
interval about one meter thick.

The Late Tithonian Crassicollaria Standard Zone comprises

3 m  thick  biomicrite  beds.  This  zone  is  subdivided  into
Remanei  and  Intermedia  Subzones.  The  Intermedia  Subzone
is  represented  by  light  grey  biomicrites  and  microbreccias
with  calpionellids.  The  calpionellid  assemblages  observed  in
the dark grey limestone clasts and the light grey cement (33-6
sample) have similar composition (Fig. 5): Calpionella alpina,
Crassicollaria  brevis,  Cr.  intermedia  and  Cr.  parvula(?).
Thus, Upper Tithonian calcareous sediments were eroded and
redeposited along the basinal slope (Michalík et al. 1990).

The limestones of the Padlá Voda Formation are about

24 m thick. Clast-bearing calpionellid-Globochaete biomicrite
at the base of this formation (34-1 sample) contains abundant
Calpionella alpina, frequent Crassicollaria parvula and rare
Calpionella sp., Crassicollaria intermedia and Cr. brevis.
This assemblage may represent either the Tithonian/Berriasian

316

GRABOWSKI, MICHALÍK, PSZCZÓŁKOWSKI and LINTNEROVÁ

boundary interval (Crassicollaria/Calpionella Zones) or, alter-
natively, redeposited Upper Tithonian Crassicollaria loricas
in the earliest Berriasian Calpionella alpina—Cr. parvula
assemblage. The latter explanation seems to fit the results of
thin section analysis better.

A typical Lower Berriasian association of C. alpina, Cr.

parvula  and  T.  carpathica  with  rare  (less  than  0.5 %  of  all
identified  calpionellid  specimens)  Crassicollaria  colomi
Doben,  1963  is  contained  in  the  34-7  sample  (Fig. 5).  In  the
standard  zonation  (Remane  et  al.  1986)  this  calpionellid
assemblage indicates Early Berriasian Alpina Subzone.

The index taxon of the Ferasini Subzone (Pop 1994; Rehá-

ková 1998), Remaniella ferasini (Catalano 1965) has been
found in our sample 39, only. In 40—41-5 samples, limestone
clasts with Cr. intermedia and Cr. brevis occur, sometimes
with oncolitic crusts.

The boundary of the Ferasini- and Elliptica Subzones was

recognized between samples 41-5 and 42-4. Limestones of the
middle  Berriasian  Elliptica  Subzone  are  3.3 m  thick  (Fig. 5).
The  index  of  the  Cadischiana  Subzone,  Remaniella  cadis-
chiana  (Colom,  1948),  along  with  Remaniella  duranddelgai
Pop,  Calpionella  elliptica  Cadisch  and  Tintinnopsella  sp.  ex

Fig. 6. Rock magnetic properties of the Tegernsee- and the Padlá Voda Formations. a –Crossplot of S ratio and IRM

; b – magnetic sus-

ceptibility changes during thermal treatment; c,d – IRM acquisition curve and thermal demagnetization of the 3 axes IRM acquired in the
fields of 0.1 T, 0.4 T and 1.4 T for representative specimens of the Tegernsee (c) and the Padlá Voda Formations (d).

317

STRATIGRAPHY OF THE JURASSIC/CRETACEOUS BOUNDARY IN THE VYSOKÁ UNIT (SLOVAKIA)

gr. T. longa-subacuta was found in four samples from 6 m
thick beds above (Fig. 5).

Rock magnetic properties

Measurements of magnetic parameters revealed distinct

differences in rock magnetic properties between the Tegernsee
and the Padlá Voda Formations (Fig. 6a,b). High coercivity
minerals occur in high amounts in the Tegernsee Formation.
Its maximum unblocking temperature close to 700

°C

(Fig. 6c) proves its identification with hematite. The hematite
is accompanied by a low coercivity magnetite with unblock-
ing temperatures between 550 and 600

°C. The magnetite is

the only magnetic mineral in the Padlá Voda Formation:
only a low coercivity fraction is observed and the maximum
unblocking temperature does not exceed 600

°C (Fig. 6d).

Magnetic susceptibility of nodular limestones of the Tegern-
see Formation rises within the section from ca. 20

×10

—6

Units in the lowermost part (the Dobeni Subzone) up to
70

×10

—6

SI in the Crassicollaria Zone (Fig. 7). Within the

Padlá Voda Formation, large variations of magnetic suscep-
tibility are observed (between 20 and 130

×10

—6

SI Units).

Susceptibility values higher than 100

×10

—6

SI, occurring

within  the  Padlá  Voda  Formation,  are  related  to  superpara-
magnetic  (SP)  fraction  which  is  indicated  by  a  frequency
dependent  diagram  (Fig. 8a).  Differences  in  magnetic  sus-
ceptibility  changes  during  thermal  treatment  between  two
formations,  especially  large  decrease  between  350  and
450

°C in samples from the Padlá Voda Formation (Fig. 6b),

must also be attributed to alterations of the SP fraction. Simi-
lar differences in magnetic susceptibility behaviour were ob-

served in the Strážovce section (Grabowski et al. 2009), be-
tween the Jasenina- and the Osnica Formations (no SP mag-
netite), and the Mráznica Formation (abundant SP
magnetite). NRM intensities are the highest in the lowermost
part of Tegernsee Formation, up to 50

×10

—4

A/m, and de-

crease below 10

×10

—4

A/m in the Padlá Voda Formation

(Fig. 7). In the latter case, a good correlation is observed be-
tween  susceptibility  and  NRM  and  IRM  intensity,  which  is
not  the  case  in  the  Tegernsee  Formation  (Fig. 8b  and  c).
These observations account for different carriers of magnetic
susceptibility signal in the two formations: mostly paramag-
netic in the Tegernsee Formation and mostly ferro- + super-
paramagnetic  in  the  Padlá  Voda  Formation.  It  should  be
noted that the magnetic susceptibility pattern across the J/K
boundary  is  exactly  opposite  to  that  noted  typically  in  the
Tethyan  sections.  There  is  a  general  tendency  of  magnetic
susceptibility  decrease  from  the  Upper  Tithonian  to  Lower
Berriasian  strata;  it  is  known  from  sections  of  Val  Bosso
(Houša  et  al.  2004),  Brodno  (Houša  et  al.  1996,  1999),
Pośrednie  (Tatra  Mts;  Grabowski  &  Pszczółkowski  2006),
Nutzhof  (Eastern  Alps;  Pruner  et  al.  2009),  and  Lókút
(Transdanubian Range; Grabowski et al. 2010). The opposite
trend, observed in the Hlboča section only, is related to rela-
tive abundance of SP magnetite in the Padlá Voda Formation.
Calpionellid limestones from other sections mentioned did not
reveal evidence of SP particles and their susceptibility is rath-
er dominated by ferro- or paramagnetic matrix (Grabowski &
Pszczółkowski 2006; Grabowski et al. 2010).

Thermal demagnetization revealed mostly two components

of magnetization. The A labelled component was demagne-
tized between 20 and 300

°C in most samples (Fig. 8d). In

present-day coordinates, its direction is close to the expected

Fig. 7. The Hlboča section. (a) k – Magnetic susceptibility. (b) NRM intensities (Inrm). (c) Computed VGP latitude. (d) Magnetic polari-
ty: black – normal polarity, white – reversed polarity; crosses – reversed polarity determined from great circle trends. (e) Correlation
with global polarity time scale (two options, second option preferred).

318

GRABOWSKI, MICHALÍK, PSZCZÓŁKOWSKI and LINTNEROVÁ

present-day geomagnetic field of the area and the application
of  tectonic  correction  results  in  poorer  clustering  (Table 1).
These observations, as well as unblocking temperature range
account  for  interpretation  of  the  A  component  as  the  recent
viscous remanent magnetization. The second, B component, is
unblocked  between  300  and  550—575

°C (Fig. 8d). It reveals

dual polarity. Therefore, the B component might be interpret-
ed as the primary magnetization.

The directions of characteristic components are presented in

Table 1 and in Fig. 9. As the B component between 33.6 and
34.9 m of the section is greatly dispersed, it is inferred that
samples in this interval were taken from the breccia interval at

Fig. 8. a – Susceptibility differences

—

measured at low (0.47 kHz;

) and high frequency (4.7 kHz;

) plotted as a function of a

low frequency susceptibility

; b – magnetic susceptibility (k) vs. NRM intensity (Inrm); c – magnetic susceptibility (k) vs. IRM

in-

tensity; d – Thermal demagnetization of typical samples. Orthogonal projection (Zijderveld diagram). l – HL33, Upper Tithonian, mag-
netozone M20n1n; 2 – HL31-5, Upper Tithonian, magnetosubzone M20n1r (Kysuca); 3 – HL31-1, Upper Tithonian, magnetozone
M20n2n; 4 – HL28-1, Upper Tithonian, magnetozone M20r. All projections after tectonic correction. Open squares – horizontal (xy) plane;
solid circles – vertical (yz) plane. NRM intensities in 10

—3

A/m.

320

GRABOWSKI, MICHALÍK, PSZCZÓŁKOWSKI and LINTNEROVÁ

Speranza et al. 2005) but need to be explained. Normal direc-
tions of the B component are better clustered than reversed po-
larity directions, although both populations pass the fold test
(Fig. 9e).  Moreover,  not  all  reverse  polarity  directions  might
be  calculated  in  some  samples  (mostly  from  the  Padlá  Voda
Formation): their reverse polarity was inferred from great cir-
cle  trends  (Fig. 7d).  To  explain  this,  we  suggest  that  the  B
component  is  contaminated  by  a  normal  polarity  overprint
which is close to the normal direction of the calculated B com-
ponent. The unblocking temperatures of the overprint and pri-
mary  magnetization  overlap  and  therefore,  isolation  of
“purely” primary direction is not possible. This is a very com-
mon  situation  observed  in  the  paleomagnetism  of  Mesozoic
carbonate rocks from the Carpathians (e.g. Márton & Márton
1981; Grabowski 2005; Lewandowski et al. 2005) and Apen-
nines (Houša et al. 2004; Speranza et al. 2005). Normal polari-
ty  overprint  was  acquired  most  probably  during  the
Cretaceous  Quiet  Zone,  when  maximum  burial  and  over-
thrusting processes took place (see the “Geological setting”).

Magnetic stratigraphy

Normal (N) and reversed (R) polarity intervals within the

Hlboča  section  (according  to  polarity  of  the  B  component)
were numbered (Fig. 7d). Three normal (N1—N3) and two re-
versed intervals (R1—R2, between Tithonian Dobeni and Inter-
media  Subzones)  were  noted  within  the  sampled  part  of  the
Tegernsee Formation, between beds 25-3 and 33-6. The low-
ermost beds sampled, between bed 25-3 and 26-6 reveal nor-
mal  magnetization  (N1)  and  belong  to  the  Dobeni  Subzone.
Magnetozone N1 is interpreted as M21n. This is in accordance
with the data of Ogg et al. (1991) and Grabowski et al. (2010),
where the base of the Chitinoidella Zone occurs mostly within
this magnetozone. The following R1 reversed polarity interval
(between  26-8  and  29-5)  belongs  to  the Boneti  Subzone  and
might  correspond  to  the  M20r  magnetozone.  It  should  be
mentioned that the first occurrence (FO) of chitinoidellids in
the  Brodno-  and  in  the  Pośrednie III  sections  (Boneti  Sub-
zone) takes place within this magnetozone.

A short R2 reversed polarity interval, documented by sam-

ple 31-5 falls within the Remanei Subzone. It must be corre-

Table 1: Characteristic paleomagnetic components from the Hlboča section (Malé Karpaty Mts). In bold: components used for geological
interpretation.

Component D/I

k Dc/Ic

k N/N

23/58

2.9

56.3

0/16

3.7

35.6

43/47

nor

(all)

207/57

7.3

19.1

292/53

6.7

22.2

22/47

nor

(breccia excluded)

204/57

6.3

27.5

293/54

5.7

33.4

20/47

rev

(all)

84/–82

15.8

5.7

151/–38

14.1

7.0

18/47

rev

(breccia excluded) 67/–74

10.6 15.0 142/–39

8.7

14/47

nor+rev

(breccia excluded)*

215/65

6.6

15.0

307/49

6.1

17.4

34/47

nor+rev

(breccia excluded)**

218/67 –

–

310/47

–

N = 2

lated with the Kysuca (M20n1r) magnetosubzone. Indeed, the
position of the Kysuca magnetosubzone is the same within all
studied Carpathian sections (Fig. 10): the Brodno (Houša et al.
1999;  Michalík  et  al.  2009),  Pośrednie III  (Grabowski  &
Pszczółkowski 2006) and Lókút (Grabowski et al. 2010): just
above  the  base  of  the  Crassicollaria  Standard  Zone.  Conse-
quently,  normal  interval  N3,  situated  within  the  Intermedia
Subzone  (between  samples  31-9  and  33-6)  should  corre-
spond  to  the  M20n1n  magnetozone.  It  must  represent  the
lower part of the Intermedia Subzone, since the upper part of
this subzone usually embraces the M19r and large part of the
M19n2n magnetozones (Grabowski & Pszczółkowski 2006;
Grabowski et al. 2010).

The correlation of upper part of the section to the GPTS is

rather speculative. The R3 magnetozone (sample 34 to 34-9,
Alpina Zone), is situated largely within the probably brecciat-
ed interval. The B component in this interval reveals consis-
tent negative inclinations, but its declinations are dispersed.
This might indicate that the Brodno magnetosubzone (M19n1r)
is represented in clastic beds.

As the beginning of the Ferasini Subzone coincides with the

bottom of our N5 interval, it is assumed that N5 corresponds
to the M18n magnetozone. The first appearance datum (FAD)
of Remaniella ferasini usually falls within the M18n magneto-
zone (Ogg et al. 1991; Houša et al. 2004), although it should
be noted, that this index is rare in our section (Fig. 5). In this
case, the R4 and N4 intervals should be correlated with the
M18r and topmost part of the M19n, respectively.

As the M19r and a large part of the M19n magnetozones are

apparently missing in the Hlboča section, it is assumed, that
the sediments deposited during those magnetochrons were
eroded and deposited in another part of the basin.

The reversed R5 magnetozone embraces samples 41 to 41-8

(boundary of Remaniella/Elliptica Subzones). It must be inter-
preted as the M17r magnetozone, since that is where the lower
boundary of the Elliptica Subzone is situated within the stan-
dard Italian sections (Ogg et al. 1991), as well as in the Tatra
Mts  (Grabowski  &  Pszczółkowski  2006).  Magnetostrati-
graphic  interpretation  of  the  uppermost  part  of  the  section
again poses some problems. N6 normal polarity magnetozone
(based  on  only  single  sample  no.  45),  most  probably  within
the lower part of the Cadischiana Subzone, might correspond

Mean paleopole for the section: Paleopole*: latitude 46.0

°N, longitude 282.5°E, dp = 5.3, dm = 8.1. Paleopole**: latitude 46.9°N, longitude

278.2

°E. Explanations: D/I – declination/inclination before bedding correction; Dc/Ic – declination/inclination after bedding correction;

αα

, k – Fisher statistics parameters; N/N

– number of beds used for calculation of characteristic direction/number of beds sampled;

dp, dm – confidence oval of paleopole estimation. * – calculated as mean of all normally and reversely magnetized beds; ** – calculated as
mean of normal and reversed sets.

321

STRATIGRAPHY OF THE JURASSIC/CRETACEOUS BOUNDARY IN THE VYSOKÁ UNIT (SLOVAKIA)

to M17n. Indeed, the position of this magnetozone in the Tatra
Mts in the Pośrednie II section is similar, and this is the only
normal magnetozone situated entirely within the C calpionel-
lid Zone (Ogg et al. 1991; Grabowski & Pszczółkowski 2006).
However, following this pattern, the R6 magnetozone (docu-
mented  by  samples  45-8  and  47),  situated  within  the  Cadis-
chiana Subzone, should correspond to the M16r. In the Tatra
Mts, this magnetozone embraces the upper part of the Cadis-
chiana Subzone and lower part of the Simplex Subzone. The
problem in interpretation is that the last subzone was not con-
firmed  in  the  highest  part  of  the  section  sampled  by  us.  The
highest N7 magnetozone should start within the Simplex Sub-
zone  and  it  should  be  interpreted  as  M16n  (Ogg  et  al.  1991;
Grabowski  &  Pszczółkowski  2006),  but  in  fact  only  the  Ca-
dischiana  Subzone  was  documented  as  far  as  bed  51.  This
might imply that:

1. The bottom part of the Simplex Subzone is difficult to

document (its presence is documented between 54 and 57 m
of the section – see Fig. 2).

2. The N6 magnetozone, based on a single sample 45, can-

not be interpreted as a real magnetozone, but it represents ei-
ther a geomagnetic excursion or an effect of remagnetization.

In our opinion, the second explanation is more plausible.

High resolution magnetostratigraphic studies prove that mag-
netic intervals based on single samples often cannot represent

magnetozones. Speranza et al. (2005) documented previously
unrecognized geomagnetic excursions within M16n and M16r
magnetic chrons in the Bosso section. They also report a nor-
mal polarity excursion within the Kysuca (M20n1r) magneto-
subzone.  Therefore,  the  N6  interval  in  our  section  might  be
interpreted as an excursion, although it might be strange that
excursion was documented with rather low resolution of sam-
pling. Remagnetization effect perhaps represents a more likely
explanation. As can be seen from Fig. 7d, all reversed polarity
samples between 36 and 47 m of the section reveal great circle
trends towards the reversed direction, during thermal demag-
netization. This indicates that this part of the Padlá Voda For-
mation  is  more  strongly  remagnetized  than  the  Tegernsee
Formation. This is also consistent with the relative abundance
of  the  SP  magnetite  within  the  Padlá  Voda  Formation:  the
presence of SP magnetite is usually accompanied by remagne-
tization phenomena (e.g. Jackson et al. 1993), sometimes very
strong,  as  is  the  case  of  the  Mráznica  Formation  in  the
Strážovce section (Borza et al. 1980; Grabowski et al. 2009).
Thin section analysis of sample 45 revealed that it is particu-
larly strongly silicified consisting mostly of chert concretions.
Therefore,  primary  magnetization  might  be  affected  by  di-
agenesis in this sample. Whatever the reason for the origin of
the N6 interval, in this case both reversed R5 and R6 intervals
should be interpreted rather as the M17r magnetozone, and the

Fig. 10. Summary of the current magnetostratigraphic studies of the J/K boundary sections in the Carpathians. Reference GPTS time scale
and correlation to calpionellid zones after Gradstein et al. (2004). Section references: Hlboča (this study); Lókút (Grabowski et al. 2010);
Brodno (Houša et al. 1999; Michalík et al. 2009); Western Tatra (Grabowski & Pszczółkowski 2006, composite section).

323

STRATIGRAPHY OF THE JURASSIC/CRETACEOUS BOUNDARY IN THE VYSOKÁ UNIT (SLOVAKIA)

N7 normal interval as the M17n. This interpretation is also
presented in the Fig. 7e (2

option). It is in agreement with

the  integrated  bio-  and  magnetostratigraphic  scheme  (Ogg  et
al. 1991; Grabowski & Pszczólkowski 2006), where the M17n
magnetozone  falls  into  the  Cadischiana  Subzone,  and  to  put
the  base  of  the  M16n  magnetozone  into  this  subzone  is  not
necessary.

The resolution of our magnetostratigraphic data is not high

enough  to  calculate  changes  of  sedimentation  rate  for  each
magnetozone.  However,  estimations  are  possible  for  the
M20r (4.59—6.22 m/Myr), M20n (3.1—4.5 m/Myr) and M17r
(7.58—9.83 m/Myr)  magnetozones.  Sedimentation  rates  for
M20n  and  M17r  should  be  treated  as  the  minimum  values,
since both these magnetozones are not complete in the Hlboča
section.  The  values  obtained  are  in  better  agreement  with
estimations of sedimentation rates by Michalík et al. (1995;
3—3.7 m/Myr  for  the  Tegernsee  Formation  and  7—11 m/Myr
for the Padlá Voda Formation) than by Vašíček et al. (1994;
0.23—1.56 m/Myr for the Tegernsee Formation and 5.5—9 m/Myr
for the Padlá Voda Formation). Anyhow, the typical trend of
sedimentation  rate  increase  across  the  J/K  boundary
(Grabowski & Pszczółkowski 2006; Grabowski et al. 2010)
is observed in this section, too.

The state of the art in magnetic stratigraphy of the Car-

pathian sections is presented in the Fig. 10. Until now, four
J/K boundary sections in the Carpathians have been calibrated
magnetostratigraphically, the magnetostratigraphic divisions
being controlled by microfossil stratigraphy. They embrace
the interval between the uppermost part of M22n (Lower Ti-
thonian, Brodno section) and M16n (Upper Berriasian, West-
ern Tatra Mts) magnetozones.

Both short reversed (Kysuca and Brodno) magnetosubzones

are  located  in  similar  positions  in  the  Brodno  and  the  Lókút
sections.  The  position  of  the  Brodno  magnetosubzone  in  the
Western Tatra section is fairly similar to those in the Brodno
and  the  Lókút  sections.  In  the  Hlboča  section,  part  of  the
Brodno magnetosubzone might be situated in the stratigraphic
gap at the J/K boundary. In the Western Tatra sections, the po-
sition of the Kysuca magnetosubzone is not well constrained
(Grabowski & Pszczółkowski 2006). Its location in the upper-
most part of the M20n zone is probably an artifact due to pre-
viously  unrecognized  thrust  contact  within  a  part  of  the
section, between M20 and M19 (Fig. 10).

The J/K boundary, indicated at the Crassicollaria/Calpi-

onella zones boundary, is traditionally placed in the middle
part of M19n2n (Gradstein et al. 2004). In the Brodno section,
this boundary was recently designated in the topmost part of
the M19n2n, just below the Brodno (M19n1r) magnetosub-
zone (Michalík et al. 2009).

Isotope stratigraphy

Weissert & Channell (1989) documented a decreasing trend

C-values from 2.07± 0.14 in the Oxfordian (CM 24—22)

to 1.16± 0.16 ‰ near to the Tithonian/Berriasian boundary
(CM18—CM14) in four Italian sections.

A trend, observable in the Hlboča section, was accompanied

by a decrease of organic C content in sediments. High positive

C values in the lowermost part of this section belonging to

the dinoflagellate Fibrata Acme Zone (Reháková in Michalík
et al. 1990; Reháková 2000) are comparable to the Oxfordian
δ

C event of Jenkyns (1996) located in the Transversarium

ammonite Zone (Padden et al. 2002). Due to low sedimentary
rate and oxidic environment with effective organic matter bio-
cycling, the water equilibrium has been shifted more to a neg-
ative value as a part of the decreasing

C trend in the

Kimmeridgian and Tithonian part of the Tegernsee Formation
(Fig. 11). This global trend was interrupted by more negative
spikes at 18.5 (1.4 ‰), or at 29.5 (0.87 ‰). Diagenetic alter-
ation of sediment seems to be the most acceptable interpreta-
tion of these spikes on the

C curve. Transport of limestone

clasts from disintegrated shallower gentle slope environment
of “Ammonitico Rosso” type could evoke input of solutions
with a higher content of light

C isotope during the sediment

lithification.

Detailed correlation between

C and

O isotopes and

magnetic  stratigraphy  between  the  Hlboča  and  Brodno  sec-
tions in the Tithonian—Berriasian boundary interval is also dif-
ficult  due  to  a  stratigraphical  gap  within  the  Hlboča  section,
embracing the uppermost part of the Intermedia Subzone and
the  lower  part  of  the  Alpina  Subzone  (the  uppermost  part  of
the  M20n1n-,  entire  M19r  and  M19n2n  magnetozones)
(Fig. 11). The gap in the isotopic record in the Hlboča section
coincides with a warming trend and elevated values of

C in

the Brodno section (Michalík et al. 2009). Both oxygen and
carbon isotopic values in this part of the Hlboča section were
at least partially modified by diagenesis or were significantly
affected by local sedimentary conditions.

Paleotectonic implications

Paleoinclination of paleomagnetic directions around the J/K

boundary from Central Western Carpathians (PKB and Trans-
danubian Mts) are in good agreement (45—49

°, Table 2)

which indicates a 27—30

°N paleolatitude. The primary Titho-

nian/Berriasian direction from the Hlboča section is counter-
clockwise rotated if compared with the expected European
reference directions by about 50

° (Table 2). Evidence for

counter-clockwise tectonic rotation of Tertiary units in the
Malé Karpaty Mts has been known since the 1990s (Márton et
al. 1992; Kováč & Túnyi 1995). They were documented in the
basal Paleogene sediments in Sološnica and in several locali-
ties in Miocene depressions (Fig. 1b). The rotations were in-

Locality Dc/Ic

k References

Hlboča

307/49 6.1 17.4 This study

Strážovce

338/49 4.0 75.3 Grabowski et al. 2009

Western Tatra

23/47 5.5 499.1 Grabowski 2005

Brodno

236/45 5.6 9.8 Houša et al. 1996

Lókút

270/38 3.6 25.7 Grabowski et al. 2010

European reference direction
Berriasian stratotype

0/47 2.9 15.75 Galbrun 1985

Table 2: Comparison of the Tithonian—Berriasian declinations and
inclinations from the Hlboča section (this study) with coeval direc-
tions from adjacent areas and European reference data. For explana-
tions see Table 1.

324

GRABOWSKI, MICHALÍK, PSZCZÓŁKOWSKI and LINTNEROVÁ

terpreted as the result of tectonic escape of the Central West-
ern Carpathians from the domain of the Alpine collision. The
overall rotation of 40—60

° took place, mostly at the end of the

Early Miocene (Kováč & Túnyi, l.c.). Variegated magnitudes
of Tertiary tectonic rotation in the Malé Karpaty Mts were in-
terpreted as the result of local block rotations in the zones of
ENE—WSW trending dislocations during the Middle Miocene
(Kováč & Túnyi, l.c.). Our data reveal that essentially no rota-
tion occurred between the Tithonian—Berriasian and Eocene in
the area: paleodeclinations for these two time intervals in the
Malé Karpaty Mts are virtually the same (Fig. 1b). In contrast,
a  large  difference  between  Mesozoic  and  Paleogene  declina-
tions exists in the N part of the Central Western Carpathians
(Tatra  Mts  –  Podhale  region,  Grabowski  &  Nemčok  1999;
Márton et al. 1999; Grabowski 2005). Declination difference
amounts  to  90

° (Fig. 1a). The difference in the Strážovske

Vrchy Mts, situated halfway between the Malé Karpaty- and
the Tatra Mts is ca. 75

°, taking into account angular difference

between  primary  magnetization  of  the  Tithonian—Berriasian
strata in the Strážovce section (Grabowski et al. 2009) and Pa-
leogene rocks in the Omastiná locality (Bánovská Kotlina Ba-
sin,  Túnyi  &  Márton  1996).  Our  conclusion  is  that  the
counter-clockwise rotation of Tithonian—Berriasian paleodec-
linations in the Krížna Unit tends to increase westwards along
the strike of the Central Western Carpathians. A similar obser-
vation was reported by Kruczyk et al. (1992) and Pruner et al.
(1998)  who  studied  paleomagnetism  of  Jurassic  rocks  from
different  parts  of  the  Central  Western  Carpathians  (between
Ružbachy and the Malá Fatra Mts).

Conclusions

1. Tithonian magnetozones, from the top of M21n to

M20n1n, embracing the Dobeni to the Intermedia Subzones,
were documented within the uppermost part of the Tegernsee
Formation  in  the  Hlboča  section.  The  magnetostratigraphy
of  the  overlying  Padlá  Voda  Formation  is  not  well  con-
strained  due  to  breccias  and  a  stratigraphic  gap  at  the  J/K
boundary  and  more  intense  remagnetization  of  this  forma-
tion.  Nevertheless,  it  is  assumed  that  sediments  deposited
during the M19r and a large part of the M19n magnetochrons
were mostly eroded. Above the breccia, magnetozones from
the topmost part of M19n to M17n were identifed within the
Padlá Voda Formation.

2. The magnetic susceptibility values of the Berriasian

Padlá  Voda  Formation  are  higher  than  for  the  Tithonian  Te-
gernsee  Formation,  which  differs  from  typical  magnetic  sus-
ceptibility  trends  across  the  J/K  boundary  in  the  Tethyan
region.  The  anomalously  high  magnetic  susceptibility  of  the
Padlá Voda Formation is related to the presence of superpara-
magnetic magnetite, which occurs commonly in remagnetized
carbonates.

3. Primary C isotopic data were preserved in limestones

within  the  Oxfordian—Kimmeridgian  part  of  the  Tegernsee
Formation  with  typically  decreasing  C-isotope  trend.  Data
from the Tithonian part of the Tegernsee Formation probably
reflect “local” basin processes connected with the breccia for-
mation  and/or  with  possible  diagenetic  overprint.  The  C-iso-

tope record of the Berriasian Padlá Voda Formation is more
homogeneous (1.4—1.8 ‰ V-PDB) and assumed to be prima-
ry. Detailed correlation between isotope and magnetic stratig-
raphy of the Tithonian—Berriasian interval between the Hlboča
and Brodno sections is also complex due to a J/K stratigraphic
gap within the Hlboča section.

4. Tithonian-Berriasian paleodeclinations reveal counter-

clockwise rotation of the Vysoká Unit by an amount of ca.
50

°. As the Eocene-Miocene paleodeclinations from the cover

rocks of the area are comparable, the counter-clockwise rota-
tion must have taken place mostly after the Early Miocene
(after Karpatian).

Acknowledgments:  The authors are grateful to D. Reháková
(Bratislava)  for  valuable  discussion  and  inspiring  remarks.
Ing. T. Sztyrak is acknowledged for technical assistance in the
field  and  for  preparation  of  thin  sections.  The  investigations
were  supported  by  the  VEGA  scientific  Grants  0196  and
0388  and  by  the  Polish  Ministry  of  Science  and  Education
(Project 6.14.0005.00.0 of the Polish Geological Institute—Na-
tional Research Institute). The authors wish to thank P. Pruner
and H. Weissert for constructive reviews.

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