GeolCarp_Vol64_No1_39

www.geologicacarpathica.sk

GEOLOGICA CARPATHICA

, FEBRUARY 2013, 64, 1, 39—62 doi: 10.2478/geoca-2013-0003

Introduction

In spite of numerous previous works devoted to the terminal
Triassic sedimentary and biotic evolution, precise dating and
event  successions  during  the  Rhaetian  transgression  have  re-
mained  little  known  since  the  establishment  of  the  “Avicula
contorta Schichten” by Winkler (1859). We selected the Kar-
dolína  section  situated  on  a  steep  western  slope  of  the  Mt
Pálenica (NNE of the Tatranská Kotlina village) in the Belian-
ske Tatry Mts (GPS coordinate 49°14

’997”N: 20°18’894”E,

Figs. 1 and 2) as the most continuous section of the Rhaetian
Fatra  Formation  in  the  former  Zliechov  Basin  (Fatric  Unit),
the  upper  part  of  which  has  been  studied  by  Michalík  et  al.
(2007).  The  sedimentary  record  was  analysed  by  sedimento-
logical, biostratigraphical, geochemical and magnetic suscep-

Paleoenvironments during the Rhaetian transgression and

the colonization history of marine biota in the Fatric Unit

(Western Carpathians)

JOZEF MICHALÍK

, OTÍLIA LINTNEROVÁ

, PATRYCJA WÓJCIK-TABOL

ANDRZEJ GAŹDZICKI

, JACEK GRABOWSKI

, MARIÁN GOLEJ

, VLADIMÍR ŠIMO

and

BARBARA ZAHRADNÍKOVÁ

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

geolmich@savba.sk; geolmgol@savba.sk; geolsimo@savba.sk

Department of Geology and Mineral Deposits, Faculty of Natural Sciences, Comenius University, Mlynská dolina G1, 842 15 Bratislava,

Slovak Republic; lintnerova@fns.uniba.sk

Department of Geological Sciences, Jagiellonian University, Oleandry Str. 2a (room 109), 30-063 Kraków, Poland

Institute of Paleobiology, Polish Academy of Sciences, Twarda 51/55, 00-818 Warszawa, Poland; gazdzick@twarda.pan.pl

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

Slovak National Museum, Natural Science Museum, Vajanského nábrežie 2, P.O.Box 13, 810 06 Bratislava, Slovak Republic;

barbara.zahradnikova@snm.sk

(Manuscript received May 23, 2012; accepted in revised form September 18, 2012)

Abstract: Terminal Triassic environmental changes are characterized by an integrated study of lithology, litho- and
cyclostratigraphy, paleontology, mineralogy, geochemistry and rock magnetism in the Tatra Mts. The Carpathian Keuper
sequence was deposited in an arid environment with only seasonal rivers, temporal lakes and swamps with scarce
vegetation. Combination of a wide range of

O values (—0.7 to + 2.7) with negative

C values documents dolomite

precipitation either from brackish or hypersaline lake water, or its derivation from pore water comparably to the Recent
Coorong B-dolostone. Negative

C values indicate microbial C productivity. Rhaetian transgressive deposits with

restricted Rhaetavicula fauna accumulated in nearshore swamps and lagoons. Associations of foraminifers, bivalves
and sharks in the Zliechov Basin were controlled by physical factors. Bivalve mollusc biostromes were repetitively
destroyed by storms, and temporary firm bottoms were colonized by oysters and burrowers. Subsequent black shale
deposition recorded input of eolian dust. Bottom colonization by pachyodont bivalves, brachiopod and corals started
much later, during highstand conditions. Facies evolution also revealed by geochemical data, C and O isotope curves
reflect eustatic and climatic changes and help reconstruct the evolution of Rhaetian marine carbonate ramp. The Fatra
Formation consists of 100 kyr eccentricity and 40 kyr obliquity cycles; much finer rhythmicity may record monsoon-
like climatic fluctuations. Fluvial and eolian events were indicated by analysis of grain size and content of clastic
quartz, concentrations of foraminiferal (Agathammina) tests in thin laminae indicates marine ingression events. Mag-
netic susceptibility (MS) variations reflect the distribution of authigenic and detrital constituents in the sequence. In-
creasing trend of MS correlates with the regressive Carpathian Keuper sequence and culminates within the bottom part
of the Fatra Formation. Decreasing trend of MS is observed upwards the transgressive deposits of the Fatra Formation.

Key words: uppermost Triassic, Western Tethys, Slovakia, sedimentology, sequence stratigraphy, geochemistry, marine
fauna.

tibility  methods.  Detailed  study  of  cyclostratigraphy  enabled
us to assess periodicity estimate, duration of sedimentary cy-
cles,  and  climate  proxies.  Preservation  of  primary  magnetic
record  is  promising  for  future  detailed  study  of  magneto-
stratigraphy.

Geological setting

Terrigenous Carpathian Keuper was deposited during the

Carnian and Norian on extensive lowlands adjacent to North
Tethyan shelves. Limanowski (1903) interpreted its environ-
ment as a continental domain. Turnau-Morawska (1953) re-
garded variegated shales, sandstones and dolostones as marine

MICHALÍK, LINTNEROVÁ, WÓJCIK-TABOL, GAŹDZICKI, GRABOWSKI, GOLEJ, ŠIMO and ZAHRADNÍKOVÁ

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GEOLOGICA CARPATHICA, 2013, 64, 1, 39—62

Fig. 2. Rocky outcrop above the Kardolína gamekeeper’s cottage on
the western slope of Mt Pálenica. Right corner: contact of the Car-
pathian Keuper with the Fatra Formation.

sediments with fluvial intercalations. Borza (1959) postulated
a  primary  character  of  Keuper  dolostones.  Gaździcki  et  al.
(1979)  recognized  three  informal  members  in  the  sequence:
the  basal  member  with  clastic  intercalations,  the  middle  one

Fig. 1. Location of the Kardolína section on the slope of Mt Len-
dacká Pálenica near Tatranská Kotlina in the Belianske Tatry Mts.

with prevalence of variegated claystones and the upper mem-
ber,  that  consists  of  claystone/dolostone  alternation.  They
stressed the terrigenous nature of the palynoflora in the clay-
stones  (Gliscopollis/Classopollis  assemblage),  whereas  the
dolostone  intercalations  yielded  more  diversified  associa-
tions of pollen, spores and marine acritarchs. Al-Juboury &
Ďurovič  (1992,  1996)  supposed  hypersaline  conditions  of
the Keuper dolomite formation. Rychliński (2008) and Jaglarz
(2010)  distinguished  several  depositional  environments:
mudflats,  fluvial,  sabkha,  and  flat  marine,  evolving  under
fluctuating wet – semi-arid and arid climate.

During the latest Triassic, dry emerged plains were inun-

dated by shallow sea flooding the opening tensional depres-
sions  (Michalík  1993).  Transgression  was  not  a  short  and
uniform event. Instead, sea reached different parts of the area
in  several  pulses  (Gaździcki  &  Iwanow  1983).  Bioclastic,
shelly,  and  oolitic  limestones,  marlstones,  dolostones  and
marls were laid down in salt marshes, littoral banks, carbon-
ate  ramps,  up  to  deeper  neritic  slope  of  the  almost  300 km
long and 100 km wide tensional semi-closed shallow marine
basin  (the  Fatric  Zone  of  the  central  Western  Carpathians;
Michalík  1977;  Michalík  et  al.  2007).  The  carbonate  ramp
faced a deeper, dysoxic basin.

The new biotope created by the Rhaetian marine transgres-

sion  was  colonized  by  pioneer  organisms  (foraminifers,  bi-
valves  and  fish).  The  Kardolína  section  is  more  suitable  for
detailed study of this process than other less complete sections
in the Fatric Unit (Michalík 1977, 1979, 1982; Michalík et al.
2007).  Benthic  associations  were  dominated  by  bivalves
Placunopsis  alpina  (Winkler)  and  Rhaetavicula  contorta
(Portlock), gastropods, and foraminifers Agathammina austro-
alpina  Kristan-Tollmann  &  Tollmann  (Michalík  &  Jendrejá-
ková  1978;  Michalík  1978a).  Upper  Triassic  bivalve  faunas
have been studied by Allasinaz (1972), Kollárová-Andrusovová
&  Kochanová  (1973),  Hallam  (1981),  Golebiowski  (1991),
Ivimey-Cook  et  al.  (1999)  and  Hautmann  (2001).  Fish  re-
mains  (single  shark  and  actinopterygian  teeth  and  scales)
were  reported  by  Gaździcki  (1974),  Duffin  &  Gaździcki
(1977),  Michalík  (1977,  1979),  and  by  Gaździcki  et  al.
(1979). More mature communities were represented by bra-
chiopods Rhaetina gregaria (Suess), Zugmayerella uncinata
(Schafhäutl), Austrirhynchia cornigera (Suess) – (Michalík
1975, 1978b, 1980); foraminifers Aulotortus friedli (Kristan-
Tollmann), Glomospirella pokornyi (Salaj), Triasina hantkeni
Majzon  –  (Gaździcki  1983);  and/or  by  corals  Retiophyllia
paraclathrata  Roniewicz,  Rhaetiastraea  tatrica  Roniewicz,
etc. – (Roniewicz & Michalík 1998); sponges, algae and hy-
drozoans inhabiting the carbonate ramp. However, evolution
of  any  true  reef  bio-constructions  was  prevented  by  storms
and  sea-level  fluctuations  (Michalík  1980,  1982).  The  pa-
lynofacies characterized by Ricciisporites tuberculatus Lund-
blad was dominated by terrestrial components and by a high
amount of phytoclasts. Its marine fraction dominated by the
dinoflagellate cyst Rhaetogonyaulax rhaetica Sarjeant points
to a very shallow marine depositional environment (Götz in
Michalík et al. 2007). Microflora from the upper part of the
Fatra Formation resembles associations of the Ricciisporites
tuberculatus  Zone  of  the  Polish  zonation  and  of  the  Ricci-
isporites—Polydiisporites  Zone  of  the  SE  North  Sea  Basin,

RHAETIAN TRANSGRESSION AND MARINE BIOTA COLONIZATION IN THE FATRIC UNIT PALEOENVIRONMENTS

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GEOLOGICA CARPATHICA, 2013, 64, 1, 39—62

both indicating middle to late Rhaetian age (Ruckwied &
Götz 2009).

Material and methods

In the well exposed, 122 m thick Kardolína section, we

concentrated on its lower part (69 m, Fig. 3), where 42 dolo-
stone and 103 limestone layers were distinguished and num-
bered. Basal beds of the Fatra Formation were designated as
the “zero interval” (however, later, it was proved that the up-
permost layers of the Carpathian Keuper bear signs of marine
origin  and  the  Bed —5  consists  of  first  limestone  biomicrite).
Samples  were  taken  by  the  bed  by  bed  method,  but  thicker
layers were sampled more densely. The Carpathian Keuper se-
quence  was  numbered  downwards,  thus  in  opposite  order  to
the Fatra Formation, but with a “minus” mark.

From each sample, a thin section has been made for micro-

scopic  study.  Allochem  contents  were  evaluated  from  per-
centages obtained under an optical microscope both with use
of  estimation  tables  (Bacelle  &  Bosellini  1965;  Schäfer
1969;  Soudant  1972;  Michalík  et  al.  2007),  and  of  the
NICON  NIS-Elements  BR  System  for  screen  analysis.  Mi-
crite, sparite, bioclast and lithic clast contents, as well as the
average size of clastic quartz grains were measured (Fig. 4).

Micrite and sparite were compared as antagonistic elements
(as the Reijmer 1968) in Fig. 5.

Total abundance of major oxides, several trace elements,

and REE were analysed in the ACME Analytical Laborato-
ries,  Ltd  in  Vancouver,  Canada,  in  12  samples.  REE  were
normalized  to  the  Post-Archaean  Australian  Shale = PAAS
(Taylor & McLennan 1985). The Eu/Eu* ratios (Eu anomaly
values)  were  calculated  using  Eu

PAAS

/Sm

PAAS

)

0.5

ratio. The inter-elemental relationship has been evaluated us-
ing the Pearson’s Correlation Factor.

The total organic carbon content (TOC) and total inorganic

carbon content (TIC) was measured on C-MAT 5500
Ströhlein device in the laboratory of the Geological Institute
of the Slovak Academy of Sciences in Banská Bystrica. TIC
content was re-calculated on the content of CaCO

in 35 se-

lected samples.

O and C isotope ratios were analysed in 65 samples in CO

after the standard dissolution of samples in 100% phosphoric
acid on the Finigan MAT-2 Mass Spectrometer in the labora-
tories of both the Czech Geological Institute in Prague and the
Institute of Paleobiology of the Polish Academy of Sciences
in Warsaw. The results are presented in standard delta nota-
tion ( ) in permil (‰) relative to the Vienna International Iso-
topic Standard (VPDB) with 0.01‰ accuracy.

The carbon isotope ratio of C

org

was analysed after carbon-

ate dissolution in 8 samples enriched to TOC. The

C mea-

surements  were  performed  in  the  Czech  Geological  Survey
Laboratory  in  Prague  by  flash  combustion  in  a  Fisons  1108
Elemental Analyzer coupled with Mat 251 Isotope Ratio Mass
Spectrometer  in  a  continuous  flow  regime.  The  sample  size
was adjusted to contain a sufficient amount of C

org

to obtain

external reproducibility of 0.15 ‰ for

org

for all types of

samples with NBS22 as the reference material. Isotope data
are reported in the usual delta ( ) notation relative to VPDB.

Foraminiferal tests were studied in thin sections by optical

microscope. Bivalve molluscs were prepared mechanically by
vibro-tool, they were coated with ammonium chloride prior to
photographying.  Shark  teeth  were  collected  mainly  from  the
upper part of Beds 2.2 and 2.3, single fish teeth and vertebrae
from insoluble residue after dissolving samples 2.3, 3.4, 13/14
and  14  in  diluted  acetic  acid.  Descriptive  terminology  of
Chondrichthyes  is  based  on  Cappetta  (1987)  and  fish  termi-
nology is based on Swift & Martill (1999). The shark and fish
teeth are housed in the Natural Science Museum in Bratislava.
Tooth photographs were taken by JSM-6390 (JEOL) scanning
electron microscope in the Banská Bystrica Department of the
SAS Geological Institute and in the State Geological Institute
of Dionýz Štúr in Bratislava.

Magnetic susceptibility (MS) and rock magnetic studies

were performed in the Paleomagnetic Laboratory of the Polish
Geological  Institute—National  Research  Institute  in  Warsaw.
MS was measured in 143 samples using KLY-2 kappabridge
(AGICO  Brno,  frequency  0.92 kHz),  and  normalized  for
mass.  Rock  magnetic  experiments  on  pilot  collection  of  22
specimens  included  measurements  of  MS  in  low  (0.47 kHz)
and  high  (4.7 kHz)  frequency  using  a  Bartington  MS2  sus-
ceptibility meter (to evaluate the contribution of  the very fine
magnetic  fraction  close  to  superparamagnetic  state),  isother-
mal remanent magnetization (IRM) applied in the field of IT,

Fig. 3. Lower part of the Fatra Formation in the Kardolína section
formed by the “tempestite cycle” (Beds 3 to 10). Right lower cor-
ner: the Bed 4 with loadcasts on the base.

MICHALÍK, LINTNEROVÁ, WÓJCIK-TABOL, GAŹDZICKI, GRABOWSKI, GOLEJ, ŠIMO and ZAHRADNÍKOVÁ

GEOLOGICA CARPATHICA

GEOLOGICA CARPATHICA, 2013, 64, 1, 39—62

and then antiparallel in the 100 mT field, by means of
MMPM1 pulse magnetizer. S-ratio, calculated as a ratio of
IRM intensities applied in both fields was indicative for rela-
tive proportions of low and high coercivity minerals.

Results

Lithology and fossils

The Carpathian Keuper

Two of the three informal members recognized by

Michalík (1977) in the Carpathian Keuper sequence, namely
the  “lower  clastics”  and  the  “main  claystone”  are  covered
below  the  scree  (Rychliński  2008).  The  thirty  meters  thick
sequence of mixed terrigenous, lacustrine, fluvial and eolian
variegated greenish and violet-red dolomitic claystones with
occasional intercalations of pale greenish-grey clayey dolos-
tone, exposed in the Kardolína section, represents the upper-
most  part  of  the  Carpathian  Keuper  (“upper  dolomite
member” of Michalík, l.c.). Bedding planes of rusty weather-
ing  pale  greenish-grey  dolomicrite  layers  (20  to  130 cm
thick) sometimes bear ripple marks. Interbeds of yellow-, vio-
let-,  or  dark  grey  claystone  may  attain  thickness  of  20  to
160 cm, but sometimes they are only few centimeters thick.

“Unit I” is typical of thinning- and fining upwards ar-

chitecture (65 to 20 cm). Grey biomicrite with raised CaCO

content  (Beds —43  to  —41)  contains  dispersed  quartz  grains
(0.005 to 0.2 mm in diameter; Fig. 4) and numerous ostracod
tests (3 to 10 %; Fig. 5). Higher up (in Beds —40 to —38) the
dolomicrosparite  content  increases  (to  9 %),  and  fragments
of  plants  become  abundant.  Dolostone  layers  are  followed
by a 330 cm thick brown claystone interval.

Dolomicrite layers (14 to 65 cm thick) of the “unit II”

of lumpy texture contain dispersed tiny dolomite crystal nu-
clei  becoming  abundant  upwards,  where  dolomicrosparite
and  even  dolosparite  prevails.  Claystone  interbeds  are  2  to
60 cm thick. Grey claystone lense in basal part (interbed be-
tween  Beds —35  and  —34)  contains  rich  and  relatively  large
carbonized fragments of plants.

“Unit III” forms an eminent rock step of thick (20 to

130 cm)  dolostone  layers.  Dolomicrosparite  on  the  base
(Bed —23) contains small plant fragments. Dolomicrite beds
(Beds —22 to —16) are of lumpy structure, with an admixture of
eolian  quartz  silt  (0.02 mm),  larger  quartz  grains  (0.04  to
0.05 mm)  are  rare,  tiny  plant  fragments  occur  occasionally.
Dolomicrosparite beds (Beds —15 to —11) contain sparry crys-
tallites, dolomicrite occurs in irregular nests and lumps. Lumps,
pellets, phytoclasts and tiny shell fragments occur in dolomi-
crite in the upper part (Beds —10 to —6). Biodetritus (ostracods,
foraminifers, bivalve shell fragments, fish teeth and scales) be-
come frequent in the uppermost layers (Beds —7 and —6).

The Fatra Formation

The Fatra Formation attains a thickness of 96 m here, in

contrast to other places where it does not exceed 25 to 53
meters. Michalík (1978), Michalík et al. (1979), Gaździcki et

al. (1979) divided the sequence into two biostromal members,
separated from each other by a “barren interval”, from the un-
derlying Carpathian Keuper by “basal beds”, and from the
overlying Kopieniec Formation by “transitional beds”. How-
ever, detailed study of the Kardolína section shows that the ar-
chitecture of the Fatra Formation is much more complex.

Transgressional “unit IV” (Figs. 4—5): Each of five

palustrine  (shallowing  upwards)  cycles  (Beds —5  to  2.3;
Fig. 5) starts with grey dolostone or even with dark organo-
detrital  limestone  and  intercalation  of  dark  brown  to  black-
grey shale. The sequence was reduced by condensation and
resedimentation  (pale  dolostone  clasts  dispersed  in  clayey
matrix, dark crusts, erosion on bed surfaces).

Dark to black-grey argillites (70—120 cm thick) contain

small  pieces  of  carbonized  wood,  ooids,  bone  fragments,
shark teeth, linguloid brachiopods, bivalves and black inter-
layers  of  laminated  bituminous  argillitic  lime  dolostone.
Wavy  (flaser)  and  parallel  lamination  appears  in  dolostone
intercalations  in  the  middle  of  black  shales.  Black  ferrugi-
nous/phosphate crusts enriched by dispersed tiny rock clasts,
fish  teeth  and  bone  fragments  occur  on  upper  bedding
planes.

Fine clastic laminae in Beds —4, —3 and in the “zero beds”

(0.1 to 0.8) contain numerous foraminiferal tests (Agatham-
mina austroalpina Kristan-Tollmann & Tollmann; Figs. 4
and 6a—b; 15 to 60 in one thin section), indicating deposition
in a low-energy environment, most likely on tidal flats.

U-shaped spreiten-burrows (with diameter of 35 to

40 mm)  of  Rhizocorallium  jenense  Zenker,  parallel  or  ob-
lique  to  bedding  plane  occur  on  the  base  of  the  dark  marl-
stones  of  Bed 0.2  (Fig. 6c).  Their  limbs  are  more-or-less
parallel.  The  tube  ornamented  by  scratchy  bioglyphes  is
5 mm wide, its length is greater than 150 mm. Spreite lamel-
lae of coarser sediment with rounded litho- and bioclasts (1 to
2 mm) usually attain diameters of > 1 : 5 .

The oldest bivalve molluscs (Modiolus minutus Lamarck)

appear in the Bed —3.2. Higher levels of the “zero beds” (0.3
and 0.4) contain more diverse bivalve fauna: Bakevellia
praecursor (Quenstedt), Isocyprina ewaldi (Bornemann),
Modiolus minutus, Neoschizodus? sp., Pleuromya? sp.

The yellowish weathering fine-organodetrital limestone

layer (Bed 1) contains a lot of broken shells correlatable with
water  turbulence,  rather  than  with  micrite  content.  Clastic
quartz  grains  are  rare  and  rather  small,  bearing  signs  of
wind-  not  of  riverine  transport.  Biodetrital  limestone  is  fol-
lowed  by  brown  claystone  intercalated  by  dolostone  layers
with  bone-bed  type  surfaces.  Condensation  occurs  near  the
top  of  individual  layers,  sometimes  connected  with  enrich-
ment  of  phosphatic  matter,  fine  breccia  and  teeth  and  bone
fragments (“bonebeds” 2.1 and 2.2; Fig. 7).

A shark tooth of Hybodus minor Agassiz and another 23

teeth  belonging  to  Lissodus  minimus  Agassiz  were  collected
in Beds 0.4 and 2.1. The symmetrical tooth of the first species
is  1.5 mm  high.  High,  upright  central  cusp  flanked  by  up  to
four pairs of lateral cusplets with fairly wide base is lingually
inclined in lateral view. Fairly coarse vertical ridges descend
cusps from apices, occasionally bifurcate basally. Lateral cut-
ting edges of cusps are sharp. Shallow root lingually projects
in  so-called  “lingual  torus”,  roughly  semicircular  in  basal

MICHALÍK, LINTNEROVÁ, WÓJCIK-TABOL, GAŹDZICKI, GRABOWSKI, GOLEJ, ŠIMO and ZAHRADNÍKOVÁ

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GEOLOGICA CARPATHICA, 2013, 64, 1, 39—62

is very shallow, bearing a longitudinal row of tiny vascular fo-
ramina. Labial face of root is concave, containing much larger,
randomly distributed foramina in its lower portion.

Fish are represented by four molariform and incisiform

teeth of Sargodon tomicus Plieninger (Fig. 7) and conical
teeth of Severnichthys acuminatus (Agassiz), a “primitive”
basal actinopterygians. Two tooth types are recognized within
the latter species, each of which has previously been assigned
to a separate taxon: “Birgeria acuminatus” type (4 teeth) and
“Saurichthys longidens” type (2 teeth).

Tempestite “unit V”. This four and half meters thick

limestone  sequence  (Beds 3—7)  consists  of  bedded  (10—
30 cm)  grey  biomicrites  to  calcarenites  with  wavy  bedding
planes.  They  contain  frequent  mollusc  and  brachiopod
shells, sometimes with distorted geopetal fillings. Loadcasts
and  erosional  marks  on  the  layer  bases,  and  gradation  of
clasts occur frequently, indicating origin in distal tempestite
lobes  laid  on  a  soft  marly  bottom.  Intensive  storm  activity
seems to be a typical feature of the environment during sedi-
mentation of this cycle.

Between loadcasts, deformed tubular bodies with typical

Y-shaped structure and ramification attributable to Thalassi-
noides sp. occur. These traces were produced by crustaceans
(Bromley 1996) indicating omission surfaces due to sudden
erosive events (Mikuláš 2006).

Foraminiferal diversity increases upwards (Aulotortus friedli,

Aulotortus,  Frondicularia,  Planinvoluta,  Ophthalmidium,
Nodosaria).  They  are  accompanied  by  other  marine  organ-
isms  (Aciculella,  Theelia,  solenoporaceans,  ostracods).  The
first brachiopods appear in Bed 5.4.

The preservation of originally aragonite shells (recrystal-

lized or as internal or composite moulds) of four bivalve as-
sociations recognized within this cycle proves that the fossil
record was not depleted and it represents the original compo-
sition.

a. The Rhaetavicula contorta association (Bed 2.3; Figs. 8,

9,  11c)  characterized  by  dominance  of  epifaunal  byssate-
(46 %), semi-infaunal byssate- (30 %) and cementing bivalve
types  (18 %)  is  composed  of  suspension  feeders.  Pectenids
like Propeamussium  (Parvamussium)  schafhaeutli  (Stur)  and
Chlamys mayeri (Winkler) were present among these first bi-
valve colonizers. Right valves of Rhaetavicula contorta (Port-
lock) occur rarely (Fig. 8; similarly to statements of Pflücker
& Rico 1868; Cox 1961; Ivimey-Cook et al. 1999). Relatively
small shell size and lack of infaunal molluscs points to nutri-
ent-poor  and  dysoxic  substrate,  their  preservation  (left  and
right valves together, no fragmentation but post-mortem disar-
ticulation  only)  indicates  low  water  energy  above  a  soft  but
stable  substrate.  A  possible  epifaunal  character  of  these  ani-
mals attached to sea plants can be considered, too.

The mixed Rhaetavicula contorta and “Placunopsis” alpina

association (Bed 4; Fig. 8; 34 % of byssate epifauna, 25 % of
byssate  semi-infauna)  reflects  diversification  within  a  quiet,
nutrient poor environment on a firm and stable substrate in a
carbonate  regime.  Increase  of  cementing  bivalves  (“Pla-
cunopsis”  alpina:  up  to  30 %)  could  have  been  associated
with a firmer substrate (abundant bioclasts, shell fragments).

b. The tempestite coquina of 5.1 Bed contains accumula-

tions of large dissarticulated convex down (both right and left)

Gervillaria inflata (Schafhäutl) and “Permophorus” elongates
(Moore) valves with soft body imprints (Figs. 8—10, 11b). The
association is composed of byssate semi-infauna (50 %), shal-
low  infauna,  mobile-  (34 %),  or  byssate  epifauna  (14 %),
which, with the exception of one detritus eater (Nuculana sp.),
were suspension feeders. This fact indicates a firm and stable
substrate in a high energy environment, supplied with food in
suspension.  Despite  reworking  and  mixing,  right  and  left
valve  ratio  does  not  indicate  any  significant  sorting  (Fig. 9).
Shell accumulation of the “Corbula” alpina association domi-
nated by shallow infaunal suspension feeders (93 %) occur at
the  base  of  Bed 7b  (Figs. 9,  10).  The  composition  of  this
storm  shell  accumulation  is  identical  to  that  of  soft-bottom
bivalve  association  of  the  underlying  marlstone.  Lack  of
epifauna  could  be  associated  with  the  scarcity  of  attachment
opportunities. On the upper bedding plane of this bed, clusters
of  Rhaetavicula  contorta,  rarely  of  Modiolus  minutus  occur.
Shallow  infaunal  suspension  feeders  are  dominant  (96 %)  in
the association from the Bed 9.3 (Fig. 11). This 1.5 cm thick
accumulation  resembles  that  of  the  Bed 7b.  However,  while
the former association occurs on the tempestite base, the latter
one is situated in the upper part of the bed as a result of ero-
sion  of  fine  mud  by  bottom  currents.  Convex-up  and  down
and  also  articulated  shells  occur.  The  underlying  marlstone
contains the same species composition which indicates condi-
tions similar to Bed 7b.

c. Sorting due to storm activity formed temporary firm sub-

strate  for  cementing  larvae  of  “Placunopsis”  alpina,  of  large
Plicatula sp. and of attached Atreta intusstriata forming shell
accumulation (Figs. 8—11a). Epifaunal cementing bivalves are
dominant  (65 %)  in  this  association  (Beds 5.1v,  and  8b;
Fig. 9), followed by epifaunal byssate (30 %) and semi-infau-
nal byssate bivalves (10 %). In spite of some redeposition, bi-
valve  composition  indicates  a  firm  and  stable  substrate.  The
“Placunopsis” alpina shells are exclusively left upper valves.
While Triassic “Placunopsis” shells cemented to the substrate
(Seilacher  1954;  Hölder  1990;  Hautmann  2001),  Jurassic
forms attributed to different taxa were byssus-attached (Todd
& Palmer 2002). Secondary texture patterns (Fig. 8a,b) devel-
oped on left valves copying the surface of the substrate of their
right  valves.  However,  the  texture  resembles  radially  ribbed
bivalves, which are not common in the association (although
Paleocardita austriaca could be one possible candidate).

d. The Propeamussium (Parvamussium) schafhaeutli and

Entolium  sp.  association  (Bed 10;  Fig. 9)  is  dominated
(42 %) by epifaunal byssate pectinid bivalves (Entolium sp.
and  Chlamys  mayeri).  Epifaunal  free-lying/vagile  morpho-
type  is  represented  by  radially  ornamented  left  valves  of
Propeamussium  (Parvamussium)  schafhaeutli  (32 %)  only.
No  right  (smooth  and  thin-shelled)  valves  were  found,  al-
though both equally smooth and thin valves of Entolium sp.
are common. Microstructure of both species shows aragonite
shell mineralogy. Long exposure before their burial could be
indicated by common cementing of Atreta richthofeni on both
outer  and  inner  surfaces.  Hence,  less  resistant  right  valves
were broken and dissolved. The association lived on a stable
detrital  substrate  with  medium  water  energy  near  the  maxi-
mum storm wave base. Protected shelters under empty bivalve
shells were often inhabited by ostracod populations (Fig. 12).

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GEOLOGICA CARPATHICA, 2013, 64, 1, 39—62

Fig. 11. Graphic reconstructions of three Rhaetian bivalve assem-
blages from the lowermost part of the Fatra Formation, Kardolína
section. a – “Placunopsis” alpina assemblage, Bed 5.1v; b – Rhae-
tavicula contorta assemblage, Beds 2.3 and 4; c – “Corbula” alpina
assemblage, Bed 5.1.

Fig. 12. Valve of Placunopsis alpina with cluster of ostracods im-
mediately inside. Scale bar is equal to 10 mm.

arranged in longitudinal rows on both upper and lower jaws,
with the smallest teeth in front and at sides of dentitional pave-
ment. Incisiform teeth up to 14 mm long comprise chisel-like
crown surmounting a deep root. Lingual face of crown is di-
vided into two by a wear facet in centre produced by func-
tional ante-mortem contact abrasion. As in all bifid crowns,
highest cusp is located closest to midline of mouth. Incisiform

teeth were used to pluck bivalves from the substrate, and the
battery of molariform teeth provided an effective mill for
breaking their shells (Swift & Martill 1999). Teeth of Birgeria
acuminata (Agassiz) were found between Beds 13 and 14.

“Unit VII”. The seventh unit is about 10 m thick; it

starts with sandy organodetrital limestone (Beds 15 and 16)
with  nodular  appearance  (flaser  texture).  Intercalations  of
black  marls  are  rich  in  coprolites,  fish  teeth,  pectenids  and
other  bivalve  shells,  and  crinoids.  Layer 19  contains  large
megalontid  bivalve  shells.  Higher  up,  the  clay  content  in-
creases.

“Unit VIII”. Thick-bedded limestones (Beds 20—24)

contain debris of corals transported down the submarine
slope. Other organic fragments (bivalve shells, crinoids, oss-
icles) are less frequent. Intercalations of grey marl with bra-
chiopods Rhaetina gregaria (Suess) in situ appear in the
upper part of this unit.

“Unit IX”. The ninth unit starts with detrital lime-

stone. Thick algal dololaminite layer (Bed 29) preserved fine
record of dolostone rhythms. Marls increase in the higher
part of the thinning upwards cycle.

“Unit X”. The tenth unit consists of thick-bedded fine

organodetrital limestones of slope facies. This lithology
records the start of a general deepening of the basin.

Magnetic susceptibility and rock magnetic properties

MS values are moderately high for carbonate rocks, mostly

in the range between 5 and 20 10

—8

/kg, with a single

maximum above 30 10

—8

/kg (Fig. 4). An increasing trend

was observed from the bottom (Carpathian Keuper facies) up
to the middle part of the section, with maximum values in

MICHALÍK, LINTNEROVÁ, WÓJCIK-TABOL, GAŹDZICKI, GRABOWSKI, GOLEJ, ŠIMO and ZAHRADNÍKOVÁ

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GEOLOGICA CARPATHICA, 2013, 64, 1, 39—62

the  lower  part  of  the  Fatra  Formation,  at  the  bottom  of  the
VI-th cycle (Fig. 4), followed by a decreasing trend in the up-
per part of the Fatra Formation. All pilot samples studied re-
vealed significant MS frequency dependence (Fig. 13a) which
accounts for contribution of ultrafine magnetic particles, close
to superparamagnetic to single domain state to MS (Forster et
al. 1994; Grabowski et al. 2009). As there is also a very good
correlation between MS and IRM intensity acquired in the 1 T
field (Fig. 13b), it is necessary to conclude, that MS is based
mostly on ferromagnetic minerals. Magnetite seems to be the
most important magnetic, as inferred from predominantly low
coercivities  –  samples  are  almost  saturated  in  the  field  of
300 mT (Fig. 13c) and maximum unblocking temperatures of
low and medium coercivity fraction (0.1 T and 0.4 T respec-
tively;  Fig. 13d)  between  500  and  550 °C.  Subordinate
amounts of hematite occur as well, as is indicated by slightly
increasing IRM intensity above 500 mT (Fig. 13c), and max-
imum  unblocking  temperatures  around  650 °C  for  the  high
coercivity (1.4 T) fraction (Fig. 13d).

Geochemistry

Major elements

Total rock analyses of 12 samples were performed (Ta-

ble 1) in order to obtain a more precise idea of the origin of
the source material and to determine chemical changes po-
tentially forced by hydrological, climatic and other factors.
The chemical composition of the samples is given mainly by
the proportion of carbonate (represented by CaO, MgO) and
silicates (represented by SiO

, Al

; Table 1). The dolomite

non-carbonate content is higher (approximately 20 to 30 %)
than in limestones (approximately 5 to 15 %; Fig. 16). Sam-
ples —34, —3.2 and 14 can be designated as argillites, as their
carbonate content is low ( < 5 to about 30 %; Fig. 6).

The composition of major elements in argillites is close to

the Post-Archean Australian Shale (PAAS) composition and
could indicate that (weathered) felsic rocks were the proba-
ble  source  of  our  sediments  (German  et  al.  1991;  Condie
1993; Bau & Dulski 1996). These characteristics are in line
with the mineral composition of samples analysed. Illite with
only very low content of smectite dominates in the clay size
fraction of samples 32, —3.2, 14, 19G. The clay composition
of  samples  both  from  the  Carpathian  Keuper  or  from  the
Fatra  Formation  is  almost  identical  (Biroň  in  the  Środoń  et
al. 2006, or in Michalík et al. 2010).

In spite of relatively low values, P

, MnO, and S

tot

con-

tents are higher in the Fatra Formation limestone than in the
Carpathian Keuper dolostone: they document a shift in sedi-
mentary and diagenetic conditions associated with marine
transgression. P

enrichment was probably related to in-

creased bioproductivity in the marine basin indicated by
bonebed occurrence.

Trace elements and REE

Low silicate admixture complicates the interpretation of

large ion lithophile elements (LILE: Rb, Cs, Ba), with the ex-
ception of Sr. The LILE substituting K are accumulated in the

phyllosilicates in both parts of the sequence. High Sr content
in carbonate (495—861 ppm) in comparison with the argillites
(135—228 ppm) and high correlation of Sr vs. Ca (r  > 0.9) doc-
uments Ca vs. Sr substitution, typical of biogenic aragonite or
of a phase precipitated from evaporated marine water or brine
(Rosen  et  al.  1989;  Garcia  del  Cura  et  al.  2001;  Korte  et  al.
2005).  Carpathian  Keuper  dolostones  are  enriched  in  Sr  but
more depleted in total sulphur (S

tot

~ 0.02 %) than limestones

(0.02 to 0.55 %) of the Fatra Formation (Table 1). In accor-
dance with the facies scheme presented, it is possible that do-
lomite comes from the sulphate-free fluvial/lacustrine waters
(Warren 2000; Garcia del Cura et al. 2001 and their references).
However, low S content could result from diagenetic leaching
of sulphate. By analogy, higher S

tot

content and pyrite grains

observed in thin sections of limestone document a marine-water
environment. Framboidal aggregates represent a typical dia-
genetic pattern of pyrite: they indicate more O-depleted dia-
genetic conditions than those of limestone accumulation. Low
C

org

content was connected with balanced productivity and, lo-

cally, with higher input of terrestrial organic debris, as indicated
by the quality of the organic matter and by C-isotope analyses.

The compositional pattern between the incompatible ele-

ments Th and Y and the compatible Sc, Cr, V and Ni indicates
that the sediment is more likely to have originated from a fel-
sic than from a mafic source (Fig. 14; Table 1). Incompati-
bility of Th and Y results in their higher concentration in well
differentiated felsic rocks (Condie 1993; Cullers 2000). The
Th/Sc ratios are generally similar to the ratio reported for the
PAAS (0.91). The Y/Ni ratios of sediment studied are higher
than these of the PAAS (0.49). In spite of high Cr/Th and Cr/V
ratios (PAAS = 7.53; 0.73 respectively), the samples are closer
to the felsic source and point to local enrichment of Cr-miner-
als rather than to origin from a mafic source. This conclusion
fits with the interpretation of major elements and with mineral
composition.

The total rare earth elements (TREE) contents in the argillite

samples are similar to those of PAAS (Condie 1993; Cullers
2000). The samples —32 and 14 display flat PAAS-normalized
REE  pattern  with  little  depletion  of  heavy  REE  (HREE;
Fig. 15).  The  sample  —3.2  (IV-th  cycle)  reveals  weak  HREE
enrichment  expressed  by  ratios  Gd

/Yb

= 0.8 and La

=0.69. All three samples show weak negative Eu anomaly

(Eu/Eu* = 0.82, 0.77 and 0.94; Table 1) whereas Ce/Ce* ratios
are close to unity and record very weak negative Ce anomaly.

Dolostones of the Carpathian Keuper are depleted of REE

relative  to  PAAS  (0.2  to  0.4)  and  show  slight  positive  Eu
anomaly  (Fig. 15;  Table 1).  Fatra  Formation  limestones  are
depleted relatively to PAAS but the elements from Sm to Ho
(middle  –  MREE;  Ounis  et  al.  2008)  relatively  increased  to
0.5—0.6 content of PAAS. The Eu values reach PAAS level and
show positive Eu anomaly. Increased content of the MREE doc-
uments  different  fractionation  of  REE  in  the  Fatra  Formation
limestones  in  comparison  with  the  Carpathian  Keuper  dolos-
tones and can be interpreted in line with sedimentary evolution.

C and O isotopes

The results of C-isotopic analyses indicate two individual

terrestrial vs. marine sources of organic matter. Less negative

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GEOLOGICA CARPATHICA, 2013, 64, 1, 39—62

Element Unit

Beds

25.1 19.1 14

10.3 5.5 2.3A 0.8 –3.2 –22

–15

–23

–34

SiO

3.43 5.51 53.35 8.61 9.19 11.90 6.60 56.1 17.07 14.47 20.90 62.54

0.87 0.97 13.30 1.32 2.26 2.84 1.70 16.67 5.36 5.95 3.63 15.58

1.12 1.97 4.92 2.07 2.34 2.70 0.45 4.72 2.05 2.05 2.71 1.80

MgO

1.42 1.63 1.98 1.05 1.66 1.52 1.30 1.97 9.37 14.34 16.09 3.07

CaO

51.02 49.39 9.44 47.76 45.42 43.51 48.39 4.01 28.26 23.22 21.51 2.28

0.07 0.11 0.7 0.17 0.15 0.06 0.4 0.18 0.12 0.18 0.06 0.43

0.1 0.14 2.41 0.15 0.39 0.31 0.22 4.10 1.35 1.81 0.23 4.37

TiO

0.04 0.04 0.74 0.07 0.12 0.11 0.07 0.94 0.27 0.23 0.13 1.01

0.01 0.08 0.06 0.19 0.11 0.08 0.02 0.12 0.02 0.04 0.03 0.12

MnO

0.04 0.08 0.04 0.14 0.09 0.17 0.05 0.08 0.05 0.05 0.08 0.02

tot

0.21 0.55 0.02 0.41 0.30 0.13 0.03 0.02 0.02 0.07 0.02 0.00

LOI

41.8 40

12.9 38.4 37.7 36.7 40.7 10.9 35.8 37.3 34.3 8.60

ppm

165

259

214

108

218

ppm

0.8 3.5 9.5 2.7 4.2 2.0 <0.2 38.8 2.6 3.7 5.9 6.4

ppm

0.2 0.4 7.3 0.3 0.9 0.7 0.4 8.5 2.4 3.5 0.4 7.2

ppm

< d.l.

< d.l. 108.8

< d.l. 95.2 13.6 20.4 142.8 40.8 40.8 27.2 122.4

ppm

0.2 0.3 8.3 0.4 1.0 0.4 0.3 9.6 1.3 1.1 0.7 9.5

ppm

0.7 0.9 15.9 1.4 2.4 2.1 1.6 22.3 5.6 4.7 2.5 20.7

ppm

5.4 9.5 26.9 7.1 9.5 9.4 1.5 106.4 11.9 12.1 32.7 14.7

ppm

3.8 5.7 109.1 5.7 15.5 12.7 7.3 180.8 57.2 77.5 9.4 174

ppm

0.9 2

ppm

711

530

229

689

532

494

582

119

861

430

547

136

ppm

0.6 2.1 12.1 1.6 2.4 2.2 1.1 17.7 4.3 3.9 2.3 18.4

ppm

1.3 0.7 2.5 1.7 1.4 0.9 3.2 12

1.5 1.4 9

ppm

111

127

104

ppm

6.9 13.8 298.9 15.9 34

16.2 11.1 354.1 51.8 36.3 23.3 320.1

ppm

3.8 11.6 27.4 11

13.9 14.9 5.2 24.5 10.7 9.7 5.3 25.3

TREE

ppm

23.36 61.72 190.65 61.12 88.73 71.78 24.84 155.21 67.88 56.09 35.42 211.64

ppm

4.7 12.1 39.2 11.4 17.1 13.3 5.0 29.9 12.6 10.8 6.9 38.7

ppm

9.7 22.9 81.5 24.0 33.4 26.5 9.8 64.4 28.7 22.8 14.7 91.5

ppm

1.15 3.07 9.15 3.06 4.47 3.37 1.22 7.67 3.38 2.73 1.75 10.91

ppm

4.6 13.3 35.1 13.4 20.0 15.4 4.8 29.5 13.2 10.8 7.0 43.1

ppm

0.78 2.53 6.00 2.35 3.76 3.49 0.93 5.21 2.52 2.09 1.25 7.57

ppm

0.26 0.62 1.11 0.84 1.18 0.90 0.23 0.79 0.56 0.46 0.28 1.15

ppm

0.75 2.49 5.00 2.26 3.54 3.24 0.92 4.29 2.24 1.88 1.12 5.66

ppm

0.12 0.38 0.85 0.33 0.47 0.47 0.15 0.77 0.34 0.31 0.17 0.88

ppm

0.61 2.04 4.89 1.57 2.31 2.28 0.79 4.61 1.78 1.68 0.95 4.66

ppm

0.11 0.37 1.04 0.30 0.41 0.43 0.15 0.99 0.37 0.34 0.18 0.96

ppm

0.29 0.92 3.06 0.83 0.98 1.17 0.4 2.92 1.00 1.02 0.51 2.80

ppm

0.04 0.13 0.46 0.10 0.14 0.16 0.06 0.48 0.15 0.15 0.08 0.45

ppm

0.22 0.77 2.85 0.59 0.85 0.94 0.34 3.2 0.9 0.89 0.46 2.85

ppm

0.03 0.10 0.44 0.09 0.12 0.13 0.05 0.48 0.14 0.14 0.07 0.45

LaN/YbN

1.57 1.15 1.01 1.43 1.48 1.04 1.08 0.68 1.03 0.89 1.10 1.00

Gd N/YbN

2.03 1.93 1.05 2.28 2.48 2.05 1.61 0.80 1.48 1.26 1.45 1.18

EuN/EuN*

1.58 1.15 0.94 1.67 1.51 1.25 1.16 0.78 1.10 1.08 1.10 0.82

CeN/CeN*

0.96 0.86 0.99 0.93 0.88 0.91 0.91 0.98 1.01 0.96 0.97 1.02

LOI (Lost of Ignition)

Eu/Eu* Eu-anomaly
Ce/Ce* Ce-anomaly
N-normalised to PASS

Table 1

wide ranges:

C from —5.04 to +2.63 ‰ VPDB,

O from

—7.03 to +2.49 ‰ VPDB associated both with facies and with
environmental variability of the sequence.

The

O vs.

C variation chart documents the polymodal

type  of  the  data  set  but  two  main  limestones  and  dolostones
subgroups  are  distinctly  separated  (Fig. 17).  The  position  of
other  points  in  the  chart  indicates  more  complex  processes,
mainly in the “transitional beds”. The low

O vs.

C data

covariance of the whole set and/or separated subgroups docu-
ments quite well preserved isotopic records of the carbonate
beds and detects a transgression regime of sedimentation.

Discussion

REE distribution during transgression

The typical seawater REE pattern shows HREE enrich-

ment,  often  also  with  negative  Ce  anomaly  (Hannigan  &
Sholkovitz 2001; Haley et al. 2004; Ounis et al. 2008). The
REE  (III)  –  carbonate  ion  complexes  are  the  dominant  dis-
solved REE species in seawater: their ability to form carbon-
ate  complexes  increases  from  light  REE  (LREE)  to  heavy
REE (HREE). Increased REE accumulation could be more ef-

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Fig. 14. Felsic/mafic sources of clastic material.

fective in the occurrence of biogenic apatite (like bonebed ap-
atite) where Eu

or trivalent REE ions substitute Ca

. The

REE released from iron oxides, from particulated organic mat-
ter  (POC)  and  potentially  from  other  active  surfaces  (clays)
served as alternative source of REE in the carbonates precipi-
tated  (Haley  et  al.  2004;  Shield  &  Webb  2004).  Observed
changes in REE content (or pattern; Table 1, Fig. 15) indicated
a  restoration  of  marine  water  composition  during  the  trans-
gression.  However,  the  REE  distribution  in  sediments  could
change due to fluctuation of redox and pH condition. Different
dissolved species can be introduced or removed from the sea-
water and cause variation in the water and sediments (Ounis et
al. 2008; Sheldon & Tabor 2009). The distribution of REE can
also  indicate  weathering  process,  because  their  leaching  be-
haviour varies according the regional humidity and increased
acidity, as documented in paleosoils (Sheldon & Tabor 2009).
Eu  and  Ce  anomalies  in  REE  distribution  pattern  commonly
identify  redox  proxies,  because  Eu

separates from other

REE

under reducing condition and Ce

divides into oxide

under oxidizing conditions (Cao et al. 2012).

The different REE distribution patterns in the sample set

studied indicate variability of the siliclastic source or unstable

Fig. 15. REE contents in argillites, limestones and dolomites of the Kardolína section.

transport by wind and water flow during Carpathian Keuper
dolostone and Fatra Formation limestone sedimentation. Eu
enrichment in other REE indicates more reductive conditions
during biogenic limestone precipitation or during early di-
agenesis, as relative increase of C

org

contents (Fig. 16) indi-

cates.  However,  biogenic  carbonates  are  also  enriched  in
phosphate,  in  which  REE  accumulated.  The  “bell-shaped”
MREE-pattern  could  indicate  that  weathering  of  biogenic
phosphates in freshwater could mobilize MREE and relatively
increase  its  content  in  the  limestone  rock  (Hannigan  &
Sholkovitz  2001;  Ounis  et  al.  2008).  Local  bone-beds  oc-
curred  in  the  basal  part  (Beds 0.4,  2.1,  2.2;  Fig. 5)  of  the
Fatra Formation.

Carbon isotope distribution during transgression

Negative

C values in the Carpathian Keuper sequence

(Beds —43  to  0)  and  also  in  the  first  two  sedimentary  cycles
(IV/V)  of  the  Fatra  Formation  (Beds  + 1  to  + 7:  —3.25  to
—0.59 ‰;  Fig. 16)  fluctuate  between  —0.05  and  —5.0 ‰,  but
mostly in the range from —2 to —5 ‰. Later, in the sixth cycle,

C values continually increase to positive

C range (from

MICHALÍK, LINTNEROVÁ, WÓJCIK-TABOL, GAŹDZICKI, GRABOWSKI, GOLEJ, ŠIMO and ZAHRADNÍKOVÁ

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GEOLOGICA CARPATHICA, 2013, 64, 1, 39—62

Fig. 16. Contents of organic carbon (TOC) and

O and

C curves in the lowermost part of the Kardolína section.

—0.05 to + 1.22 ‰). These three cycles locate a span of tempo-
ral sedimentation and indicate continuing carbonate produc-
tion and accumulation within marine transgression. Increased

C (from 1.84 to 2.69 ‰) value fall into the typical interval

of marine limestone documented earlier (Michalík et al. 2007)
in the higher part of the Kardolína section. Positive

C val-

ues  in  limestone  could  indicate  balanced  marine  conditions,
where  “biological  pump”  supported  effective  carbonate  pro-
duction without increase of accumulation and/or burial of or-
ganic  carbon  as  documented  by  low  content  of  total  organic
matter in the samples (Fig. 16).

Negative

C values in dolomite generally document C en-

richment by light

C isotope in comparison with common

marine carbonates. Such isotopically light C could have been
produced by specific production or by biotic extinction in the

water column or by release from methane buried in sediment.
Negative C-isotope event could indicate regional or global cli-
mate change as documented in the T/J boundary beds else-
where (Pálfy et al. 2001, 2007; Ward et al. 2007; Michalík et
al. 2007, 2010; Preto et al. 2010). As

C negative values are

associated with dolostones, they must have been connected
with dolomite precipitation (Masaryk & Lintnerová 1997;
Warren 2000; Garcia del Cura et al. 2001; Berra et al. 2010).

Carpathian Keuper

O values fall in the range —7.03 to

+ 2.49 ‰ and are associated with facies differences (Fig. 17).
Negative to positive

O values in the range —1 to + 3 ‰ are

typical  of  massive  dolostones  of  the  third  cycle.  Samples
with  more  negative  values  in  the  interval  from  —3  to  —1 ‰
are  discontinually  located  in  certain  parts  of  the  cycle  and
probably indicate climatic/hydrologic changes and copy os-

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GEOLOGICA CARPATHICA, 2013, 64, 1, 39—62

cillation pattern in sediments. However, as the cyclostratig-
raphy study indicates, the isotope sample set is too small to
verify this dependence.

Sharp negative

O excursions occur in the basal part of

the dolostone sequence (Beds —43 to —40: from —5.02 to —4.74)
and in the first cycle of the Fatra Formation (from —7.05 to
+ 2.03). In both parts, mixture of calcite/dolomite mineralogy
occurs. These

O changes can be either connected with

sedimentary facies, or they reflect composition of lake/basi-
nal water. Local climatic/hydrological changes controlled
the amount of fresh or meteoric water input to the Carpathian
Keuper’s brackish lake and decreased

O values. The

pattern of the Beds —4 to + 2 (cycle IV) indicates more com-
plex process induced by marine transgression, where short
saline to freshwater floods occurred.

Although post-sedimentary alteration of this part cannot

be entirely excluded, continual increase to more positive

C values documents continual restoration of marine ramp

and does not indicate any important diagenetic substitution
of carbonate phases.

Limestone

O values are relatively similar to each other

and fall in the range from —4.33 to —6.23 ‰, as a common fea-
ture of uppermost Triassic marine limestones (Michalík et al.
2007). A more positive

O excursion (—0.66 ‰) in Bed 29

was associated with early diagenetic dolomitization of algal
mats (Fig. 16). It reflected a salinity increase rather than fresh-
water influx. This supposition is underlined by slight response
of

C values to this episodic dolomitization.

Dolomitization model

As mentioned above,

O and

C variation (Fig. 17)

simply indicates heterogeneity of the sample set. In compari-
son with diagenetic marine dolostone (Smith & Dorobek
1993; Warren 2000; Wacey et al. 2007), dolostone data fall
into unusual area of the plot because of negative

C (—4 to

—3 ‰ VPDB) and more positive

O (in range from —1.5 to

+ 1.0). Relatively positive

O data indicate either freshwa-

ter or saline reservoir waters (or dolomite-forming fluids)
and negative

C values reflect input or generation of car-

phates and producers of CO

enriched to light

C. However,

study of the Coorong dolostone did not confirm regular oc-
currence of isotopically light C (Wacey et al. 2007). Nega-
tive

C values also occur in soil carbonates where the

influence of meteoric waters which are in chemical equilibri-
um with atmospheric CO

(—7 ‰ PDB) cannot be excluded

at all (Warren 2000). Model with equilibrated soil-water or
water-atmospheric CO

could be alternatively applied to the

isotope composition of limestone/dolomite mixed mineralogy
(—43 to —41 or —6 to —1) where negative

C (—4 to —3 ‰)

values are attached to negative

O (—4 to —5 ‰). A similar

mixed marine-meteoric model of the Carnian to Norian Keu-
per dolostone generation was presented by Rychliński (2008)
and Jaglarz (2010). A relatively high content of Sr in carbon-
ates came more probably from brine water. This interpretation
is in line with the facies character of the Carpathian Keuper
dolostones as climatically induced sediments.

Cyclostratigraphic remarks

The thickness of the Fatra Formation sequence in the

Kardolína  section  (107  meters)  is  three  times  greater  than  in
other  sections.  This  gives  a  reason  to  suppose  that  the  se-
quence is more complete, formed by a more rapid sedimentary
rate (60 mm/kyr) on a gentle submarine slope. 18 sedimentary
cycles  were  distinguished  in  the  Fatra  Formation,  which  are
attributable to short eccentricity (100 kyr) cycles, taking into
consideration  the  2 Myr  duration  of  the  Rhaetian;  and  three
cycles have been discerned in the uppermost part of the Car-
pathian  Keuper.  The  dominance  of  eccentricity  cycles  was
stated during the Late Permian (cf. Legler & Scheider 2008);
or during the Late Triassic/Early Jurassic (Haas et al. 2010).
Both the geometry and lithological composition of the majori-
ty of the Fatra Formation cycles indicate a shallowing upward
trend:  however,  this  phenomenon  was  often  combined  with
the  effect  of  freshwater  influx  bringing  coarse  sedimentary
particles (Fig. 18) in conditions of raised humidity trend at the
end of the Triassic (Ahlberg et al. 2002; Preto et al. 2010).

Fine lamination preserved in the “zero interval” of the

transitional (IV) cycle between the Carpathian Keuper and

Fig. 17. Grouping of C and O isotopes in carbonates of the Kardolína section compared
with typical composition of the Coorong dolomite.

bon  enriched  to  light  C,  probable  iso-
topically fractionated in biogenic/meta-
bolic process (Pálfy et al. 2001). If we
accept the sedimentary and microfacies
character of the dolostone studied, then
the C and O isotope and Sr contents in-
dicate that Keuper fine-crystalline dolo-
mite  precipitated  from  brine  or  from
pore  water  and  can  be  compared  with
type B of the Coorong dolostone (Rosen
et  al.  1989;  Warren  2000;  Garcia  del
Cura  et  al.  2001;  Wacey  et  al.  2007).
Brine with optimal Mg/Ca ratio can be
generated  by  microbial  processes  in
specific climate and hydrology. The life
activity of S reducing (SRB) and photo-
synthesizing  bacteria  was  frequently
discussed as a source of organic matter
(Bechtel et al. 2007), consumers of sul-

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GEOLOGICA CARPATHICA

GEOLOGICA CARPATHICA, 2013, 64, 1, 39—62

the Fatra Formation deserves special attention. Beds 0.3, 0.4,
0.5, 0.6 and 0.9 consist of argillite to marly mudstone. Detri-
tal  quartz  forms  0.4  to  2.3 mm  thick  laminae.  Individual
laminae  are  arranged  in  a  regular  pattern  (Fig. 19):  two
thicker  bands  are  usually  followed  by  seven  thinner  ones.
Considering  the  average  sedimentary  rate,  influx  events
bringing quartz detritus must have repeated in rhythms of ap-
proximately 20 years (solar Hale cycles?).

The close-up view on the dololaminite in Bed 29 (Fig. 19)

is even more surprising. Laminae are well preserved, show-
ing  details  of  a  fine  stratification  pattern.  Several  laminae
show  stromatolitic  character  of  former  algal  mats.  Planar
laminae  are  very  thin  (0.2  to  0.8 mm),  in  bundles  of  7  to  9
( = Hale  rhythm?).  In  closer  view,  series  of  thinner  laminae
are visible between them, in groups of 5.

Magnetic susceptibility

According to Ellwood et al. (2000) and Crick et al. (2001),

the MS record in most marine rocks is of detrital origin and re-
lated to the influx of lithogenic fraction to a basin, controlled
by both: climate variations (e.g. humidity) and eustatic sea-
level changes. MS highs and lows are related to regressive and

transgressive intervals, respectively. The model seems to work
in  rather  open  marine  environments  (Whalen  &  Day  2010).
However, in the carbonate platform settings an inverse corre-
lation  might  also  be  observed  (Da  Silva  et  al.  2009).  In  the
Kardolína section the lowest sea-level is postulated at the tran-
sition interval between the Carpathian Keuper and Fatra For-
mation.  It  corresponds  well  to  MS  trends  observed  in  the
Kardolína section. The Carpathian Keuper with increasing MS
trend would correspond to the regressive interval, while step-
wise  decrease  of  MS  in  the  Fatra  Formation  might  be  inter-
preted as a transgressive trend. This interpretation alone would
be not sufficient because it might be possible that the decreas-
ing MS trend is related to dilution of ferromagnetic particles in
carbonate matrix, and thus to a possibly higher sedimentation
rate.  However,  as  the  same  trend  is  also  inferred  from  sedi-
mentological  analysis  (see  above)  and  MS  correlates  quite
well  with  some  sedimentological  features,  like  quartz  grain
size (Fig. 4), it might be accepted as a quite likely model.

The primary nature of the MS record might also be tested,

correlating the MS values with Al

. Al is regarded as a

predominantly lithogenic element which might be used as a
proxy for fine detrital clay input into the basin (Calvert &
Pedersen 1993; Śliwiński et al. 2010). The correlation graphs

Fig. 19. Lamination in Beds 0.3, 0.4, 0.5, 0.6, 0.9 and 29, in the Kardolína section. Scale bars are 10 mm long.

MICHALÍK, LINTNEROVÁ, WÓJCIK-TABOL, GAŹDZICKI, GRABOWSKI, GOLEJ, ŠIMO and ZAHRADNÍKOVÁ

GEOLOGICA CARPATHICA

GEOLOGICA CARPATHICA, 2013, 64, 1, 39—62

(see  Fig. 13e—f)  reveal  a  moderate  positive  correlation  be-
tween MS and Al content – this might be treated as prelimi-
nary  confirmation  that  MS  contains  a  significant  detrital
component.  However,  both  MS  and  geochemical  data  were
available from only 9 samples. Moreover, it seems that MS
carriers are different in the Fatra Formation and Carpathian
Keuper:  the  MS  correlates  with  Al

within a lithostrati-

graphic unit, but when the entire dataset is considered (Fatra
Formation+Carpathian Keuper) – the correlation is not sig-
nificant! It cannot be excluded that a part of the SP magne-
tite is of authigenic origin and not directly related to other
erosion – derived components (Jackson 1993; Grabowski et
al. 2009; Devleeschouwer et al. 2010).

Paleocommunities

The lowermost sedimentary cycles contain sporadic fos-

sils, mostly plant fragments and ostracods, inhabiting tempo-
ral  water  reservoirs.  The  third  cycle  represents  swampy
environments  which  contained  much  more  diverse  mixed
marine and brackish organisms: foraminifers (Agathammina),
bivalve  molluscs  (Rhaetavicula  community),  linguloid  bra-
chiopods,  sharks,  fish,  amphibians  (?)  and  burrowing  ani-
mals producing Rhizocorallium burrows.

The fifth cycle recorded stabilization of marine environ-

ments (and communities, cf. Michalík & Jendrejáková 1978;
Gaździcki  1983)  affected  by  storm  activity.  Inhabitants  of
shallow lagoons (Corbula and Gervillaria community) were
periodically washed out by stormy turbulent waters from the
soft bottom, killed and their broken shells were accumulated
in  tempestite  layers.  Shell  accumulations  formed  temporary
firm ground for an oyster (Placunopsis) community. During
continuing  deepening  and  accumulation  of  fine  mud,  the
bottom  was  inhabited  by  an  infaunal  Propeamussium  and
Entolium community.

Fine quartz dust transported by eolian activity accumulated

in a marine bay. Deteriorating oxygenation enabled deposition
of shaly beds rich in coprolites, crinoid ossicles, pectinid bi-
valves and fish teeth. Megalodon limestone indicates settle-
ment of pachyodont bivalves during shallowing events.

Conclusions

The Kardolína section yields an almost complete record of

the Rhaetian marine transgression into the Zliechov Basin. A
comprehensive study of mineralogy, lithology, lithostratig-
raphy, cyclostratigraphy, fossils, geochemistry including C
and O stable isotopes and rock magnetism has provided de-
tailed information about environmental changes at the end of
the Triassic.

The sequence consists of distinct cycles of 100 kyr eccen-

tricity  and  40 kyr  obliquity  character,  but  some  laminated
layers  also  bear  signs  of  much  finer  rhythmicity,  including
repetition  in  100,  20  and  even  in  4(?)  year  cycles  of  events.
Rhythmically repeating detrital laminae were formed by al-
ternation  of  climatic  parameters  (monsoon-like  periods).
Analysis of clastic quartz grain size and content shows that
both fluvial input and eolian activity were involved in their or-

igin. On the other side, high concentrations of foraminifers
(Agathammina) in some of these laminae indicates rather in-
tensification of marine influence.

The sequence stratigraphic and cyclostratigraphic division

fits well with magnetic susceptibility which reflects the dis-
tribution of authigenic and detrital constituents in the rock
sequence. The good preservation of the primary magnetic
record is promising from the point of view of magnetostrati-
graphic study which will be performed in the near future.

The integrated geochemical data are consistent with the

character  and  time  span  of  sedimentary  facies  evolution.  C
and  O  isotope  curves  responded  selectively  to  changes  of
eustacy  and  climate  and  tightly  followed  restoration  of  ma-
rine carbonate ramp during the Rhaetian.

A wide range of

O values (—7.0 to + 2.7) by itself is not

anomalous in the Triassic carbonates but combination of these
data with negative

C values resulted in an unusual distri-

bution of dolostone data in the plot (Fig. 15, Table 1). It
documents either dolomite precipitation from brackish or hy-
persaline lake water or its derivation from pore water compa-
rable to the Recent Coorong B dolostone. Less positive

values indicate level of diagenetic/thermal fractionation of the
oxygen isotope. Negative C values indicate water enrichment
to light C (HCO

—

) induced by microbial productivity.

Stabilization of benthic communities in the Fatra Formation

basin  was  not  straightforward  since  it  was  strictly  controlled
by physical environmental factors. Although foraminifers, bi-
valves and sharks appeared shortly after the start of the trans-
gression,  bivalve  mollusc  biostromes  were  repetitively
destroyed  by  storms  and  temporary  firm  bottoms  were  colo-
nized  by  oysters  and  burrowers.  Bottom  colonization  by
pachyodont  bivalves,  brachiopods  and  corals  was  possible
much later, in highstand conditions.

Acknowledgments:  The  authors  acknowledge  help  from
three reviewers, namely Prof. József Pálfy for valuable dis-
cussion,  inspiring  comments  and  thorough  corrections,  but
also  Prof.  Ján  Soták  and  Dr.  Tomasz  Rychliński  who  sub-
stantially  contributed  to  the  scientific  level  of  the  manu-
script.  Field  works  could  not  have  been  done  without  the
painstaking  help  of  our  young  co-workers,  namely  Jakub
Rantuch,  Martin  Závacký,  Štefan  Szalma,  Mgr.  Zuzana
Weissová, Dr. Peter Ledvák, Dr. Martina Martincová, Mgr.
Peter  Klepsatel,  Mgr.  Ján  Čatloš,  and  Mgr.  Hanna  Nizin-
kiewicz. We always met with friendly support from the Tatra
National  Park  State  Forests  administration  and  its  Research
Station in Tatranská Lomnica (Dr. Stanislav Pavlarčík), and
from  the  Spišská  Belá  municipality,  as  well.  Field  research
was  also  supported  by  direction  and  workers  of  the  Aca-
demia Hotel in Stará Lesná, where we always had our home
base.  Thanks  for  financial  support  go  to  0065/12  VEGA
Project.  SEM  photographs  were  provided  by  Dr.  I.  Holický
(State  Geological  Institute  of  Dionýz  Štúr,  Bratislava)  and
by  Mgr.  N.  Halašiová  (Geological  Institute  SAS,  Banská
Bystrica). MS and rock magnetic experiments were performed
within a Project No. 61.2301.0902.00.0 of the PGI-NRI, as a
part  of  the  IGCP  580  Project.  Isotope  analyses  were  done
mostly by Dr. K. Małkowski (Polish Academy of Sciences,
Warszawa).

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GEOLOGICA CARPATHICA, 2013, 64, 1, 39—62

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