GeolCarp_Vol58_No4_321

GEOLOGICA CARPATHICA, AUGUST 2007, 58, 4, 321—332

www.geologicacarpathica.sk

Introduction

The  Krosno  lithofacies  consisting  of  Upper  Oligocene  to
Lower  Miocene  synorogenic  sediments  crowns  the  flysch
deposition  in  the  Western  Carpathian  Flysch  Belt.  It  reflects
the  integrated  effects  of  the  Helvetian  Neoalpine  orogeny
and  eustatic  changes  in  the  Oligocene.  This  lithofacies  char-
acterizes,  together  with  the  Menilite  Formation,  the  Outer
(Menilite-Krosno)  Group  of  thrust  sheets  of  the  Flysch  Belt.
In  the  Magura  Group  of  thrust  sheets  this  lithofacies  de-
scribed  from  eastern  Slovakia  and  Poland  by  Świdziński
(1961)  as  the  Malcov  Formation  was  not  studied.

The purpose of the present paper is to characterize the

Krosno  lithofacies  and  its  underlying  sediments  from  the
point  of  view  of  lithology,  petrology,  sedimentology,  pa-
leogeography  and  ductile  deformation  interpreted  in  terms
of  plate  tectonics.  The  obtained  results  follow  up  the  bios-
tratigraphic  study  (Švábenická  et  al.  2007),  which  indicates
the  gradual  onset  of  the  Krosno  lithofacies  from  the  internal
to  external  zones  of  the  Outer  Group  of  thrust  sheets.

Geological setting

The Upper Oligocene—Lower Miocene Krosno lithofa-

cies represents the youngest flysch sequence of the Outer
(Menilite-Krosno) Group of thrust sheets in the Flysch

The Upper Oligocene—Lower Miocene Krosno lithofacies in

the Carpathian Flysch Belt (Czech Republic): sedimentology,

provenance and magnetic fabrics

ZDENĚK STRÁNÍK

, FRANTIŠEK HROUDA

2,3

, JIŘÍ OTAVA

, HELENA GILÍKOVÁ

and LILIAN ŠVÁBENICKÁ

Czech Geological Survey, Leitnerova 22, CZ-602 00 Brno, Czech Republic; stranik@cgu.cz; otava@cgu.cz; gilikova@cgu.cz

Agico Inc., Ječná 29a, Box 90, CZ-621 00 Brno, Czech Republic; fhrouda@agico.cz

Institute of Petrology and Structural Geology, Charles University, Albertov 6, CZ-128 43 Praha, Czech Republic

Czech Geological Survey, Klárov 131/3, P.O.Box 85, 118 21 Praha, Czech Republic; lilian.svabenicka@geology.cz

(Manuscript received March 1, 2006; accepted in revised form December 7, 2006)

Abstract: The Krosno lithofacies is the Upper Oligocene—Lower Miocene synorogenic sequence that terminates the flysch
sedimentation in the orogenic system of the Western Carpathians. Its deposition replaced the hypoxic sedimentation of the
underlying Oligocene Menilite Formation. This change in deposition was connected with the Helvetian Neoalpine orogeny
which iniciated the fundamental rearangement in the orogenic belt, gradual isolation of foreland basins and creation of the
“Protoparatethys”. The differences in deformation between the Krosno lithofacies and the underlying Upper Cretaceous to
Eocene strata are recorded in all tectonofacial units of the Outer (Menilite-Krosno) Group of thrust sheets. Moreover, a trend
towards increase of ductile deformation from the outer to the inner margin of the Flysch Belt is evident. The investigation
of translucent heavy minerals produced evidence of different spectra between the Krosno lithofacies and underlying strata
of individual tectonofacial units. The spatial distribution of the Krosno lithofacies and the transport of clastic material from
the SE indicate the deposition of a submarine fan that prograded to the NW.

Key words: Upper Oligocene—Lower Miocene, Carpathians, Flysch Belt, Krosno lithofacies, tectonics, paleogeography,
sedimentology, heavy minerals, magnetic anisotropy.

Belt  of  the  Western  Carpathians.  In  the  territory  of  the
Czech  Republic  this  lithofacies  is  developed  in  the  Kros-
no,  Ždánice-Hustopeče  and  Křepice  Formations  within  the
stratigraphic  range  Late  Oligocene—Early  Miocene.  The
Krosno  lithofacies  in  the  Outer  Group  of  thrust  sheets  usu-
ally  overlies  the  Menilite  Formation  originated  in  the  hy-
poxic  environment  which  dominated  in  the  northern  part
of  Tethys  during  the  Early  Oligocene  (Table 1).  The  rela-
tion  of  the  Lower  Miocene  Šakvice  Marl  to  the  underlying
Krosno  lithofacies  in  the  Ždánice  and  Pouzdřany  Units  in
South  Moravia  is  not  clear  (Cicha  &  Pícha  1964;  Molčí-
ková  &  Stráník  1987;  Krhovský  et  al.  1995).

The diachronous onset of the Krosno lithofacies based

on  the  occurrence  of  the  marker  Jasło  Limestone  in  differ-
ent  lithostratigraphic  units  (Menilite,  Krosno  and  Malcov
Formations)  was  supported  by  Koszarski  &  Źytko  (1959),
Jucha  (1969)  and  Haczewski  (1989)  in  the  Polish  and  Slo-
vak  Flysch  Carpathians.  In  the  Czech  Republic  only  in-
complete  information  exists  from  this  point  of  view  about
the  age  of  the  Krosno  lithofacies  (Bubík  1987;  Bubík  &
Švábenická  2000;  Stráník  &  Švábenická  2004).

Material

Not only the profiles containing boundary strata of the

Krosno lithofacies and Menilite Formation but also indi-

323

THE UPPER OLIGOCENE—LOWER MIOCENE KROSNO LITHOFACIES (CARPATHIAN FLYSCH BELT)

Fig. 2. 1 – Pelitic facies of the Ždánice-Hustopeče Formation, Ždánice Unit locality Vážany u Slavkova. 2 – Flute-casts of the
Ždánice-Hustopeče Formation, Ždánice Unit, locality Boleradice (disused quarry).

Fig. 3. 1 – Psammite-pelitic facies of the Ždánice-Hustopeče Formation, Ždánice Unit, locality Boleradice (disused quarry). 2 – Nanno-
fossil Zagórz Limestone of the Ždánice-Hustopeče Formation, Ždánice Unit, locality Boleradice (disused quarry).

ates.  The  proportion  of  sandstones  and  shales  varies  both
vertically  and  horizontally  from  predominantly  shaly  to
predominantly  sandy  facies.  Based  on  these  changes  the
pelitic,  psammite-pelitic  and  psammitic  facies  were  distin-
guished  (Cicha  et  al.  1964).  The  maximal  extent  of  the  for-
mation  is  known  from  southeast  Moravia.  A  Krosno
lithofacies  with  planar  laminated  sandstones  was  distin-
guished  in  the  vicinity  of  Kroměříž  and  named  by  Menčík
et  al.  (1954)  as  the  Těšnovice  development.

The pelitic facies of the Ždánice-Hustopeče Formation,

originally  termed  the  Hustopeče  Marls  (Rzehak  1881),  is
characterized  by  complete  predominance  of  calcareous  lay-
ered  claystones  and  marls  with  sporadic  thin  intercalations
and  laminas  of  sandstones  and  siltstones  (Fig. 2.1).  The  fa-
cies  presents  some  similarities  in  lithology  and  microbios-
tratigraphy  to  the  overlying  Šakvice  Marl  (Cicha  et  al.
1975)  of  Eggenburgian  age.  This  facies  of  Eggenburgian
age  (Švábenická  et  al.  2007)  is  widespread  in  the  northwest-
ern  margin  of  the  Ždánice  Unit  south  of  Slavkov  u  Brna.

The psammite-pelitic facies of the Ždánice-Hustopeče

Formation  is  characterized  by  rhythmic  alternation  of
sandstones,  siltstones  and  layered  calcareous  shales
(Fig. 3.1).  The  cycles  usually  begin  with  sandstone  at  the
bottom  and  gradually  pass  upwards  through  siltstones  into
shales  at  the  top.  The  thickness  of  cycles  varies  from  deci-
meter  to  several  meters.  The  accumulation  of  cycles  of  the
same  thicknesses  gives  rise  to  a  sequence  of  thin,  medium-
and  thick-bedded  rhythmites.  In  the  middle  rhythmic  fly-
sch  of  the  disused  quarry  near  Boleradice  village  thin  in-
tercalations  of  Zagórz  Limestone,  described  by  Haczewski
(1984)  in  Poland,  were  observed  (Fig. 3.2).

The psammitic facies of the Ždánice-Hustopeče Forma-

tion,  originally  termed  the  Ždánice  Sandstone  (Steinitzer
in  Paul  1890),  is  formed  of  thick  bedded  massive  fine-  to
coarse-grained  calcareous  sandstone  of  low  lithification.
Some  irregular  bodies  of  conglomerates  (usually  debris-
flows)  occur.  Thin  intercalations  of  mudstones  are  very
rare.  The  psammitic  facies  has  a  large  extension  in  the  SE

324

STRÁNÍK, HROUDA, OTAVA, GILÍKOVÁ and ŠVÁBENICKÁ

part  of  the  Ždánice  Unit  and  in  the  lower  part  of  the
Ždánice-Hustopeče  Formation  (based  on  the  log  of  deep
wells).  The  total  thickness  of  Ždánice-Hustopeče  Forma-
tion  is  estimated  to  be  1250 m.

The Krosno lithofacies of the Zdounky Unit possess a

slightly  specific  lithology  characterized  by  algal  sand-
stones  with  Lithothamnium  sp.  Chmelík  (1970)  described
these  Oligocene  sediments  as  the  Upper  division  and  the
underlying  Upper  Cretaceous  to  Eocene  strata  as  the  Low-
er  division  of  the  Zdounky  Unit.  The  Lower  division  man-
ifests  some  lithological  similarities  with  its  stratigraphic
equivalents  in  the  Ždánice  Unit.  The  Menilite  Formation
was  not  observed.

In the Silesian and Fore-Magura Units the Krosno lithofa-

cies  is  represented  by  the  Krosno  Formation  (Tietze  1889)
which  is  very  similar  in  lithology  to  the  Krosno  lithofacies
of  the  Ždánice  Unit.  Only  the  facial  differentiation,  espe-
cially  the  pelitic  facies,  is  not  so  distinctly  developed.  The
underlying  Menilite  Formation  in  the  Silesian  and  Fore-
Magura  Units  contains  some  layers  of  the  fine  to  coarse
sandstones  (Kliwa  Sandstone).  The  Submenilite  Formation,
recently  renamed  to  the  Rožnov  Formation  (Eliáš  2001),  is
characterized  by  similar  lithology  to  the  Němčice  Forma-
tion  of  the  Ždánice  Unit.  In  its  lower  part  the  lenticular  bod-
ies  of  sandstones  and  conglomerates  occur.  The  thickness  of
the  Rožnov  Formation  is  estimated  to  be  600—800 m.  The
facies  with  slump  bodies  of  tilloid  conglomerates  (debris
flows)  in  the  Pre-Magura  Unit  was  termed  the  Chvalčov
Member  by  Pesl  &  Hanzlíková  (1983).

In the Pouzdřany Unit, we consider the Křepice Forma-

tion  of  Aquitanian  to  Eggenburgian  age  (Cicha  et  al.
1965)  overlying  the  Boudky  Marl,  to  belong  to  the  Kros-
no  lithofacies.  The  Křepice  Formation  consists  of  fine-  to
medium-grained  slightly  lithificated  sandstones,  siltstones
and  layered  shales.  Their  layers  are  centimeter  to  several
meters  thick,  rhythmically  alternate  and  forming  a  se-
quence  a  few  hundred  meters  thick.

The presence of the Krosno lithofacies in the Subsile-

sian  Unit  is  a  subject  of  discussion.  Earlier,  the  Menilite
Formation  was  considered  to  be  a  youngest  member  of  the
Subsilesian  Unit.  Recently,  Eliáš  (1998)  put  the  sediments
in  the  source  tributary  of  Sedlnice  stream  near  Ženklava
village  into  the  Krosno  lithofacies  and  termed  them  the
Ženklava  Formation.  Roth  et  al.  (1973)  assigned  these
sediments  to  the  Frýdlant  Formation  (new  name  intro-
duced  by  Eliáš  1993  for  the  earlier  Submenilite  Forma-
tion).  Studies  of  petrology  (see  in  this  paper)  and  the
microbiostratigrafic  study  by  Švábenická  &  Bubík  (pers.
com.)  do  not  confirm  Eliáš’s  observations.

Petrology and mineralogy

The sandstones of the Krosno lithofacies were sampled

for  thin  sections,  the  translucent  heavy  mineral  assem-
blages  and  the  geochemical  analyses  of  detrital  garnet.  In
order  to  evaluate  the  change  of  provenance,  comparative
samples  from  the  underlying  strata  were  collected  and
analysed.

Thin section petrology

The sandstones of the Krosno lithofacies possess ac-

cording  to  the  thin  section  study  a  fairly  consistent  petro-
logic  composition.  The  sharp  to  half-rounded  quartz
clasts,  forming  about  20 %  of  the  rock,  prevail  over  the  of-
ten  sericitized  feldspars.  Muscovite  and  chloritized  bi-
otite,  assorted  into  parallel  structure,  locally  create  up  to
15 %  of  the  rock.  The  calcite  grains  are  probably  both  of
clastic  and  authigenic  origin.  The  rock  fragments  are
present  in  the  amount  of  7 %  and  include  volcanic  glass,
gneiss,  phyllite  and  vulcanite.  The  carbonate  matrix  is  of
basal  character  and  often  corrodes  the  feldspar  and  quartz
grains.  There  are  generally  badly  visible  clasts  of  fossils  in
the  rock.

Heavy minerals

Translucent heavy mineral assemblages (further only

THMA) were studied and correlated at several dozen lo-
calities along the whole area of investigation (see Fig. 1).

There are three groups of assemblages distinguished

within  the  sandstone  samples  belonging  to  the  Krosno
lithofacies  and  the  underlying  strata.  The  first  group
should  be  defined  as  a  garnetic  assemblage,  the  second
one  as  a  tourmaline-garnetic  assemblage  and  the  third
group  as  a  polymict  assemblage  of  varied  composition
(Fig. 4).

Garnetic assemblage

The garnet amount is mostly higher than 85 %, further

minerals as the apatite, tourmaline, zircon, rutile and stau-
rolite are present in the amounts between 1—10 %.

Fig. 4. Comparison of the translucent heavy mineral assemblages of
sandstones. Dot – garnetic assemblage of the Krosno lithofacies of
the Silesian and Ždánice Units, square – tourmaline-garnetic as-
semblage of the Krosno lithofacies of the Zdounky and Fore-
Magura Units, cross – polymict assemblage of the strata underlying
the Krosno lithofacies of the Outer Group of thrust sheets.

325

THE UPPER OLIGOCENE—LOWER MIOCENE KROSNO LITHOFACIES (CARPATHIAN FLYSCH BELT)

The garnetic THMA was investigated with all analysed

sandstone  samples  from  Krosno  Formation  of  the  Silesian
Unit.  There  are  only  two  garnetic  THMA  from  the  six  anal-
ysed  sandstones  of  the  Ždánice-Hustopeče  Formation.  The
other  four  sandstone  samples  with  different  composition
of  THMA  were  found  in  the  pelitic  facies  of  the  Ždánice-
Hustopeče  Formation  extended  along  the  external  margin
of  the  Ždánice  Unit.  Nevertheless,  the  garnetic  THMA  is
characteristic  of  the  Ždánice-Hustopeče  Formation  as  dem-
onstrated  by  the  data  (150  sandstone  analyses)  presented  by
Pícha  (1973)  from  this  formation  of  the  Ždánice  Unit.

Tourmaline-garnetic assemblage

The tourmaline amounts are usually in tens of %, in sev-

eral  cases  higher  than  those  of  garnet.  Other  minerals  such
as  staurolite,  apatite,  rutile,  zircon  and  hornblende  are
present  in  variable  unstable  amounts.

The tourmaline-garnetic THMA characterizes generally

the  Krosno  lithofacies  of  the  Fore-Magura  and  Zdounky
Units.  This  THMA  was  found  also  in  two  samples  belong-
ing  to  the  Těšnovice  development,  whose  tectono-facial
appurtenance  is  not  clear.  The  identical  THMA  was  de-
scribed  from  the  Těšnovice  development  by  Pícha  (1973).

Polymict assemblage

The assemblages of the sandstones underlying the Kros-

no  lithofacies  are  of  varied  composition.  This  THMA  pre-
sents  a  high  amount  of  the  tourmaline,  garnet  and
staurolit.  The  substantial  diversity  in  amount  of  other  hae-
vy  minerals  may  be  influenced  by  provenance  from  differ-
ent  tectono-facial  units.  A  similar  THMA  was  determined
in  the  sandstones  near  Ženklava,  mistaken  by  Eliáš  (1998)
for  the  Krosno  lithofacies.

A special subgroup with some typical and unifying fea-

tures  was  identified  in  the  Menilite  Formation  of  the  Fore-
Magura  Unit.  It  is  characterized  by  high  ratio  of  oval  to
idiomorphic  zircons  (6 : 1)  and  high  amounts  of  rutile.

Correlation and provenance

There are significant differences in THMA not only be-

tween  the  Krosno  lithofacies  and  the  underlying  strata  but
also  between  the  individual  tectono-facial  units.  These
differences  are  connected  with  the  changes  in  deposition
and  in  the  source  areas.  The  changes  reflect  the  Helvetian
orogeny  during  the  Oligocene.  Most  probably  the  differ-
ences  in  THMA  are  controlled  by  different  provenance,
because  of  change  in  the  ratios  of  ultrastable  minerals.  The
primary  source  of  translucent  heavy  minerals  was  un-
doubtedly  rich  in  high  temperature  and  high-pressure
metamorphites  (gneiss,  granulite).  Most  probably  the  gar-
nets  were  redeposited  from  the  uplifted  Magura  Flysch.

Detrital garnet geochemistry

The sandstones of the Krosno lithofacies in the Silesian

Unit  were  analysed  and  the  results  were  compared  with
earlier  analysed  sandstones  of  the  Magura  Group  of  thrust
sheets.  The  obtained  results  alow  us  to  comment  on  cer-
tain  overlaps  and/or  analogies  in  the  composition  of  the
detrital  garnet  assemblages  (estimated  as  30—40 %)  of  the
sandstones  of  the  Krosno  Formation  (Oligocene—Miocene)
of  the  Silesian  Unit  and  selected  sandstones  of  the  Soláň
Formation  (Upper  Cretaceous—Paleocene)  of  the  Rača
Unit  of  the  Magura  Group  of  thrust  sheets  (Fig. 5A,B).  The
detrital  garnets  common  in  the  sandstones  of  both  units
have  high  almandine  contents  (65—85 %),  low  spessartine

Fig. 5. Comparison of the detrital garnet geochemistry between: A – sandstone of the Krosno Formation, Silesian Unit, locality Lhota
u Kelče (19 – see Fig. 1) and B – sandstone of the Soláň Formation, Rača Unit, Magura Group of thrust sheets, locality Hostýn (quar-
ry, 23 – see Fig. 1). The diagram was constructed by “opening” the walls of a tetrahedron where the tops represent almandine, grossu-
lare, spessartine and pyrope end members.

326

STRÁNÍK, HROUDA, OTAVA, GILÍKOVÁ and ŠVÁBENICKÁ

(1—8 %) and similar stable amounts of pyrope and
grossulare (5—20 %).

The coincident composition of detrital garnet in the

sandstones  of  the  Krosno  and  Soláň  Formations  indicates
the  redeposition  of  detritus  from  the  Proto-Magura  Group
of  thrust  sheets  into  basins  of  the  Krosno  lithofacies.

Sedimentology

The Krosno lithofacies can be characterized in all tec-

tono-facial  units  from  the  point  of  view  of  sedimentology
as  synorogenic  deepwater  flysch  sediments.  The  transport
and  deposition  of  these  sediments  is  produced  mainly  by
gravity  flows.  The  dominant  sediment  support  mecha-
nisms  of  gravity  flows  are  fluid  turbulence,  escaping  pore
fluid,  dispersive  pressure,  matrix  strength  and  density.
These  mechanisms  characterize  the  turbidity  and  contouri-
ty  currents  from  which  turbidites  and  contourites  origi-
nate.  The  most  significant  features  of  turbidites  and
contourites  are  the  sole  markings,  size  grading,  plane,  rip-
ple-cross  and  convolute  laminations.  The  size  grading
which  usually  is  not  present  in  the  contourites,  is  regarded
as  a  diagnostic  feature  to  distinguish  them  from  turbidites.
The  vertical  succession  of  these  features  was  framed  into
an  ideal  sequence  (interval  Ta-e  –  Bouma  1962,  or  divi-
sion  S

1—3

, Tt and Td-e – Lowe 1982). According to Shan-

mugam  (2000)  the  massive  sandstones  can  be  applied
universally  for  either  turbidites,  contourites,  or  sandy  de-
bris  flows  usually  found  in  the  Ta-c  interval  of  the  flysch
sediments.

The sedimentological study of the Krosno lithofacies

was  pursued  only  in  the  Ždánice  Unit,  where  this  lithofa-
cies  (Ždánice-Hustopeče  Formation)  could  be  examined  in
a  lot  of  artificial  outcrops  and  boreholes  from  the  1960s  to
1990s.

The Ždánice-Hustopeče Formation was studied in detail

in  the  disused  quarry  at  the  NW  border  of  the  Boleradice
village,  where  a  sequence  of  thin-bedded  turbidites  in
thicknesses  of  ca.  12.5 m  is  exposed  (see  Fig. 3.1).  This  se-
quence  consists  of  rhythmic  alternance  of  fine-  to  medi-
um-coarse  calcareous  sandstones,  siltstones  and  grey
brownish  and  greenish  wheathered  calcareous  shales.  The
layers  of  sandstones  usually  up  to  15 cm,  sporadically
maximum  40 cm  thick  slightly  predominate  over  the
shales  of  the  same  thicknesses.  The  turbidity  sequences
usually  begin  with  interval  Tb  and  Tc  (thin  layers).  On  the
base  of  sandstone  layers  rare  flute-casts  (Fig. 2.2),  load-
casts  and  ichnofossils  occur.  The  grade  bedding  is  little
pronounced.  The  Bouma’s  interval  Tc  has  very  frequent
parallel  and  ripple-cross  laminations.  Conversely  the  con-
volute  lamination  is  rare.  The  flute-casts  and  ripple-cross-
lamination  (9  measurements)  indicate  the  direction  of
paleocurrents  from  SSE  (within  the  extent  290  to  26º).  The
studied  sequence  represents  distal  turbidites  deposited  un-
der  low  flow  regime  conditions  from  the  lobes  of  the  lower
submarine  fan.  The  Zagórz  Limestone  may  be  regarded  as
the  nannofosil  pelagite  of  the  turbidity  sequence  (Te)
originated  during  the  maximum  decrease  in  the  strength  of

the turbidity current over the calcite compensation depth
(CCD) level.

The facies analysis of the Ždánice Unit based on the

geological  mapping  and  well-log  indicates  that  the  psam-
mite-pelitic  facies  is  the  most  extended  facies  of  the
Ždánice-Hustopeče  Formation.  The  psammitic  facies  more
commonly  found  in  the  rear  of  the  Ždánice  Unit  is  charac-
terized  by  a  lot  of  typical  features  of  turbidity  currents
such  as  Bouma’s  interval  Ta,  graded  bedding,  slump  and
slide  structures,  erosion  and  others.  It  contains  numerous
conglomerate  bodies  interpreted  as  debris  flows.  The  sedi-
ments  of  psammitic  facies  represent  the  base-of-slope  de-
posits  more  commonly  found  in  the  middle  and  upper  fan
abutting  the  continental  slope.  They  may  be  regarded  as
proximal  turbidites.  In  contrast,  the  pelitic  facies  was  ob-
served  mainly  in  the  external  margin  of  the  Ždánice  Unit.
In  comparison  with  proximal  psammitic  facies  its  sedi-
ments  were  deposited  far  from  source  area.  The  relatively
abundant    microfossils  and  total  predominance  of  calcare-
ous  shales  indicate  the  deposition  in  open  sea  under  very
low  flow  regime  conditions.  The  distribution  of  the  facies
of  the  Ždánice-Hustopeče  Formation  indicates  a  deposi-
tional  environment  of  prograding  and  overlapping  subma-
rine  fan  which  gradually  filled  the  basin.  This  assumption
coincides  with  the  northwestward  trending  of  paleocur-
rents  markings  not  only  on  the  locality  Boleradice  and  nu-
merous  measurements  in  the  whole  of  Ždánice  Unit,  but
also  with  episodic  measurements  in  the  Krosno  lithofacies
of  the  Silesian  and  Fore-Magura  Units.  These  indicators  as
well  as  the  massive  redeposition  of  microfossils  from  the
older  flysch  sequences  into  the  Krosno  lithofacies  and  the
pebbles  of  the  Zlín  Formation  and  of  the  Variscan
granitoids  observed  in  the  debris-flows  of  the  Ždánice-
Hustopeče  Formation  near  Velké  Pavlovice  suggest,  that
the  clastic  material  originates  both  from  internal  basinal
source  and  the  Carpathian  thrust  belt  (Stráník  et  al.  1982;
Hanžl  et  al.  1998).  This  assumption  is  compatible  with  the
result  of  the  study  of  the  garnet  geochemistry  (see  in  this
paper)  which  indicates  the  possibility  of  sources  in  the  up-
lifted  Magura  Flysch.

Magnetic fabric and ductile deformation

For investigating the anisotropy of magnetic suscepti-

bility  (AMS),  oriented  specimens  (10  to  15  pieces  per  lo-
cality),  were  sampled  in  176  localities  of  the  western
(Moravian  and  Slovak)  sector  of  the  Flysch  Belt  in  the
framework  of  various  research  projects.  The  results  were
partially  published  elsewhere  (Hrouda  &  Stráník  1985;
Hrouda  &  Potfaj  1993;  Hrouda  et  al.  in  preparation)  and
serve  for  overall  characterization  of  the  AMS  of  the  west-
ern  sector  of  the  Flysch  Belt.  In  order  to  characterize  the
AMS  of  the  Krosno  lithofacies,  special  oriented  sampling
was  done  for  the  purpose  of  the  present  paper.  In  all  the
samplings,  psammites  (mostly  sandstones)  were  taken,  be-
cause  they  are  more  sensitive  to  the  initial  deformation
than  siltstones  and  pelites.  The  latter  show  relatively
strong  depositional/compactional  magnetic  fabric  and  its

327

THE UPPER OLIGOCENE—LOWER MIOCENE KROSNO LITHOFACIES (CARPATHIAN FLYSCH BELT)

change into a deformational one needs more intense de-
formation than in the case of psammites.

The anisotropy of magnetic susceptibility (AMS) of ori-

ented  specimens  was  measured  by  the  KLY-2  and  KLY-3S
Kappabridges  (Jelínek  1973,  1980;  Jelínek  &  Pokorný
1997)  and  computed  using  the  ANISO  11-14  and  SUSAR
programs  (Jelínek  1977,  1996).

The results of AMS measurements are summarized in

terms  of  P,  T,  and  f  parameters,  being  presented  in  the  box-
and-whisker  plots  (Tukey  1977;  McGill  et  al.  1978).  The
P  and  T  parameters  are  defined  as  follows:

P = k

/ k

T = 2 ln(k

/ k

) / ln(k

/ k

)—1,

where k

are the principal susceptibilities.

The P

parameter,  called  the  degree  of  AMS,  indicates  the  intensi-
ty  of  the  preferred  orientation  of  magnetic  minerals  in  a
rock  and  the  T  parameter  (Jelínek  1981)  indicates  the
shape  of  the  susceptibility  ellipsoids;  it  varies  from  —1  (per-
fectly  linear  magnetic  fabric)  through  0  (transition  between
linear  and  planar  magnetic  fabric)  to  + 1  (perfectly  planar
magnetic  fabric).  The  f  parameter  is  the  angle  between  the
magnetic  foliation  and  bedding.

The mean bulk susceptibility of the sandstones investi-

gated is very low, being in the order of 10

—5

[SI] and in the

very beginning of the order of 10

—4

. The magnetic miner-

als,  as  revealed  by  investigation  of  temperature  variation
of  susceptibility,  are  represented  by  a  mixture  of  paramag-
netic  minerals  and  magnetite,  the  former  prevailing.  There
are  no  systematic  differences  among  tectono-facial  and
lithostratigraphic  units.

The AMS in sedimentary rocks provides information on

the  deposition  and  compaction  processes.  In  addition,  in
sedimentary  rocks  that  underwent  ductile  deformation,
which  is  the  frequent  case  of  accretionary  prisms,  it  can
serve  as  a  sensitive  indicator  of  progressive  ductile  defor-
mation.  In  natural  sedimentary  rocks  unaffected  by  later
deformation,  the  magnetic  foliation  is  always  oriented
near  the  bedding,  while  the  magnetic  lineation  is  mostly
roughly  parallel  to  the  near-bottom  water  current  direc-
tions  determined  using  sedimentological  techniques.  Less
frequently,  the  magnetic  lineation  may  be  perpendicular
to  the  current  direction,  which  is  typical  of  the  flysch  sedi-
ments  of  the  lowermost  A  member  of  the  Bouma  sequence.
The  degree  of  AMS  is  relatively  low  and  the  AMS  ellip-
soid  is  in  general  oblate  (Stage I  in  Fig. 6a).

During the processes of diagenesis and early ductile de-

formation,  the  originally  sedimentary  magnetic  fabric  may
be  slightly  modified.  If  the  ductile  deformation  is  repre-
sented  by  vertical  shortening  due  to  the  loading  by  the
weight  of  overlying  strata,  the  degree  of  AMS  and  the  ob-
lateness  of  the  AMS  ellipsoid  increase,  while  the  magnetic
foliation  and  lineation  retain  their  orientations.  If  the  duc-
tile  deformation  is  represented  by  the  bedding  parallel
shortening  or  by  the  bedding  parallel  simple  shear  or  by
both,  the  degree  of  AMS  initially  decreases  and  only  later
increases  when  the  deformation  is  strong  enough  to  over-
come  the  initial  vertical  compaction.  The  magnetic  fabric

becomes  initially  more  planar  and  only  later  is  it  more  tri-
axial  or  even  linear.  The  magnetic  lineation  deviates  grad-
ually  from  the  direction  of  flow  towards  that  of  maximum
strain,  often  creating  a  bimodal  pattern.  The  magnetic  foli-
ation  remains  initially  near  the  bedding,  after  a  stronger
strain  it  deviates  from  it,  creating  a  girdle  in  magnetic  foli-
ation  poles  that  is  perpendicular  to  the  magnetic  lineation
(Stages II and III in Fig. 6a).

The AMS of the Flysch Belt was investigated extensive-

ly  in  the  past  and  the  results  were  presented  by  Hrouda  &
Stráník  (1985),  Hrouda  &  Potfaj  (1993)  and  Hrouda  et  al.
(in  preparation).  They  can  be  summarized  as  follows.

The magnetic fabrics in the Flysch Belt show both sedi-

mentary  and  deformational  features.  The  relatively  low  de-
gree  of  AMS,  planar  magnetic  fabric,  small  angle  between
magnetic  foliation  and  bedding  in  the  majority  of  speci-
mens,  and  small  angle  between  magnetic  lineation  and
current  direction  (if  measured)  may  indicate  the  sedimen-
tary  origin  of  the  magnetic  fabric.  On  the  other  hand,  the
predominantly  prolate  magnetic  fabric  and  moderate  to
very  large  angle  between  magnetic  foliation  and  bedding
(in  many  specimens  magnetic  foliation  is  almost  perpen-
dicular  to  bedding)  or  the  existence  of  a  girdle  pattern  in
the  magnetic  foliation  poles  no  doubt  indicate  deforma-
tional  effects  on  the  magnetic  fabric.  Consequently,  the
magnetic  fabric  can  be  regarded  in  general  as  composite,
that  is  composed  of  the  deformational  magnetic  fabric  su-
perimposed  on  the  sedimentary  magnetic  fabric.  This  su-
perimposition  has  a  character  of  overprinting  of  variable
degree,  sometimes  none  or  very  weak,  sometimes  relative-
ly  strong,  but  never  obliteration.

The weakest tectonic deformation is indicated in the

Ždánice  Unit  whose  mean  degree  of  AMS  is  the  highest  of
all  the  thrust  sheets  investigated,  the  magnetic  fabric  is
mostly  planar,  and  the  magnetic  foliation/bedding  angle
is  the  smallest.  In  the  Silesian  Unit,  the  indications  of  the
tectonic  deformation  are  stronger,  but  not  very  much.  It  is
comparable  to  the  Bílé  Karpaty  and  Oravská  Magura  Units
of  the  Magura  Group  of  thrust  sheets.  In  the  innermost  tec-
tonic  structure  (the  Fore-Magura  Unit)  the  effect  of  tecton-
ic  deformation  on  the  magnetic  fabric  is  the  strongest,  so
strong  that  the  magnetic  foliation  in  numerous  specimens
was  reoriented  from  the  position  parallel  to  the  bedding
into  the  position  perpendicular  to  the  bedding.  The  same
degree  of  deformation  characterizes  the  Rača  and  Bystrica
Units  of  the  Magura  Group  of  thrust  sheets.  The  above  re-
lationship  demonstrates  the  box-and-whisker  plots  of  the
degree  of  AMS  in  individual  units  of  the  western  sector  of
the  Flysch  Belt  (Fig. 6b).  The  degree  of  AMS,  though  rath-
er  variable  in  all  units,  is  relatively  high  in  the  marginal
units  indicating  mostly  sedimentary  magnetic  fabrics  (the
Ždánice  and  Silesian  Units  in  the  west  and  the  Bílé  Kar-
paty  and  Oravská  Magura  Units  in  the  east),  while  it  is  rel-
atively  low  in  the  central  Fore-Magura,  Rača,  and  Bystrica
Units,  indicating  non-coaxial  superposition  of  the  defor-
mational  magnetic  fabric  on  the  sedimentary  one.

The AMS is able to indicate differences in the ductile

deformation not only between the tectono-facial units, but
also between the strata within these units. From this point

329

THE UPPER OLIGOCENE—LOWER MIOCENE KROSNO LITHOFACIES (CARPATHIAN FLYSCH BELT)

of  view,  the  relationship  between  the  Krosno  lithofacies
and  the  underlying  formations  is  particularly  important,
because  it  can  indicate  changes  in  the  arrangement  of
plates  in  the  vicinity  of  the  Paleogene/Neogene  boundary.
This  relationship  can  be  best  studied  in  the  Ždánice  Unit,
where  the  Ždánice-Hustopeče  Formation  was  extensively
investigated  by  Hrouda  &  Stráník  (1985)  and  the  underly-
ing  Němčice  Formation  was  investigated  for  the  present
paper.  The  degree  of  AMS  is  clearly  higher  in  the  Ždánice-
Hustopeče  Formation  than  in  the  underlying  Němčice  For-
mation  (Fig. 6c).  Similarly,  the  magnetic  fabric  shape  is
more  planar  in  the  former  formation  than  in  the  latter
(Fig. 6d).  The  magnetic  foliation/bedding  angle  is  on  the
other  hand  much  larger  in  the  Němčice  Formation  than  in
the  Ždánice-Hustopeče  Formation  (Fig. 6e—g).  All  these
parameters  indicate  that  the  Ždánice-Hustopeče  Formation
suffered  very  low  ductile  deformation  if  any,  while  the
ductile  deformation  of  the  underlying  Němčice  Formation
was  clearly  stronger,  even  though  also  weak  absolutely.

In the Zdounky Unit, the degree of AMS is clearly high-

er  in  the  Upper  division,  than  in  the  Lower  division  (see
Fig. 6c).  The  shape  parameter,  indicating  the  magnetic
fabric  shape,  shows  relatively  planar  magnetic  fabrics  in
the  Lower  division  and  very  variable,  but  less  planar,  mag-
netic  fabrics  on  average  in  the  Upper  division  (see
Fig. 6b).  The  magnetic  foliation/bedding  angle  is  low  in
the  Lower  division,  while  it  is  very  variable  and  large  in
average  in  the  Upper  division  (see  Fig. 6c).  This  magnetic
fabric  is  not  easy  to  interpret  from  the  point  of  view  of
ductile  deformation.  The  degree  of  AMS  indicates  stron-
ger  ductile  deformation  in  the  Lower  division,  whereas  the
shape  parameter  and  magnetic  foliation/bedding  angle  in-
dicate  stronger  ductile  deformation  in  the  Upper  division.

In the Silesian Unit, the degree of AMS is clearly higher

in  the  Krosno  Formation  than  in  the  underlying  Rožnov
Formation  (see  Fig. 6c).  The  magnetic  fabric  shapes  are
similar  in  both  the  formations,  being  very  slightly  more
planar  in  the  former  formation  than  in  the  latter  (see
Fig. 6d).  The  magnetic  foliation/bedding  angle  is  very
variable  and  relatively  large  on  average  in  the  Krosno  For-

Fig. 6. Characteristics of the AMS in sandstones of the western sector of the Flysch Belt of the Western Carpathians. a – Schematic devel-
opment  of  the  AMS  in  progressively  weakly  deformed  rocks  of  the  accretionary  prisms  (adapted  from  Aubourg  et  al.  2004)  b  –  Box-
and-whisker plot of the degree of AMS in individual units of the western sector of the Flysch Belt. In the plot the mean value is represented
by the median being the central line in the central box. The central box covers the middle 50 % of the data values, between the lower and
upper quartiles. The “whiskers” extend out to extremes (minimum and maximum values), but only to those points that are within 1.5 times
the interquartile range. ZD – Ždánice thrust sheet, SL – Silesia thrust sheet, FM – Fore-Magura thrust sheet, RA – Rača thrust sheet,
BY – Bystrica thrust sheet, OM – Oravská Magura thrust sheet, BK – Bílé Karpaty thrust sheet. c – Box-and-whisker plot of the degree
of AMS in the Krosno lithofacies and in the underlying formations in selected units of the Flysch Belt. ZD1 – the Němčice Formation in
the  Ždánice  Unit,  ZD2  –  the  Ždánice-Hustopeče  Formation  in  the  Ždánice  Unit,  ZK1  –  the  Lower  division  in  the  Zdounky  Unit,
ZK2  –  the  Upper  division  in  the  Zdounky  Unit,  SL1  –  the  Rožnov  and  Menilite  Formations  in  the  Silesian  Unit,  SL2  –  the  Krosno
Formation in the Silesian Unit, FM1 – the Submenilite Formation in the Fore-Magura Unit, FM2 – the Krosno (Chvalčov) Formation in
the  Fore-Magura  Unit.  d  –  Box-and-whisker  plot  of  the  shape  parameter  in  the  Krosno  Formation  and  in  underlying  formation  in  selected
units  of  the  Flysch  Belt.  For  legened  see  fig. 6c.  e  –  Box-and-whisker  plot  of  the  magnetic  foliation/bedding  angle  in  the  Krosno
Formation  and  in  the  underlying  formation  in  selected  units  of  the  Flysch  Belt.  For  legend  see  fig. 6c.  f  –  Orientations  of  magnetic
foliation poles in the Ždánice-Hustopeče Formation of the Ždánice Unit after simple tectonic correction (rotation of bedding about bedding
strike  into  horizontal  position).  Equal-area  projection  on  the  lower  hemisphere.  g  –  Orientations  of  magnetic  foliation  poles  in  the
Němčice Formation of the Ždánice Unit after simple tectonic correction. Equal-area projection on the lower hemisphere.

mation,  while  it  is  moderately  variable  and  small  on  aver-
age  in  the  underlying  Rožnov  Formation  (see  Fig. 6e).
The  degree  of  AMS  and  the  shape  parameter  indicate
weaker  ductile  deformation  in  the  Krosno  Formation,
while  the  magnetic  foliation/bedding  angle  indicate  the
weaker  deformation  in  the  underlying  Rožnov  Formation.

In the Fore-Magura Unit, the degree of AMS shows very

low  variability  and  very  low  mean  value  in  the  Krosno
(Chvalčov)  Formation,  while  in  the  underlying  Submeni-
lite  and  Menilite  Formations  it  is  extremely  variable  and
very  high  on  average  (much  higher  than  in  all  the  forma-
tions  investigated  in  this  study  (see  Fig. 6c).  The  magnetic
fabric  is  relatively  planar  in  the  Submenilite  and  Menilite
Formations,  while  in  the  Krosno  (Chvalčov)  Formation  it
is  much  less  planar  (see  Fig. 6d).  The  magnetic  foliation/
bedding  angle  is  very  variable  and  very  large  on  average
in  the  Submenilite  and  Menilite  Formations,  while  it  is
moderately  variable  and  small  on  average  in  the  Krosno
(Chvalčov)  Formation  –  see  Fig. 6e).  The  magnetic  fabric
in  the  Fore-Magura  Unit  is  no  doubt  deformational  in  ori-
gin,  the  intensity  of  ductile  deformation  being  much  high-
er  in  the  underlying  formations  than  in  the  the  Krosno
(Chvalčov)  Formation.

The above differences in ductile deformation, even

though  not  always  unambiguous,  but  evident,  between
the  Krosno  lithofacies  and  the  underlying  formations
may  indicate  changes  in  the  tectonic  setting  of  the  plates
in  the  terminal  stages  of  closing  the  Flysch  Belt  basins.
The  relatively  strong  ductile  deformation  in  the  latter
formations  may  result  from  motions  connected  with
subduction,  while  much  weaker  ductile  deformations  in
the  former  formations  may  indicate  the  situation  when
subduction  terminated  and  started  to  be  transformed  into
the  beginning  of  collision.  The  rocks  of  the  Krosno
lithofacies  were  evidently  deposited  on  the  slopes  of  the
European  plate,  fed  also  from  the  Magura  Flysch  likely
underplated  to  the  southern  West  Carpathian  plate.  After
deposition,  the  whole  body  was  slightly  thrust  over  the
Carpathian

Foredeep

without

suffering

observable

ductile deformation.

330

STRÁNÍK, HROUDA, OTAVA, GILÍKOVÁ and ŠVÁBENICKÁ

Regional correlation and attribution to major

tectonic and depositional events

The Upper Oligocene to Lower Miocene sediments rep-

resented  by  Krosno  lithofacies  of  the  Carpathian  Flysch
Belt  are  defficient  of  diagnostic  paleontological  data.
Their  age,  facies  determination  and  regional  correlation,
therefore,  depend  also  on  the  lithology  and  the  overall
tectonostratigraphic  setting.  In  order  to  better  integrate
this  lithofacies  into  the  broader  Alpine-Carpathian  system
we  relate  them  to  principal  depositional  and  tectonic
events.  The  Krosno  lithofacies  is  a  typical  synorogenic
flysch  sequence  being  deposited  in  a  complex  system  of
foreland  basin  formed  on  the  mobile  European  platform
margin  in  the  Late  Oligocene.  Its  deposition  reflects  the
important  environmental  changes  which  took  place  on  the
north  margin  of  Tethys  in  the  Oligocene.  The  Krosno  fly-
sch-type  sedimentation  is  marked  by  a  very  high  influx  of
detrital  material  especially  from  the  orogenic  belt,  large
thickness  of  deposits  and  distinct  facial  changes.  It  re-
placed  the  hypoxic  sedimentation  of  the  underlying  Me-
nilite  Formation.  These  changes  in  deposition  are  related
to  the  Helvetian  orogeny  in  the  Oligocene.  The  foreland
basins  on  the  downbended  margin  of  the  platform  and  the
rearrangement  of  the  orogenic  belt  shown  by  the  study  of
heavy  minerals  and  ductile  deformation  are  also  connect-
ed  with  the  Helvetian  movements.  The  flexural  down-
bending  of  the  platform  margin  is  most  likely  related  to
the  loading  of  the  progressing  Carpathian  thrust  sheets.  A
similar  interpretation  of  the  downbending  of  the  subduct-
ing  European  plate  was  presented  in  the  Western  Alps  by
Ziegler  (1987,  1988).

The Krosno lithofacies has a large extent in the Alpine-

Carpathian  orogenic  belt.  The  sediments  of  similar  lithofa-
cies  are  known  from  Eastern  Carpathians  in  Poland,
Ukraine  and  Romania.  The  strata  in  the  tectonic  window
of  the  Eastern  Alps  near  Rogatsboden  in  Austria  and  the

Purkirchen Beds (Bachmann & Müller 1991) of the Bavar-
ian Molasse show some similarities.

Conclusions

The Krosno lithofacies is a synorogenic sequence that

terminates  the  flysch  sedimentation  in  the  Upper  Oli-
gocene  up  to  Lower  Miocene  in  the  Outer  Group  of  thrust
sheets  of  the  Flysch  Belt  in  the  Alpine-Carpathian  orogen-
ic  system.

The spatial distribution of the individual developments

of  the  Krosno  lithofacies  within  the  Ždánice  Unit  and  the
transport  of  the  material  from  the  SE  in  all  tectono-facial
units  indicate  the  depositon  from  a  submarine  fan  that  pro-
graded  to  the  NW  and  gradually  filled  in  newly  estab-
lished  foreland  basins.

Different spectra of translucent heavy minerals were

found  in  the  Krosno  lithofacies  and  the  underlying  strata
of  individual  tectono-facial  units.  The  provenance  of  the
clastic  material  (pebbles  of  the  Zlín  Formation  in  the  con-
glomerates  of  the  Ždánice-Hustopeče  Formation)  from  the
Proto-Magura  Group  of  thrust  sheets  coincides  with  iden-
tical  geochemical  composition  of  garnets  from  sandstones
of  the  Krosno  Formation  in  the  Silesian  Unit  and  those
from  the  Soláň  Formation  in  the  Magura  Group  of  thrust
sheets  (see  Fig. 5A—B).  According  to  these  results  we  sug-
gest  that  the  Proto-Magura  Group  of  thrust  sheets  was
folded,  emerged  and  supplied  the  material  into  the  basins
of  the  Outer  Group  of  thrust  sheets  where  the  sedimenta-
tion  of  the  Krosno  lithofacies  continued  (Fig. 7).  The  dif-
ferences  in  the  tectonic  deformation  recorded  by  the  AMS
between  the  Krosno  lithofacies  and  the  underlying  forma-
tions,  originally  found  in  the  Ždánice  Unit,  were  recently
indicated  in  all  tectono-facial  units  of  the  Outer  Group  of
thrust  sheets.  In  addition,  a  trend  was  observed  in  increas-
ing  of  the  ductile  deformation  from  the  outer  towards  the
inner  margin  of  the  Outer  Group  of  thrust  sheets  (see
Fig. 6c—e).  The  differences  in  deformation  are  ascribed  to
the  Helvetian  Neoalpine  orogeny  in  the  Oligocene  that
initiated  the  changes  in  sedimentation  in  the  foreland  ba-
sins  and  the  rearrangement  of  the  orogenic  zone.  In  terms
of  plate  tectonics  this  orogeny  represents  the  stage  of  clos-
ing  subduction  and  starting  collision.

Acknowledgments:  The  financial  support  of  the  Grant
Agency  of  the  Czech  Republic  (Grant  No. 205/03/0154)  is
gratefully  acknowledged.  Special  thanks  are  due  to  re-
viewers  Andrzej  Ślączka  (Kraków),  Jacek  Grabowski
(Warszawa)  and  Ján  Soták  (Banská  Bystrica)  for  their  criti-
cal  remarks.

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