GeolCarp_Vol57_No3_157

GEOLOGICA CARPATHICA, JUNE 2006, 57, 3, 157—176

www.geologicacarpathica.sk

Metamorphosed and ductilely deformed conodonts from

Triassic limestones situated beneath ophiolite complexes:

Kopaonik Mountain (Serbia) and Bükk Mountains

(NE Hungary) – a preliminary comparison

MILAN SUDAR

and SÁNDOR KOVÁCS

Institute of Regional Geology and Paleontology, Faculty of Mining and Geology, University of Belgrade, Kamenička 6,

11000 Belgrade, Serbia and Montenegro; sudar@eunet.yu

Geological Research Group of the Hungarian Academy of Sciences, Department of Geology, Eötvös Loránd University,

Pázmány Péter sétány 1/c, H-1117 Budapest, Hungary; skovacs@iris.geobio.elte.hu

(Manuscript received March 7, 2005; accepted in revised form December 8, 2005)

Abstract: Metamorphosed and ductilely deformed conodonts with CAI (Colour Alteration Index) values 5—7 are
described and illustrated from Kopaonik Mt, Vardar Zone, Serbia and from Bükk Mts, NE Hungary. They derive from
Upper Triassic cherty metalimestones, overthrust by ophiolite complexes. The metamorphism and ductile deformation
of the conodont elements evidently took place simultaneously with those of the limestone host rocks, which might have
been related to subduction and obduction; however, younger tectonometamorphic events could also have played a role.
Unfortunately, illite “crystallinity” indices from Kopaonik Mt are too random for thermometric assessment and geochro-
nological data are missing so far. Nevertheless, by comparison with published data about limestone textural alteration and
with previously published metamorphic petrological data from NE Hungary, at least a Szendrő-type (min. 400 °C, but
less then 500 °C, temperature and 300 MPa pressure) can be supposed for the regional metamorphism of conodont-
bearing cherty limestone series of Kopaonik Mt.

Key words: Serbia, Vardar Zone, NE Hungary, ductile deformation, regional metamorphism, limestone textural
alteration, conodont alterations.

Introduction

Conodont  thermometry  to  reveal  the  thermal  history  of  sed-
imentary  rock  sequences  has  been  widely  used  since  the
publication  of  the  basic  works  by  Epstein  et  al.  1977  and
Rejebian  et  al.  1987.  It  is  based  on  colour  alteration  of  con-
odonts  ( = Colour  Alteration  Index  –  CAI)  caused  by  coali-
fication  of  the  small  amount  of  organic  matter  they  contain
due  to  increasing  temperature:  the  originally  yellowish
white,  translucent  (CAI = 1)  conodonts  become  darker  and
darker,  then  black  (CAI = 5).  At  a  further  increase  of  temper-
ature,  due  to  loss  of  organic  matter,  they  again  become
lighter  coloured:  grey  (CAI = 6),  white  (CAI = 7),  finally
crystal  clear,  glassy  (CAI = 8).  Calibration  was  done  by  heat-
ing  in  an  electronic  furnace  under  atmospheric  conditions,
and  using  the  Arrhenius  plot,  was  projected  back  to  geolog-
ical  times  up  to  500 Ma.  Temperature  values  of  this  experi-
mental  test  are  shown  in  Table 1.  Up  to  the  value  CAI = 5,
that  is  within  the  range  of  the  diagenetic  zone,  correlation
was  also  made  with  palynomorph  colour  alteration.

The investigation of conodont colour alteration seems

to  be  a  useful  method  to  estimate  temperatures  of  burial
and  contact  metamorphism.  Numerous  papers  have  been
published  on  this  topic,  for  example  Buggisch  (1986),
Belka  (1990),  Nöth  (1991),  Königshof  (1992),  Gawlick  et
al.  (1994),  Garcia-Lopez  et  al.  (1997),  Gawlick  &  Hopfer
(1999),  and  many  others.

However, under conditions of regional dynamothermal

metamorphism,  where  besides  temperature,  lithostatic
and  fluid  pressures  also  play  decisive  roles,  the  alteration
of  conodonts  is  different  and  above  CAI = 5  is  much  more
intense:  they  become  progressively  recrystallized  and
deformed,  in  accordance  with  the  metamorphism  and
ductile  deformation  of  their  host  rock.  Mineral  paragene-
sis,  illite  “crystallinity”  and  vitrinite  reflectance  data
above  the  diagenetic  zone  indicate  considerably  lower
temperatures,  than  could  be  deduced  from  simple  experi-
mental  heating  (Kovács  &  Árkai  1987;  Rejebian  et  al.
1987).  Furthermore,  it  was  found,  that  different  CAI  indi-
ces,  that  should  indicate  different  temperatures,  can  be
found  even  in  the  same,  usually  fractured  specimens
(CAI=5  to  7,  black,  grey  and  white  parts;  Kovács  &  Árkai
op. cit.).

Table 1: Temperature ranges related to different CAI of conodonts
(after Epstein et al. 1977; Rejebian et al. 1987 and Königshof 1992).

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SUDAR and KOVÁCS

From the experimental (hydrouos pyrolysis at 50 MPa

pressure) data shown on the Arrhenius plot (Rejebian et al.
1987, Fig. 4), postulating a thermal heating of ~ 10 Myr du-
ration, ~ 4 50 to 600

C temperature values can be calculat-

ed to these high CAI (5 to 7) values. These are higher, than
could be determined for regionally metamorphosed terraines
in NE Hungary using illite “crystallinity” (KI – Kübler in-
dex) and b

indices (350 to 400

C, exceptionally 450

at 250 to 300 MPa or more pressure; Árkai 1983; Árkai &
Kovács 1986; Kovács & Árkai 1987; see Table 2 in the
present paper). Furthermore, conodont elements are sup-
posed to disappear above 500

C in conditions of regional

dynamothermal metamorphism (Neubauer & Friedl 1997,
and Neubauer, pers. commun.).

Conodonts from metamorphosed Triassic sequences of the

Kopaonik Mt (Vardar Zone, Serbia) and from the Bükk Mts
(Bükk Composite Terrane, NE Hungary), which are structur-
ally beneath ophiolite complexes are presented and com-
pared in this paper. Evidently, their alteration was not related
simply to sedimentary burial and thermal effects, but to
subduction and collisional processes, although subsequent
nappe movements could still play a role in their alteration.

Comparison is also done with previously published meta-

morphosed conodonts from the Szendrő Hills and Torna s.s.
(or Martonyi) Unit of the Rudabánya Hills, NE Hungary
(Árkai & Kovács 1986; Kovács & Árkai 1987, 1989).

The preliminary results of the above mentioned investi-

gations were already given in the abstract by Sudar &
Kovács (1998).

These are the first metamorphosed conodonts described

and illustrated in details from Serbia. We should add to
this point that conodonts of similar preservation were
shown from approximately similarly metamorphosed Tri-
assic limestones from the Fruška Gora Mt, Northern Serbia
(Đur anović 1971; for recent description of the metamor-
phosed series see Čanović & Kemenci 1999 and Karamata
et al. 2002) and from the Medvednica Mt near Zagreb,
Croatia (Đur anović 1973; for a recent geological descrip-
tion of the Medvednica Metamorphic Series see Pamić &
Tomljenović 1998; Judik et al. 2004).

Rare CAI determinations of Triassic conodont elements

have been performed in the territory of the former Yugo-
slavia, when either their numerical values have been cited
(in Slovenia: Kolar-Jurkovšek 1994; Kolar-Jurkovšek &
Jurkovšek 1995, 1996; Krystyn et al. 1998), or the results
of the method have been used for assessing organic meta-
morphism (in Croatia: Palinkaš et al. 2000).

Geological setting

The geological units compared in the present study are

located now in a distant position within the Neogene—
Quaternary geological framework of the Pannonian area,
the basement of which had been amalgamated and accret-
ed only by the Middle Miocene, due to sizeable micro-
plate and terrane movements (Csontos & Nagymarosy
1998; Kovács et al. 2000), the Kopaonik Mt being on the
South of the Pannonian Basin, whereas the Bükk Mts were
on its northern margin. Separated by the large Tisia Ter-
rane (or Tisza Mega-unit) (Fig. 1) of quite different origin,
the Bükk and neighbouring units show an undoubtedly
Dinaridic Paleozoic and Mesozoic development, suggest-
ing that they were originally parts of the same geological
domain (cf. Csontos 1999; Dimitrijević et al. 2003 and
Filipović et al. 2003 for latest reviews). Consequently, the
tectonometamorphic evolution of the units containing the
metamorphosed conodonts shown herein could be related
to the same geodynamic events. However, it is not yet
widely known in the international geological literature,
therefore we present below the geological facts in some
more detail.

The metamorphosed Triassic sequences yielding the con-

odonts presented herein are structurally beneath ophiolite
complexes, that are eroded in most part of the Bükk Mts.
Fig. 1 also shows other areas of the former Yugoslavia (Fruš-
ka Gora and Medvednica Mts), from where metamorphosed
Triassic conodonts were published from a similar setting
(Đur anović 1971, 1973; for the geological setting see
Čanović & Kemenci 1999 and Pamić & Tomljenović 1998).

Table 2: Average temperature (determined from illite “crystallinity” and vitrinite reflectance data) and pressure (determined from white
K-mica b

geobarometric data) of regional dynamothermal metamorphism of tectonic units in NE Hungary, as well as CAI indices of conodonts

and textural alteration types of limestones recorded in them (after Árkai & Kovács 1986 and Kovács & Árkai 1987, 1989, slightly modified).

159

METAMORPHOSED AND DUCTILELY DEFORMED CONODONTS (SERBIA—NE HUNGARY)

Fig. 1.  Tectonic/terrane  sketch  map  of  the  Dinarides + Vardar  Zone  and  of  the
Pannonian  area  (slightly  modified  after  Dimitrijević  et  al.  2003).  1  –  Neo-
tethyan  ophiolite  complexes  (Vardar  Zone,  Dinaridic  Ophiolite  Belt,  and  in  the
Zagorje-Mid-Transdanubian  and  Bükk  Composite  Terranes);  2  –  units  related
to  the  North  Tethyan  continental  margin  in  the  Pelsonia  Composite  Terrane;
3  –  units  related  to  the  Adriatic/Apulian  continental  margin  of  the  Neotethys
in the Dinarides + Vardar Zone and in the Pelsonia Composite Terrane; 4 – ar-
eas  with  marine  Upper  Carboniferous + Permian  within  3  (“Noric-Bosnian
Zone”  in  sense  of  Flügel  1990);  5  –  Paleozoic  units  without  marine  Upper
Carboniferous  and  Permian  in  the  Dinarides  and  Pelsonia  Composite  Terrane
(“Betic-Serbian  Zone”  in  sense  of  Flügel  1990);  6  –  units  related  to  the
Variscan Median Crystalline + Moldanubian zones (in sense of Neubauer & von
Raumer  1993)  and  to  the  North  Tethyan  (European)  continental  margin  during
the Mesozoic. Green dots in NE Hungary indicate drill hole occurrences of the
Neotethyan  Bódva  Valley  Ophiolite  Complex,  whereas  the  green  triangle
shows the outcrops of the Upper Jurassic (?) Telekesoldal rhyolites in the Rud-
abánya  Mts.  The  area  in  the  full  colour  (a)  indicates  surface  occurrences,
whereas  those  with  hachures  (b)  borehole  show  proven  ones  in  the  pre-Tertia-
ry basement. A – Kopaonik Mt area (Vardar Zone, Serbia; Fig. 2);  B – Bükk
+ Aggtelek + Rudabánya  Mts  (Pelsonia  Composite  Terrane,  NE  Hungary;
Fig. 4).  Conodont  localities:    1  –  Županj  (Kopaonik  Mt);  2  –  Smrekovnica
(Kopaonik  Mt);  3  –  Fruška  Gora  Mt;  4  –  Medvednica  Mt;  5  –  Bükk  PA
Unit; 6 – Torna s.s. or Martonyi Unit; 7 – Szendrő Unit; 8 – Uppony Unit.

Geological framework of the Kopaonik Moun-
tain area

There are two main groups of viewpoints in

Serbian  or  Yugoslavian  geological  literature
referring  to  the  geological  position  of  the  Ko-
paonik  Mt  area:  these  terrains  are  considered
either  as  parts  of  the  Vardar  Zone  as  a  separate
first-order  geotectonic  unit,  or  parts  of  the  (In-
ternal)  Dinarides.  We  find  it  necessary  to  turn
to  the  papers  by  M.D.  Dimitrijević  and  S.
Karamata,  published  during  the  last  ten  years.
These  papers  contain  the  most  detailed  and  re-
cent  geological  data  and  facts  on  the  composi-
tion,  origin  and  distribution  of  the  Kopaonik
Block,  as  a  specific  part  of  the  Vardar  Zone
with  a  long  and  complex  evolution.  These  au-
thors’  viewpoints  on  the  Vardar  Zone,  and  on
the  Kopaonik  area  as  its  integral  part,  can  be
summarized  as  follows:

a) both authors distinguish the Vardar

Zone,  as  a  separate  first-order  geotectonic
unit  which  is  presently  located  between  the
Drina-Ivanjica  Element/Terrane  (DIE)  and
the  Serbian-Macedonian  Massif/Composite
Terrane  (SMCT)  (Fig. 3).

b) Dimitrijević (1995, 1997, 2000, 2001) di-

vide  the  Vardar  Zone  into  three  Sub-zones:
External  (EVSZ),  Central  (CVSZ),  and  Internal
(IVSZ).  The  Kopaonik  Block  (KB),  as  one  of
its  integral  parts  covers  the  whole  southern
part of the EVSZ (Figs. 2 and 3). Its boundaries
are:  the  Západná  Morava  trough  in  the  north,
the  regional  tectonic  zone  Vrnjačka  Banja—
Brzeće—Podujevo—Preševo  in  the  east,  Skopje
depression  in  the  south,  and  as  specific  ele-
ment,  the  Studenica  Slice,  and  Kosovska
Mitrovica  Flysch  of  the  DIE  in  the  west.

c) Karamata (1995), Karamata et al. (2000),

and  Resimić-Šarić  et  al.  (2000),  divide  the
Vardar  Zone  into  three  Sub-zones  as  well:  the
Vardar  Zone  Western  Belt  (VZWB),  Kopaon-
ik  Block  and  Ridge  Unit  (KBRU)  including
the  Kopaonik  block  (Kb),  and  Main  Vardar
Zone  (MVZ)  (Fig. 3).  Such  division  differs
from  that  by  M.D.  Dimitrijević  (loc.  cit.)  be-
cause  the  VZWB  and  the  KBRU  (with  Kb)
correspond  to  EVSZ,  while  MVZ  includes
both  CVSZ  and  IVSZ.  Thus,  the  Kopaonik
block  covers  a  smaller  area,  because  its  west-
ern  boundary  is  in  the  valley  of  the  river  Ibar,
and  it  narrows  in  the  direction  Kosovska
Mitrovica—Sitnica—Lab  in  the  south  (Fig. 2).
Its  southern  boundary  is  not  precisely  de-
fined  yet,  because  the  deposits  of  the  Kb  are
covered  in  this  area.  Besides,  the  Kb  extends
northwards  to  Belgrade  and  southwards  to
Priština,  in  the  form  of  a  narrow  zone,  form-
ing  the  Kopaonik  Block  and  Ridge  Unit.

160

SUDAR and KOVÁCS

In the papers by Dimitrijević (1995, 1997, 2000) dealing

with  the  Vardar  Zone  and  with  the  Kopaonik  Mt  area,  the
registration  of  new  facts  and  evolution  of  different  models,
during  more  than  the  last  50  years  are  quoted.  In  the  same
papers,  and  particularly  in  Dimitrijević  (2001),  only  a
rough  sketch  of  the  known  facts  of  the  evolution  of  the
whole  Vardar  Zone  is  given,  without  consideration  of  the
geological  history  of  its  segments,  because  there  were  not
any  and  still  are  no  sufficient  paleomagnetic  data.  The  only
thing  mentioned  is:  “Occurrence  of  two  ophiolitic  mélang-
es  –  Jurassic  and  Upper  Cretaceous  –  points  to  a  very  in-
tricate  history  of  the  ocean  closing  –  the  main  at  the  end  of
the  Jurassic,  with  subsequent  opening  of  a  back-arc  basin
between  the  main  land  and  the  Kopaonik  arc.”  (Dimitrijević
2000,  p. 12).

Fig. 2.  Kopaonik  Block  of  the  External
Vardar  Subzone  (simplified  after  Dimi-
trijević  1995,  1997,  2001,  and  modified
according  to  Karamata  1995;  Karamata
et al. 2000). 1 – Miocene and Pliocene
sediments;  2  –  Oligocene-Miocene
granodiorites;  3  –  Tertiary  volcanic
rocks; 4 – Binačka Morava Oligocene;
5  –  Cretaceous  deposits  (a  –  Upper
Cretaceous  deposits  of  the  Kopaonik
Block;  b  –  Kačanik  Flysch);  6  –  ultra-
mafites; 7 – ophiolitic mélange (a – un-
metamorphosed  mélange  of  the  western
margin  of  the  KBRU  (KB)  and  the
VZWB;  b  –  slightly  metamorphosed
mélange  of  the  eastern  margin  of  KB);
8 – Triassic metamorphites; 9 – Pale-
ozoic  metamorphites;  10  –  western
boundary  of  the  Kb  within  KBRU  (in
sense  of  Karamata  1995  and  Karamata
et  al.  2000);  11  –  first  order  thrust
faults: boundaries of the External Vard-
ar Zone; 12 – nappe boundaries within
the External Vardar Zone; 13 – normal
faults; 14 – sedimentary contacts. Con-
odont  localities:  A  –  locality  Županj
(“Central Kopaonik Series”); B – local-
ity  Smrekovnica  (“Metamorphic  Trepča
Series”).

A more detailed discussion on the geological evolution

of these areas was given by Karamata (1995), Karamata et
al. (2000), and Resimić-Šarić et al. (2000).

Both authors (M.D. Dimitrijević and S. Karamata) start

from  the  fact  that  the  present  Vardar  Zone  is  one  of  the
three  different  Mesozoic  ophiolitic  belts  which  exist  in
the  central  part  of  the  Balkan  Peninsula,  and  that  as  such,
it  is  the  relic  of  the  main  oceanic  realm  –  the  Vardar
Ocean,  which  formed  the  NW  part  of  the  (Neo)Tethys.  S.
Karamata  and  co-authors  are  of  the  opinion  that  the  Vardar
Zone  includes  the  relics  of  (at  least)  two  oceanic  areas:
(a)  the  remnants  of  the  Main  Vardar  (Tethys)  Ocean  (now
the  Main  Vardar  Zone  –  MVZ)  in  the  east,  and  (b)  for-
mations  of  the  western  branch  (i.e.  scar  of  a  marginal  ba-
sin  or  sea)  of  the  Vardar  Ocean  (now  the  Vardar  Zone

161

METAMORPHOSED AND DUCTILELY DEFORMED CONODONTS (SERBIA—NE HUNGARY)

Western  Belt  –  VZWB)  in  the  west.  The  KBRU  (Kb)
which  formed  during  the  Upper  Triassic  and  at  the  begin-
ning  of  the  Jurassic,  had  previously  been  an  integral  part
of  a  continental  margin  at  the  side  of  a  large  Vardar
(Tethys)  Ocean.  Uplifting  of  the  KBRU  (Kb)  has  been  go-
ing  on  till  present  times.  However,  its  complex  evolution
resulted  in  formation  of  various  rock  complexes  such  as
ophiolitic  mélanges,  Upper  Cretaceous  deposits,  as  well  as
large  masses  of  ultramafic,  volcanic  and  granodioritic
rocks.  The  main  characteristics  of  the  above  mentioned
oceanic  basins  are  as  follows:

a) The Main Vardar Ocean (MVO, present MVZ) – long

continuous  existence  as  the  continuation  of  an  Early  Pale-
ozoic  (or  older?)  oceanic  realm  (e.g.  of  Paleotethys);  clos-
ing  at  the  end  of  the  Jurassic;  presence  of  Paleozoic  island
arc  relics  (“Veles  Series”);  prevalence  of  material  from  the
higher  parts  of  the  oceanic  crust  (mafic  i.e.  basaltic  rocks),
cherts  and  lithic  sandstone  in  the  olistostrome;  absence  of
limestone  olistoplakae;  and

b) Western basin of the Vardar Ocean (VOWB, present

VZWB)  (which  originated  simultaneously  with  the  closure
of  the  MVO,  and  was  during  Jurassic  and  Cretaceous,  the
most  important  oceanic  realm  in  the  central  part  of  the
Balkan  Peninsula)  –  existence  from  the  Late  Triassic  to
the  latest  Cretaceous  with  very  long  and  complex  closing
with  formation  of  island  arcs,  obduction  of  ultramafic
masses  and  development  of  huge  masses  of  olistostromes.
The  olistostromes  formed  in  the  trench  by  the  closure  of
the  basin  are  characterized  by  predominance  of  sandstones
and  basalts  (MORB  and  IAB  affinity),  and  presence  of
cherts  (Upper  Triassic  and  younger),  and  limestone  olis-
toliths  of  Middle—Late  Triassic,  Late  Jurassic  and  Late
Cretaceous  age.

Fig. 3.  Schematic  tectonic  cross-section  of  the  Vardar  Zone  in  the  northern  area  of  Kopaonik  Mt  (slightly  modified  after  Grubić  et  al.
1995).  1  –  Oligocene  granodiorites;  2  –  ultramafites;  3  –  Upper  Cretaceous  deposits  of  the  Kopaonik  Block  (KB)  i.e.  Kopaonik  block
(Kb);  4  –  Cretaceous  paraflysches/flysches:  a  –  Lower  Cretaceous  paraflysch  of  the  Central  Vardar  Subzone  (CVSZ)  i.e.  Main  Vardar
Zone (MVZ); b –  Upper Cretaceous Toplica flysch of the Internal Vardar Subzone (IVSZ) i.e. MVZ; 5 – ophiolitic mélange of the west-
ern margin of the KB i.e. Kb (Kopaonik Block and Ridge Unit (KBRU)) and the Vardar Zone Western Belt (VZWB) – unmetamorphosed;
6 – ophiolitic mélange of the eastern margin of the KB i.e. Kb (KBRU) and the MVZ – slightly metamorphosed; 7 – Triassic and Paleo-
zoic metamorphites ( + “Studenica slice”-type); 8 – deposits of the Drina—Ivanjica Element/Terrane (DIE); 9 – metamorphites of the Ser-
bo-Macedonian  Composite  Terrane  (SMCT).  2,  5,  6, 7.  thrusts,  Late  Jurassic  structures  of  Western  and  Central  Kopaonik;  2,  3,  4,  6.  Late
Cretaceous structures of Eastern Kopaonik.   EVSZ  (External Vardar Subzone), KB, CVSZ, IVSZ – in the sense of Dimitrijević (1997);
VZWB, KBRU, Kb, MVZ – in the sense of Karamata et al. (2000).

According to the data by Dimitrijević (1995, 1997,

2000, 2001), Karamata (1995), and new observations, the
Kopaonik Mt region is composed of the following units
(Fig. 2):

a) (low-grade) metamorphic rocks of (Late?) Paleozoic

age  composed  of  the  clastic  sediments  metamorphosed  to
sericite-chlorite  schists,  metasandstones,  and  rare  chlorite-
epidote-actinolite  schists,  metabasalts  and  calcschists;

b) (very low-grade) metamorphic rocks of Triassic age

represented  by  schistous  and  intensely  folded  clayish-silty
or  sandy  rocks  and  deep-water  grey,  cherty  limestones
with  nodules  and  rare  beds  of  cherts;  intraserial  basaltic
lava  flows  (now  metabasalts)  and  small  intrusive  diabase
bodies  occur  with  these  sediments  only  locally;

c) ophiolitic mélange representing a typical olistostromal

mixture  of  clasts  and  olistoliths  of  different  sediments  and  ig-
neous  rocks  in  a  sandy  to  silty-clayey  matrix.  In  this  unit  two
facies  can  be  distinguished:

) the mélange at the eastern margin of the area, of Ju-

rassic age, slightly metamorphosed, with plenty of
basaltic fragments;

) the mélange at the western margin of the Kopaonik

block  (in  the  Ibar  valley),  of  Jurassic—Cretaceous
age,  where  the  sandstones  dominate  over  all  other
sedimentary  and  magmatic  rocks  together;

d) Cretaceous sediments, including the Upper Cretaceous

deposits of the Kopaonik Block, and the Kačanik Flysch;

e) very large bodies of ultramafic rocks (mostly

harzburgites) thrusted over all the aforementioned forma-
tions during the Eocene—Lower Oligocene;

f) volcanics, of andesitic, dacitic and quartzlatitic (rhy-

olitic-dacitic) composition, of Oligocene—Miocene (Tertia-
ry) age with associated granodiorites which were intruded

162

SUDAR and KOVÁCS

during the same time period into the core of the Kopaonik
block and formed a large contact metamorphic aureole;

g) marine Middle Oligocene at the south, the so-called

Binačka Morava Oligocene; and

h) Miocene and Pliocene lacustrine deposits.
In the Kopaonik area Triassic slightly metamorphosed

sediments  (with  rare  volcanics  and  in  this  case  by  Dimitr-
ijević  1995  treated  as  “volcanogenic-sedimentary”  forma-
tion)  are  widely  developed,  especially  at  the  Central
Kopaonik  and  in  the  region  of  Trepča,  and  few  “series”
were  distinguished,  mostly  locally  named,  as  at  the  north
the  “Central  Kopaonik  Series”  or  “Suvo  Rudište  Series”,
and  at  the  south  the  “Metamorphic  Trepča  Series”,  or  the
“Stari  Trg  Series”,  etc.  All  these  metamorphic  rocks,  as
well  as  those  occurring  on  Željin  and  Goč  (“Goč”,  “Žel-
jin”  and  “Banjski  Kopaonik”  “Series”),  and  those  devel-
oped  west  of  the  Ibar  river  (“Studenica  Series”,  “Rogozna”
and  “Golija”  “Series”  and  “Radočelo”  and  “Čemerno”
“Series”),  which  are  also  partly  Paleozoic  in  age,  are  con-
sidered  by  Grubić  (1995)  and  Grubić  &  Protić  (2000)  as
equivalents  of  the  Alpine  “schistes  lustres”  of  Piemont-
type  formed  in  deep-water  conditions.  In  the  above  men-
tioned  papers  the  problems  concerning  their  origin,
development  and  age  are  considered  in  detail,  and  inter-
ested  readers  can  find  more  data  in  them.

S. Karamata (pers. commun.) considers all these rock se-

ries  as  deposits  of  the  continental  slope  at  the  margin  of
the  Vardar  Ocean,  that  is  the  subsided  margin  of  the  intra-
oceanic  Drina-Ivanjica  carbonate  platform  (Dimitrijević  &
Dimitrijević  1991).

After the discovery of conodonts in slightly metamor-

phic  rocks  of  the  northern  (in  the  “Central  Kopaonik  Se-
ries”,  Mićić  et  al.  1972),  and  the  southern  Kopaonik
(“Metamorphic  Trepča  Series”,  Klisić  et  al.  1972),  the  Late
Triassic  age  of  some  of  their  parts/levels  was  firstly  docu-
mented.  According  to  the  determined  conodont  fauna
(only  platform  conodonts  are  cited  here:  Gondolella  nav-
icula,  Neogondolella  abneptis,  Neogondolella  tethydis),
and  the  current  knowledge  on  their  stratigraphic  range,  it
was  determined  that  the  Carnian  Stage  was  present  in  both
“series“.  On  the  basis  of  the  original  material  on  which  the
above  mentioned  results  considering  the  age  of  certain
parts  of  the  metamorphic  rocks  on  Kopaonik  Mt  were
based,  and  according  to  his  own  material,  Sudar  (1986)
made  a  revision  to  the  conodonts  and  their  age.  Thus,  the
new  data  confirmed  their  Carnian  age,  and  the  presence  of
a  Norian  Stage  in  the  metamorphites  was  determined  for
the  first  time.  Besides,  biostratigraphic  divisions  of  the
sediments  into  conodont  zones  were  also  performed.

The specific “Central Kopaonik Series” (“CKS”) occur all

around  the  Kopaonik  granodiorite  massif  and  is  composed
of  phyllitoids  (dominantly  sericite-chlorite  schists),  chlo-
rite-epidote-actinolite  schists,  and  (particularly  in  higher
horizons)  thin-bedded  crystalline  limestones.  These  grey,
cherty  limestones  occur  either  as  the  middle  horizon  with
interlayers  of  pelitic-psammitic  rocks,  or  as  interlayers
within  the  uppermost  horizon  of  the  “series”  made  of  ter-
rigenous  (meta)sediments.  The  parent  rocks  were  shales,
marls,  and  carbonates,  subordinately  sandstones,  with

consedimentary magmatic rocks: basalt (spilite), diabase,
dolerite, and tuff.

NW of the village Županj at the right side of the river

Jošanička  Reka  (about  2 km  along  the  road  Jošanička
Banja-Biljanovac,  Fig. 2)  in  the  limestone  interlayers  in
the  higher  levels  of  the  “series”,  the  following  Carnian
conodonts  were  found  (conodont  determination  and  zona-
tion  from  Kopaonik  Mt  was  made  by  M.  Sudar,  according
to  the  taxonomic  concept  and  biozonal  subdivision  by
Budurov  &  Sudar  1990):

a) Epigondolella echinata, Paragondolella navicula,

and Pg. polygnathiformis – Paragondolella polygnathi-
formis Zone (middle Cordevolian, Julian, lower Tuvalian);

b) Pg. nodosa and Pg. polygnathiformis – Paragon-

dolella nodosa Zone (lower and upper Tuvalian).

The “Metamorphic Trepča Series” (“MTS”) covers an

area of about 30 km

between Trepča and Smrekovnica (vi-

cinity  of  Kosovska  Mitrovica,  Fig. 2)  and  its  lower  part  is
composed  of  phyllitoids,  argillaceous  schists,  cherts,
gneisses,  feldspathic  micaschists,  amphibolite  and  amphib-
ole  schist,  and  in  the  middle  part  of  the  unit,  the  Smrekovni-
ca  limestones.  This  metamorphic  rock  “series”  contains
abundant  basaltoid  sills  and  lava  flows  of  spilitic  character.

The following Lower and Middle Norian conodonts were

found  at  a  few  places  in  the  neighbourhood  of  Smre-
kovnica  in  100—150 m  thin-bedded  grey  cherty  Smre-
kovnica  limestones,  with  intercalated  platy  cherts  in  lower
levels  and  with  abundant  clayey  interlayers:

a) Ancyrogondolella triangularis, Metapolygnathus ab-

neptis, Mp. communisti, Pg. navicula, and Pg. steinber-
gensis – Metapolygnathus abneptis Zone (Lacian);

b) Ag. triangularis, Eg. postera, Mp. abneptis, Pg.

hallstattensis, and Pg. steinbergensis – Epigondolella
postera Zone (Alaunian).

Geological framework of the Bükk Mountains and neigh-
bouring units

Bükk nappe system (Bükk Composite Terrane)

The south-vergent nappe system of the Bükk Mts and

adjacent  Darnó  Hill  area  at  the  NE  part  of  the  Mátra  Mts
are  built  up  by  the  following  units:  the  Bükk  Parautoch-
thon  Unit  (Bükk  PA  Unit)  in  the  lowermost  position  and
the  Szarvaskő  and  Darnó  Ophiolite  Complexes  emplaced
onto  it  from  the  NW  according  to  present  coordinates
(Figs. 4  and  5).  However,  taking  into  account  the  large-
scale  Tertiary  anti-clockwise  rotation  (up  to  90

) of the

Bükk  block,  the  original  direction  of  nappe-stacking
should  have  been  from  the  NE  to  SW,  the  same  as  in  the
Dinarides  (see  Csontos  1999  and  references  therein).  The
subsurface  continuation  of  the  Bükk  Composite  Unit  in
the  basement  of  the  northern  Pannonian  Basin  is  bound
by  the  Zagreb-Zemplín  (or  Mid-Hungarian)  Lineament
on  the  south  and  the  Hernád  fault  on  the  east.  On  the
west,  towards  the  Transdanubian  Range  Unit  the  bound-
ary  is  not  clear,  as  there  could  also  be  a  facies  transition.
Towards  the  north  it  will  be  discussed  below  at  the  Up-
pony  and  Szendrő  Units.

163

METAMORPHOSED AND DUCTILELY DEFORMED CONODONTS (SERBIA—NE HUNGARY)

Fig. 4. Structural units in NE Hungary with vergence directions of the nappes.
1—4 – Bükk Mts and Darnó Hill: 1 – Szarvaskő and Darnó Ophiolite
Complexes; 2 – Jurassic formations of the Bükk PA Unit; 3 – Triassic
formations of the Bükk PA Unit; 4 – Upper Paleozoic formations of the
Bükk PA Unit; 5—6 – Szendrő Unit: 5 – Abod Subunit; 6 – Rakaca
Subunit; 7—9 – Uppony Unit: 7 – Tapolcsány Subunit; 8 – Lázbérc Subunit;
9 – Upper Cretaceous Gosau-type conglomerates; 10—12 – Aggtelek-
Rudabánya Mts: 10 – Aggtelek Unit: s.l.; 11 – Bódva ( + Szőlősardó Unit );
12 – Martonyi (or Torna s.s.) Unit; 13 – Bódva Valley Ophiolite Complex
(in boreholes); 14 – Upper Jurassic (?) rhyolites; 15 – structural vergencies.

The exposed part of the Bükk PA Unit is built up by

four large, S-ward recumbent antiforms and strongly
sheared-off synforms between them. Its known stratigraph-
ic sequence extends from the Middle Carboniferous
Variscan flysch to the Upper Jurassic Eohellenic flysch
(for most the recent reviews see Haas 2001 and Filipović
et al. 2003). Following the Late Paleozoic to Early Trias-
sic marine sedimentation (with a hiatus in the Early Permi-
an and coastal plain sediments at the beginning of the
Alpine cycle in the Middle Permian), a carbonate ramp en-
vironment came into existence during the Anisian. After a
significant (mostly andesitic) volcanic activity in the La-
dinian, the former ramp desintegrated and platform and
basin environments were differentiated during the Late

Triassic. In the course of the Late Jurassic (?)—Ear-
ly Cretaceous Eohellenic tectogenesis (160—120 Ma,
Árkai et al. 1995) the antiforms were formed from
the areas of Late Triassic carbonate platforms,
whereas the sheared-off synforms developed from
the basinal carbonates (grey, cherty limestones;
Felsőtárkány Limestone Formation) (Csontos
1988, 1999). The conodonts involved in the
present study are from the latter. In the most com-
plete section studied (borehole Felsőtárkány 7)
the basinal carbonate sequence extends from the
basal Carnian (“Metapolygnathus” diebeli Zone,
together with Gondolella polygnathiformis) to
the Rhaetian (Neospathodus posthernsteini Zone)
(Kovács in Velledits 2000).

The emplacement of the Szarvaskő Ophiolite

Complex onto the Bükk PA Unit is supposed to
have taken place during the latest Jurassic and
large-scale folding, resulting in the formation of
the antiforms—synforms mentioned above, al-
ready affected both units together, accompanied
by the first (and likely more intense) metamor-
phic event (Csontos op. cit.; Fig. 6 herein).

The east-west striking axis of the antiforms

plunges to the west. Consequently, stratigraphi-
cally older and more metamorphosed sequences
are exposed to the east, whereas younger (Juras-
sic) and less to non-metamorphosed ones appear
to the west. The rocks exposed in the eastern and
central parts of the Bükk Mts are high tempera-
ture anchizonal to epizonal metamorphosed
( ~ 350

C and 300 MPa in average, but reaching

up to 500 MPa in some zones; Árkai 1983). The
degree of metamorphism and style of deformation
suggest, that these processes took place at 5 to
10 km depth (Papanikolaou pers. commun. on the
field in 1993). A second tectonometamorphic
event (85—90 Ma) can be recognized in the NE
part of the Bükk Mts. It is thought to be linked
with NW-SE directed strike-slip faulting and
arching of the unit (Csontos op. cit.), as well as
with the emplacement of the intra-Bükkian, but
non or only weakly metamorphosed Kisfennsík

Fig. 5. Structural sketch of the Bükk Composite Terrane (after Haas
& Kovács 2001, slightly modified). U – Unit; Bükk PA U – Bükk
Parautochthon Unit.

164

SUDAR and KOVÁCS

(Little Plateau) partial unit (Forián-Szabó & Csontos 2002).
Similarly non or weakly metamorphosed intra-Bükkian
Triassic occurs below the Szarvaskő Complex to the
west, in the vicinity of Felsőtárkány (Velledits 2000),
which likely represents the highest part of the Bükk PA
Unit, not removed by erosion. The Szarvaskő Complex
was affected by low temperature anchizonal (pumpelly-
ite-prehnite facies) metamorphism (Árkai 1973, 1983;
Sadek et al. 1996).

Upper Eocene shallow-marine deposits at the base of the

Tertiary cover sequence postdate any metamorphic or duc-
tile deformational event in the Bükk Mts.

Uppony and Szendrő Units

These units were previously regarded because of facial

and stratigraphic links as part of the “Bükkium” (see, for
example, Árkai 1983; Kovács & Péró 1983). However,
they have a N-vergent structure, opposite to that of the
Bükk PA Unit, therefore they can no longer be considered
to form parts of the same tectonostratigraphic unit (cf.
Kovács et al. 2000). They are separated from the Bükk PA
Unit by the Nekézseny fault and its supposed E-ward con-
tinuation (Fig. 4).

The Uppony Unit of small surface areal extension is

built almost exclusively of Paleozoic formations and is
enclosed entirely within the Darnó fault zone (Fig. 4). For
its stratigraphy we refer to Kovács (1992) and Ebner et al.
(1998). As opposed to the Bükk PA Unit and related ophi-
olitic units, it has a N-vergent structure. The Paleozoic
rocks were affected by a mid-Cretaceous (118 ± 14 Ma)
tectonometamorphic event (Árkai et al. 1995), with meta-
morphic conditions reaching the boundary zone between
the anchizone and epizone (350

C, ~ 250 MPa; Árkai

1983). Upper Cretaceous Gosau-type sediments, covering
the southern part of the unit, postdate this event.

The Szendrő Unit is built up exclusively by Paleozoic

(Silurian?—Devonian—Carboniferous) formations and also
has a N-vergent structure (Fig. 4). For details on its stratig-
raphy we refer to Kovács (1992) and Ebner et al. (1998).
Facially, it appears to be linked with the Bükk Upper Pale-
ozoic, however, their different vergencies point to a clear
structural distinction (Kovács et al. 2000). The Paleozoic
rocks were affected by a mid-Cretaceous (108 ± 8

Ma) tec-

tonometamorphic event (Árkai et al. 1995) of greenschist
facies, or epizonal conditions ( ~ 400

C, ~ 300 MPa; Árkai

1983). It indicates the chlorite isograde, however, in some
parts even the biotite isograde (min. 450

C) was recorded

(Árkai op. cit.).

Aggtelek-Rudabánya Units

The Aggtelek-Rudabánya Units include the non-meta-

morphosed Aggtelek and Bódva Units and the metamor-
phosed Torna s.s. or Martonyi Unit (Grill et al. 1984; Less
2000; Fig. 4 herein). They are formed by Upper Permian to
Jurassic, but mainly Triassic formations (Kovács et al.
1989). The dismembered ophiolites (serpentinites, gab-
bros, basalts, some radiolarites and siliceous shales) do not
form a distinct structural unit, but occur in the sole-thrust
of the Aggtelek Unit, imbricated as isolated bodies/slices
into Upper Permian evaporites (Réti 1985), as shown by
borehole evidence.

The Aggtelek and Bódva Units were affected only by

diagenetic alterations, whereas the Torna s.s. or Martonyi
Unit by anchizonal to epizonal metamorphism of medi-
um pressure ( ~ 350

C, ~ 700 MPa; Árkai & Kovács

1986). The age of the tectonometamorphic event is poor-
ly constrained, but appears to be also of Early to middle
Cretaceous age (128 and 115 Ma, respectively; Balogh
Kad. 1991 in Kovács et al. 2000). The ductile deforma-
tional history of the Martonyi Unit along a NNW—SSE

Fig. 6. Structural cross-section of the western part of Bükk Mts, through the Szarvaskő synform (after Gulácsi, in Haas 2001, slightly
modified).

165

METAMORPHOSED AND DUCTILELY DEFORMED CONODONTS (SERBIA—NE HUNGARY)

section,  with  obviously  southward  overturned  setting,
was  presented  by  Fodor  &  Koroknai  (2000).  The  Ag-
gtelek  and  Bódva  Units  show  a  southward  thrust  and
folded  structure,  but  northward  backthrusts  are  also  rec-
ognizable  (Péró  et  al.  2002,  2003).

Metamorphosed Upper Triassic (Carnian-Norian) grey,

cherty  limestones  of  the  Torna  s.s.  or  Martonyi  Unit,  re-
ferred  to  as  “metamorphosed  Pötschen  Limestone  Forma-
tion”  (Kovács  et  al.  1989),  are  of  particular  importance  for
our  comparison,  because  the  metamorphosed  conodonts  of
the  same  age  from  the  Kopaonik  Mt  presented  herein,  and
those  from  other  territories  of  the  former  Yugoslavia  (see
below)  derive  from  similar  lithologies.  Such  limestones  in
the  Bükk  PA  Unit  are  called  “Felsőtárkány  Limestone  For-
mation”  s.l.  (Haas  2001).

Conodont alterations

Colour alteration indices (CAI), recrystallization and duc-

tile deformation of conodonts in the units from Serbia and
NE Hungary are discussed and compared in this chapter.

Serbia

Kopaonik, metamorphosed Upper Triassic limestones

The Upper Triassic conodonts from the Kopaonik Mt

included  in  this  study  come  from  two  localities:  Smre-
kovnica  (“MTS”),  in  the  southern  part  and  Županj
(“CKS”),  in  the  northern  part  of  the  mountains.  The  illus-
trated  ones  (Figs. 7—9)  are  all  from  the  former  locality.

The colours of the conodonts from both localities are

partly  black  to  dark  grey  (CAI = 5  to  5.5),  partly  grey  to
white  (CAI = 6  to  7).  In  some  samples  the  former,  in  some
others  the  latter  predominate.  However,  CAI  values  5—6—7
(black—grey—white)  may  occur  not  only  within  the  same
sample,  but  even  within  different  parts  of  the  same,  recrys-
tallized,  usually  fractured  and  deformed  specimen  (Kovács
&  Árkai  1987).  An  example  concerning  recrystallization  is
shown  in  Fig. 10.1—4  herein:  the  middle  part  of  the  carina
shows  CAI = 7  (Fig. 10.1,2),  while  the  anterior  part  CAI = 6
(Fig. 10.3,4),  without  remarkable  difference  in  the  degree
of  recrystallization.

All of the conodont specimens involved into the present

study  are  considerably  recrystallized  and  usually  ruptured
by  minor  cracks,  which  did  not  result  in  their  complete
breaking  apart.  The  degree  of  recrystallization  was  analy-
sed  on  the  same  parts  (middle  or  anterior  part)  of  the  carina
of  selected  specimens  at  standard  SEM  magnifications:
1000   and  3000   (see  Figs. 10  and  12).  Apatite  grain  size
on  these  photos  could  be  measured  between  0.83  and  9.66
micrometers,  in  average  4.42  micrometers.

Many of the specimens show ductile deformation, evi-

dently  in  accordance  with  the  development  of  the  folia-
tion  and  texture  with  preferred  orientation  of  their
enclosing  metamorphosed  limestone/marble  host  rock.  In
some  cases  they  show  extreme,  crook-like  (Fig. 7.8—11;
Fig. 9.1—3),  or  even  accordion-like  (Fig. 9.4—6)  bending.

NE Hungary

Bükk Parautochthon Unit

The first report on the presence of metamorphosed, re-

crystallized  and  deformed  conodonts  in  the  NE  part  of  the
Bükk  Mts  was  given  by  Kozur  &  Mock  (1977).  Detailed
metamorphic  petrologic  study  of  low-  to  very  low-grade
metamorphosed  rocks  of  the  NE  part  of  the  mountains  was
presented  by  Árkai  (1983)  (for  earlier  works  see  references
therein).  Although  metamorphic  alteration  of  conodonts
was  compared  to  the  metamorphic  petrological  parameters
of  other  units  of  NE  Hungary  by  Árkai  &  Kovács  (1986),
and  Kovács  &  Árkai  (1987,  1989),  such  a  comparative
work  for  the  Bükk  PA  Unit  has  not  been  presented  up  to
now.  A  number  of  samples  were  analysed  for  conodonts
from  the  central  and  SE  part  of  the  mountains  (the  latter
being  not  accessible  for  geological  studies  before  1990)
by  S.  Kovács  in  collaboration  with  G.  Nagy  and  P.  Pelikán
during  the  field  works  of  the  recently  published  geological
map  of  the  Bükk  area  (Less  et  al.  2002),  which  have  also
been  unpublished  so  far.  In  the  present  contribution  we  pro-
vide  a  brief  summary  of  metamorphic  alterations  of  con-
odonts  of  Upper  Triassic  cherty  limestones  (Felsőtárkány
Limestone  Formation  s.l.;  for  areal  distribution  see  Less  et
al.  2002)  and  compare  them  with  those  of  the  Kopaonik  Mt.

These cherty limestones in the NE, central and SE part

of  the  mountains,  where  the  structurally  deeper  parts  of  the
E—W  striking,  W-ward  plunging  antiforms  are  exposed,  are
strongly  schistose  and  folded,  with  even  macroscopically
clearly  visible  S

and locally S

schistosity (cf. Németh &

Mádai  2003),  the  latter  resulting  in  characteristic  S/C
structures  (Koroknai  pers.  commun.).  Conodonts  here  are
strongly  recrystallized  (Fig. 12.3—6),  of  greyish-whitish
colour  (CAI = 6—7),  but  often  of  completely  white  colour
(CAI = 7)  and  strongly  sheared-deformed  (Fig. 11).  Evi-
dently,  their  ductile  deformation  was  first  of  all  related  to
the  development  of  the  S

schistosity, although the S

could  also  contribute  to  their  deformation.  At  the  south-
easternmost  part  of  the  mountains,  however,  conodonts  are
mostly  black  to  dark  grey  coloured  (CAI = 5—5.5),  less  re-
crystallized  and  non-deformed.  In  this  latter  area  the  struc-
turally  higher  parts  of  the  southernmost  antiforms  may  be
exposed.  However,  metamorphic  petrologic  investigations
from  this  area  are  still  missing  and  precise  thermobaromet-
ric  evaluations  are  not  yet  available.

Triassic limestones occurring in the SW Bükk Mts be-

low  Jurassic  rocks  (the  latter  belonging  mostly  to  the
“Szarvaskő-Mónosbél  nappes”  in  the  sense  of  Csontos
1988)  show  only  weak  or  no  foliation  at  all  (cf.  Velledits
&  Péró  1987;  Velledits  2000).  Conodonts  from  the  type
section  of  the  Felsőtárkány  Limestone  Formation  (bore-
hole  Felsőtárkány  7),  extending  in  age  from  the  basal
Carnian  to  the  Rhaetian  (Kovács  in  Velledits  op. cit.),
are  black  (CAI = 5),  not  recrystallized  and  not  deformed.
Together  with  the  limestone  textures  they  would  indicate
the  boundary  interval  of  diagenesis  and  regional  meta-
morphism  or  the  low  temperature  part  of  the  anchizone.
This  is  in  accordance  with  metamorphic  petrologic  pa-

167

METAMORPHOSED AND DUCTILELY DEFORMED CONODONTS (SERBIA—NE HUNGARY)

Fig. 8.  Metamorphosed,  recrystallized  and  deformed  conodonts  from  Upper  Triassic  Smrekovnica  Lms.  (Norian,  Lacian  and  Alaunian,
Metapolygnathus  abneptis  and  Epigondolella  postera  Zones)  of  the  “Metamorphic  Trepča  Series”,  Smrekovnica,  Kopaonik  Mt,  Vardar
Zone,  Serbia.  1—6  –  Metapolygnathus  abneptis  (Huckriede,  1958).  1—3  –  CAI  6—7,  extremely  elongated  specimen,  No. 4/MS  872,
Metapolygnathus  abneptis  Zone.  4—6  –  CAI  6—7,  specimen  with  a  strongly  curved  anterior  part  of  carina,  No. 6/MS  882,  Epigondolella
postera Zone.  7—10 – Paragondolella hallstattensis Mosher, 1968. CAI 6—7, double twisted specimen, No. 10/MS 880, Metapolygnathus
abneptis Zone. Scale bar = 100  m (magnification: 200 ).

Árkai  et  al.  (1981).  Correlation  with  metamorphic  alter-
ation  of  conodonts  was  briefly  given  in  Kovács  &  Árkai
(1987),  with  some  specimens  illustrated.  This  latter  we
just  summarize  here,  for  comparison  with  previously  un-
described  alteration  of  conodonts  from  the  Kopaonik  and
Bükk  Mts.

Conodonts of the Szendrő Paleozoic (from Middle De-

vonian  to  Middle  Carboniferous,  e.g.  up  to  Early  Bashkiri-
an)  are  mostly  light  grey  to  white  coloured  (CAI = 6—7,
usually  within  the  same  specimen),  strongly  recrystal-
lized  and  often  deformed.  However,  in  some  samples,  es-
pecially  those  from  the  Upper  Visean  to  Lower  Bashkirian
Verebeshegy  Limestone  Member,  all  the  specimens  were

black  (CAI = 5),  but  similarly  strongly  recrystallized  and
deformed  (cf.  Kovács  &  Árkai  1987,  Pl. 13.4,  Figs. 3—6;
Pl. 13.5,  Figs. 6—10).

Conodonts of the limestone formations of the Up-

pony  Paleozoic  (from  the  Upper  Devonian  to  Middle
Carboniferous,  e.g.  from  Frasnian  to  Early  Bashkirian)
are  black  (CAI = 5),  less  recrystallized  and  not  deformed
(cf.  Kovács  &  Árkai  1987,  Pl. 13.4,  Figs. 1—2).  Con-
odonts  from  older  limestone  blocks  of  olistostromal  for-
mations  show  even  higher  CAI  values  (6—7),  but  they
are  not  recrystallized  and  free  of  any  deformation;  be-
cause  of  their  specific  conditions  of  preservation  they
are  not  considered  here  for  comparison.

168

SUDAR and KOVÁCS

Fig. 9.  Metamorphosed,  recrystallized  and  deformed  conodonts  from  Upper  Triassic  Smrekovnica  Lms.  (Norian,  Alaunian,  Epigondolella
postera  Zone)  of  the  “Metamorphic  Trepča  Series”,  Smrekovnica,  Kopaonik  Mt,  Vardar  Zone,  Serbia.  1—3  –  Ancyrogondolella  triangu-
laris  Budurov,  1972.  CAI  6,  extremely  deformed  specimen  from  sinistral  sheared  regime,  No.  9/MS  885.  4—6  –  Metapolygnathus  ab-
neptis (Huckriede, 1958). CAI 6, complexly bent specimen in a accordion-like form, almost unrecognizable, No. 8/MS 885. Scale bars for
figs. 1, 2 = 100  m (magnification: 172 ); for fig. 3 = 100  m (magnification: 156 ); for figs. 4—6 = 100  m (magnification: 200 ).

Aggtelek-Rudabánya Mountains

Conodont alteration in the tectonostratigraphic units of

the  Aggtelek-Rudabánya  Mts  and  their  correlation  with
metamorphic  petrologic  parameters  were  described  in  de-
tail  in  Árkai  &  Kovács  (1986)  and  Kovács  &  Árkai  (1987,
1989).  Those  of  the  non-metamorphosed  Aggtelek  and
Bódva  Units  are  of  light  brownish-grey  to  dark  grey
(CAI = 2  to  4,  5),  exceptionally  black  colour  (CAI = 5).  They
can  show  a  corroded  surface,  but  lack  features  of  recrystalli-
zation  or  deformation.  According  to  illite  “crystallinity”  in-
dices  both  (except  the  specific  Telekesoldal  Subunit)  were
not  affected  by  a  temperarure  higher  than  200

Conodonts of the epizonal (Esztramos) and high tempera-

ture  anchizonal  (surrounding  of  Hidvégardó—Becskeháza—
Tornaszentjakab;  Becskeháza  Subunit  in  sense  of  Less
2000)  partial  units  of  the  Torna  s.s.  (or  Martonyi)  Unit,  ex-
posed  in  NE  part  of  Rudabánya  Mts,  are  light  grey  to  white
coloured  (CAI = 6—7),  strongly  recrystallized  and  deformed
(see  Kovács  1986,  Pls. 4—9  and  13;  Kovács  &  Árkai  1987,
Pl. 13.2,  Figs. 5, 6  and  Pl. l3.5,  Figs. 1—5;  Kovács  &  Árkai
1989,  Pl. 3,  Figs. 3—6,  Pl. 4,  Figs. 2, 4, 6, 7).  Especially

strongly  sheared,  flattened  specimens  are  completely  whit-
ened;  samples  with  such  conodonts  likely  indicate  zones
of  intense  ductile  shearing.  These  partial  units  endured  a
medium-pressure  metamorphism  (Árkai  &  Kovács  1986).
However,  from  the  region  between  Bódvarákó  and  Marto-
nyi  (Bódvarákó  and  Martonyi  s.s.  Subunits;  Fodor  &  Ko-
roknai  2000)  samples  collected  mainly  by  Gy.  Less
yielded  conodonts,  which  are  black  (CAI = 5),  recrystal-
lized,  but  not  deformed.

Ductile deformation of limestones

Detailed studies on the ductile deformation of micritic

limestones  were  carried  out  by  Burkhard  (1990)  in  the
Swiss  Alps.  Accordingly,  plastic  deformation  of  such
limestones  may  begin  at  temperatures  as  low  as  150

However, it was found, that up to the temperature 300

the  dominant  deformational  mechanism  is  grain  boundary
sliding.  Crystallographic  preferred  orientation  and  fea-
tures  of  dynamic  recrystallization  are  missing  at  these
temperatures;  these  were  found  to  develop  above  300

170

SUDAR and KOVÁCS

At  these  higher  temperatures,  increase  in  grain  size  and
plastic  flow  by  twinning,  strongly  dependent  on  the  grain
size,  as  well  as  other  intracrystalline  slips  together  with
dynamic  recrystallization  result  in  well  developed  crystal-
lographic  textures,  such  as  preferred  orientation.

Kovács & Árkai (1987, 1989) empirically subdivided

limestone textures into three types, both for platform and
basinal facies.

T y p e A : Intact original microfacies, without any in-

cipient foliation or schistosity.

T y p e B : Incipient preferred orientation with micro-

scopically observable foliation or schistosity (generally

Fig. 11. Metamorphosed and deformed Upper Triassic (Carnian and Norian) conodonts from the Bükk Mts, NE Hungary. 1—3 – Gondolella
polygnathiformis Budurov et Stefanov, 1965. Carnian, road between Szinva Spring to Hollóstető, sample No. SzF-Ht-18. 4 – Metapolyg-
nathus  abneptis  triangularis  (Budurov,  1972).  Norian,  sample  Setétvölgy-3.  5  –  Metapolygnathus  abneptis  abneptis  (Huckriede,  1958).
Norian, base  of  cliff  Füzérkő.  6—12 –  Gondolella  steinbergensis  (Mosher,  1968).  Norian,  sample  Pazsag-1,  11,  12,  isoclinally  deformed,
crook-like specimens. Scale bar = 100  m (magnification: 100 ).

). Allochemical components (bioclasts, such as calcified

radiolarian  tests  or  pelagic  bivalve  shells  –  “filaments”)
are  still  recognizable,  although  they  are  flattened  into  the
plane  of  schistosity.  The  matrix  is  still  distinct,  usually
only  weakly  recrystallized  in  pelagic  limestones.

Type C: The original microfacies is completely obliter-

ated  by  recrystallization,  the  matrix  or  cement  cannot  be
distinguished  from  formerly  existing  bioclasts  or  intraclasts.
A  homogeneous  microsparitic  or  sparitic  texture  ( = meta-
sparite  or  marble)  is  formed,  with  well-expressed  preferred
orientation.  Only  large  grains  (such  as  echinoderm  frag-
ments)  are  still  distinct,  showing  intense  twinning.

172

SUDAR and KOVÁCS

This “type C” texture obviously corresponds to the one,

which forms at temperatures above 300

C in deformed

limestones according to Burkhard (1990).

Evidently, the recrystallization and ductile deformation

of conodonts took place in definite interaction with those
of the limestone host rock, that is above the 300

C mini-

mal temperature boundary.

For the investigations of the ductile deformation and il-

lite  “crystallinity”  of  limestones  from  the  Kopaonik  Mt,
samples  were  taken  only  from  the  Županj  (“CKS”),  be-
cause  the  deposits  of  the  Smrekovnica  (“MTS”)  in  the

Fig. 13.  Textures  of  metamorphosed  Upper  Triassic  grey,  cherty
limestones/marbles  from  the  Kopaonik  Mt,  Serbia.  Samples  were
taken  along  the  road  leading  from  Brzeće  to  Kopaonik  Sky  Center,
near  the  eastern  gate  of  Kopaonik  National  Park.  1  –  Marble  with
faint  developed  S

foliation, sample MS 1851. 2 – Marble with

well developed S

foliation, sample MS 1852. Scale bar = 1 mm

(magnification: 17.5 ).

Fig. 14. Textures of metamorphosed limestones from the Bükk Mts (1 and 2) and Szendrő Mts (3 and 4), NE Hungary. 1 – Grey, cherty
limestone (Lower Norian) from borehole Felsőtárkány 7, 83.0 m; radiolarian biomicrite with slight, incipient S

foliation. (Courtesy of F.

Velledits.) 2 – Grey, cherty limestone with well developed S

foliation; note the radiolarians strongly flattened into the plane of schistosi-

ty. Road cut along the road leading from Eger to Miskolc, between Hollós-tető and Lusta-völgy, sample B-1/1975. 3 – Upper Visean
Verebeshegy Limestone, western slope of Bátori-völgy; marble with well developed S

foliation and with crinoid fragments, sample Szrő-68.

4 – Upper Visean Verebeshegy Limestone, road curve SE of Rakacaszend; marble with well developed S

foliation, sample Szrő-62.

Scale bar = 1 mm (magnification: 17.5 ).

southern  Kopaonik  Mt  are  located  in  the  territory  of  Koso-
vo,  where  geological  investigations  have  not  been  possi-
ble  during  the  last  ten  years.

From the Kopaonik Mt, thin sections were made only

from  the  “CKS”  Upper  Triassic  grey  cherty  limestones
which  outcrop  on  the  eastern  slope  of  the  main  ridge  (on
the  first  curve  of  the  road  Brzeće—Kopaonik  Sky  Center
(Suvo  Rudište)  after  the  eastern  gate  of  the  Kopaonik  Na-
tional  Park).  They  show  strong,  rather  xenotopic  recrys-
tallization  with  well-expressed  preferred  orientation
(foliation/S

schistosity) and correspond to a higher de-

gree of type C metasparites/marbles (see Fig. 13).

The Upper Triassic grey cherty limestones of the anchi-

to  epizonal  metamorphosed  Bükk  PA  Unit  show  both  B
and  C  type  textures,  independently  from  the  degree  of  de-
formation  of  conodonts:  strongly  deformed  and  recrystal-
lized  specimens  may  occur  in  both  textures.  Similar
limestone  textures  and  deformed/recrystallized  conodonts
characterize  the  anchi-  to  epizonal  metamorphosed  Torna
s.s.  (or  Martonyi)  Unit  of  the  Aggtelek-Rudabánya  Mts
(for  details  see  Árkai  &  Kovács  1986;  Kovács  1986  and
Kovács  &  Árkai  1989)  (see  Fig. 14).

Illite “crystallinity”

Altogether 7 samples from crystalline cherty limestones

with  metaclastic  intercalations  were  analysed  by  X-ray
powder  diffractometry  in  the  Institute  of  Geochemical  Re-
search  of  the  Hungarian  Academy  of  Sciences,  by  P.  Árkai
and  K.  Judik.  They  derive  partly  from  the  eastern  slope,
partly  from  the  western  slope  of  the  Kopaonik  Mt,  from
the  “CKS”  outcrops  along  the  road  Brzeće—Kopaonik  Sky
Center—Jošanička  Banja.  Unfortunately,  the  illite  “crystal-
linity”  indices  (KI  –  Kübler  index)  obtained  are  too  ran-

173

METAMORPHOSED AND DUCTILELY DEFORMED CONODONTS (SERBIA—NE HUNGARY)

Fig. 15.  Possible  types  of  ductile  deformation  of  conodonts  in  dif-
ferent  parts  of  a  fold  during  the  development  of  axial-plane  schis-
tosity  (S

): flattened and elongated (left limb), crook-like (right

limb) or accordion-like (hinge zone).

Fig. 16. Structural cartoon of the Kopaonik Mt (Vardar Zone, Serbia) and of the Aggtelek-Rudabánya and Bükk Mts (NE Hungary), illus-
trating  the  setting  of  metamorphosed  Triassic  carbonates  containing  the  conodonts  described  herein  and  in  Kovács  &  Árkai  (1987,  1989).
These  units  are  situated  beneath  obducted  ophiolite  complexes,  that  were  reworked  in  the  Aggtelek-Rudabánya  Mts  during  the  emplace-
ment  of  the  non-metamorphosed  Aggtelek—Bódva  Units  (cf.  Péró  et  al.  2002,  2003).  Note:  the  Tertiary  70—90

counter-clockwise rotation

recorded in the eastern part of the Pelso Megaunit ( = Pelso Composite Terrane) (Márton in Csontos 1999 and Less 2000) implies, that the
emplacement of ophiolitic units was originally from the NE to SW, the same, as in the present Dinarides.

domly scattered for thermometric evaluation, which can
be explained by two reasons (Árkai pers. commun.):

a) the samples were too much weathered;
b) the KI indices were partly resetted due to the Oli-

gocene granodiorite intrusion.

Regarding the regional geological setting of the investi-

gated rocks (see Fig. 3), the second case could even be
more responsible for the random KI indices.

For correlation of conodont alterations with metamor-

phic petrologic data (illite “crystallinity”, vitrinite and b

reflectances,  mineral  parageneses)  from  NE  Hungary  the
reader  is  referred  to  the  papers  by  Árkai  &  Kovács  (1986),
and  Kovács  &  Árkai  (1987,  1989).

Conclusions

1 – Contemporaneously with the dynamic recrystalli-

zation  and  development  of  foliation/schistosity  of  the
limestone  host  rocks,  the  recrystallization  and  ductile  de-
formation  of  conodonts  also  took  place  (cf.  Fig. 15).

2 – In a dynamic system, in which besides increasing

temperature,  fluid  pressure  and  oriented/tectonic  pres-
sure  (stress)  also  played  a  significant  role,  the  colour  al-
teration  of  conodonts  took  place  differently  from  what
could  be  deduced  from  laboratory  experiments  (hydrous
pyrolysis  at  50 MPa  pressure,  Rejebian  et  al.  1987).  Due
to  increasing  fluid  and  tectonic  pressure,  the  lightening

174

SUDAR and KOVÁCS

(CAI = 6—7 in our case) of the previously blackened
(CAI = 5) conodonts could be accelerated. Tectonic shear-
ing could also accelerate this process. Consequently, dif-
ferent colours (black, grey and white) could develop even
within the same specimen (cf. also Kovács & Árkai 1987).
This makes temperature estimates solely based on the co-
lour of conodonts, even if always the same part of the ele-
ments is considered, highly problematic.

3 – The metamorphism and ductile deformation of the

conodonts presented here evidently took place contempo-
raneously with those of the limestone host rocks. The gen-
eral structural setting (being situated below overthrust
ophiolitic nappes; see Fig. 16) suggests that this tec-
tonometamorphic event could be related to subduction
and obduction processes (160 to 120 Ma in the Bükk Mts;
Árkai et al. 1995). However, subsequent nappe movements
could also play a role in the metamorphism and ductile
deformation of the limestones and of the conodonts con-
tained in them.

4 – Compared with other methods (illite “crystallini-

ty”, mineral paragenesis), at CAI values 5 the lowest
temperature values given by Rejebian et al. (1987) on the
basis of experimental testing seem to be the most realistic
approximation to the ones obtained by those methods for
conditions of regional dynamothermal metamorphism.

5 – Compared with thermobarometric data of very low

to low grade metamorphosed units of NE Hungary con-
taining recrystallized and deformed conodonts with CAI
values 5—6—7 (Torna Unit s.s., Szendrő Unit, Bükk PA
Unit), at least a Szendrő-type metamorphism (which was of
~400

C temperature and of ~ 300 MPa pressure; cf. Árkai

1983) can be assumed for the metamorphosed Upper Trias-
sic limestones of the Smrekovnica (“MTS”). If the apatite
grain size illustrated here (Fig. 10.1—6; Fig. 12.1,2) is also
compared with those illustrated by Kovács & Árkai (1987)
from epizonal metamorphosed units from NE Hungary (Es-
ztramos, Torna Unit s.s.: Pl. 13.3, Figs. 5, 6, and Szendrő
Unit: Pl. 13.4, Figs. 3, 4 therein), a Szendrő-type metamor-
phism can also be assumed for the “MTS”, e.g the lower
part of the greenschist facies, at minimal pressure of the
boundary of low and medium pressure domains. The same
can also be postulated by comparing the texture and cal-
cite grain size of the recrystallized limestones/marbles;
cf. Fig. 13.1,2 and 14.3,4 herein. We should add to this
point, that P. Horváth, also at the Institute of Geochemi-
cal Research of HAS, Budapest, investigated two metaba-
site samples from the Županj (“CKS”), collected by the
second author, which yielded considerably higher data:
530—550

C and 500 MPa, as well as 620—630

C and

500 MPa, respectively (P. Horváth, pers. commun. and un-
publ. manuscript).

6 – It is worth noting, that in the high temperature anchi-

metamorphosed Uppony Unit (at ~ 350

C and ~ 250 MPa;

Árkai et al. 1981; Árkai 1983) conodonts are black
(CAI = 5), but less recrystallized (Kovács & Árkai op. cit.,
Pl. 13.4, Figs. 1, 2) and not deformed. It implies, that at
temperature ~ 4 0 0

C and ~ 300 MPa (e.g. at the Szendrő-

type metamorphism) there should be a remarkable increase
in metamorphism and deformation of conodonts, that is

about at the boundary of the anchizone and epizone, and
at the boundary of low and medium pressure domains, re-
spectively. It also underlines, that the metamorphism of
“MTS” was at least of Szendrő-type.

7 – As the colour of conodonts under the conditions of

regional dynamothermal metamorphism is also influenced
by the factors mentioned above, the apatite grain size could
probably be a more trustworthy indicator of the temperature
of metamorphism. However, detailed studies are needed on
the statistic evaluation of the average grain size and its cor-
relation with other metamorphic petrologic methods (illite
“crystallinity”, chlorite “crystallinity”, etc.).

Acknowledgments:

In Serbia, the research has been

supported by the Ministry of Science and Environmental
Protection of the Republic of Serbia, Projects
No. 101767 and No. 146009 (MS). Financial support in
Hungary was provided by the National Research Fund
(OTKA), Grants No. T 029654 and T 037595 (SK). Ste-
van Karamata’s and Milorad Dimitrijevic’s (Belgrade)
contributions on the geology of the Kopaonik Mt is
gratefully acknowledged. Our thanks are also due to
Péter Árkai, Péter Horváth and Katalin Judik (Institute of
Geochemical Research, Hungarian Academy of Sciences,
Budapest) for carrying out metamorphic petrologic (es-
pecially illite “crystallinity”) investigations on samples
from the Kopaonik Mt, as well as to László Csontos,
Balázs Koroknai (Budapest) and Stefan Schmid (Basel)
for their help with literature and advice on ductile defor-
mation and limestone recrystallization. We thank also to
the reviewers: Péter Árkai (Budapest), Fritz Ebner (Le-
oben) and Ján Mello (Bratislava) for their suggestions
and critical notes.

References

Árkai P. 1973: Pumpellyite-prehnite-quartz facies Alpine metamor-

phism in the Middle Triassic volcanogenic-sedimentary se-
quence of the Bükk Mountains, Northeast Hungary. Acta
Geol. Acad. Sci. Hung. 17, 67—83.

Árkai P. 1977: Low-grade metamorphism of Paleozoic formations

of the Szendrő Mountains (NE Hungary). Acta Geol. Acad.
Sci. Hung. 21, 53—80.

Árkai P. 1983: Very low- and low-grade Alpine regional metamor-

phism of the Paleozoic and Mesozoic formations of the Bükki-
um, NE-Hungary. Acta Geol. Hung. 26, 1—2, 83—101.

Árkai P. & Kovács S. 1986: Diagenesis and regional metamorphism

of the Mesozoic of Aggtelek-Rudabánya mountains (Northeast
Hungary). Acta Geol. Hung. 29, 3—4, 349—373.

Árkai P., Horváth Z.A. & Tóth M. 1981: Transitional very low-

and low-grade regional metamorphism of the Paleozoic for-
mations, Uppony Mountains, NE Hungary: mineral assem-
blages, illite crystallinity, -b

and vitrinite reflectance data.

Acta Geol. Acad. Sci. Hung. 24, 265—294.

Árkai P., Balogh Kad. & Dunkl I. 1995: Timing of low-tempera-

ture metamorphism and cooling of the Paleozoic and Mesozo-
ic formations of the Bükkium, innermost Western Carpathians,
Hungary. Geol. Rdsch. 84, 334—344.

Belka Z. 1990: Thermal maturation and burial history from Con-

175

METAMORPHOSED AND DUCTILELY DEFORMED CONODONTS (SERBIA—NE HUNGARY)

odont  Colour  Alteration  data,  Holy  Cross  Mountains,  Poland.
In:  Ziegler  W.  (Ed.):  Papers  on  conodonts  and  Ordovician  to
Triassic  conodont  stratigraphy.  Cour.  Forschungsinst.  Senck-
enberg  118,  241—251.

Budurov K.J. & Sudar M.N. 1990: Late Triassic Conodont Stratig-

raphy.  In:  W.  Ziegler  (Ed.):  Papers  on  conodonts  and  Ordovi-
cian  to  Triassic  conodont  stratigraphy.  Cour.  Forschungsinst.
Senckenberg  118,  203—239.

Buggisch W. 1986: Diagenese and Anchimetamorphose aufgrund

von Conodontenfarbe (CAI) und “Illit-Kristallinität” (IC).
Geol. Jb. Hessen 114, 181—200.

Burkhard M. 1990: Ductile deformation mechanisms in micritic

limestones naturally deformed at low temperatures (150—350

In: Knipe R.J. & Rutter E.H. (Eds.): Deformation, rheology and
tectonics. Geol. Soc. Spec. Publ. 54, 241—257.

Csontos L. 1988: Etude géologique d’unes portion des Carpathes

internes: le massif du Bükk (NE de la Hongrie) (Stratigraphie,
structures, metamorphism et géodynamique). Thése doctorat,
Univ. Sci. Techn., Lille Flandres-Artois 250, 1—327.

Csontos L. 1999: Structural outline of the Bükk Mts., N. Hungary.

Földt. Közl. 129, 4, 611—651 (in Hungarian, English abstract).

Csontos L. & Nagymarosy A. 1998: The Mid-Hungarian line: a zone

of repeated tectonic inversions. Tectonophysics 297, 51—71.

Čanović M. & Kemenci R. 1999: Geologic setting of the Pre-Tertia-

ry basement in Vojvodina (Yugoslavia) Part II: The north part
of the Vardar zone in the south of Vojvodina. Acta Geol.
Hung. 42, 4, 427—449.

Dimitrijević M.D. 1995: The Kopaonik block – its position in the

Vardar Zone. In: Symposium “Geology and Metallogeny of
Kopaonik Mt.”, June 19—22, 1995. Kopaonik—Beograd, 33—40
(in Serbian, English abstract).

Dimitrijević M.D. 1997: Geology of Yugoslavia. Geol. Inst. Gemi-

ni, Spec. Publ., Barex, Belgrade, 1—187.

Dimitrijević M.D. 2000: The Dinarides and the Vardar Zone – the

Eternal  Conundrum.  In:  Karamata  S.  &  Janković  S.  (Eds.):
Proc.  Int.  Symp.  “Geology  and  Metallogeny  of  the  Dinarides
and  the  Vardar  Zone”.  Acad.  Sci.  Arts  Repub.  Srpska,  Collect.
Monogr., I, Dep. Nat., Math. Tech. Sci. I, 5—13.

Dimitrijević M.D. 2001: Dinarides and the Vardar Zone: a short re-

view of the geology. In: Downes H. & Vaselli O. (Eds.): Tertia-
ry magmatism in the Dinarides. Acta Vulcanol. 13, 1—2, 1—8.

Dimitrijević M.N. & Dimitrijević M.D. 1991: Triassic carbonate

platform of the Drina-Ivanjica element (Dinarides). Acta Geol.
Hung. 34, 1—2, 15—44.

Dimitrijević M.N., Dimitrijević M.D., Karamata S., Sudar M., Gerzi-

na N., Kovács S., †Dosztály L., Gulácsi Z., Less Gy. & Pelikán
P. 2003: Olistostrome/mélanges – an overview of the problems
and preliminary comparison of such formations in Yugoslavia
and NE Hungary. Slovak Geol. Mag. 9, 1, 3—21.

Đur anović Ž. 1971: Ein beitrag zur lithologie und stratigraphie

der  kristallinen  gesteine  der  Fruška  Gora  (Sirmien-Jugoslaw-
ien). Bull. Sci., Cons. Acad. Sci. Arts RSF Yougsl., Sect. A  16,
5—6,  137—138.

Đur anović Ž. 1973: About the Paleozoic and the Triassic of

Medvednica  mountain  and  the  area  near  Dvor  na  Uni  on  the
basis  of  conodonts.  Geol.  Vjes.  25,  1971,  29—49  (in  Croatian,
English  summary).

Ebner F., Kovács S. & Schönlaub H.P. 1998: Stratigraphic and fa-

cial  correlation  correlation  of  the  Szendrő-Uppony  (NE  Hun-
gary)  with  the  Carnic  Alps-South  Karawanken  Mts.  and  Graz
Paleozoic (Southern Alps and Central Eastern Alps): some pa-
leogeographic  implications.  Acta  Geol.  Hung.  41,  4,  355—388.

Epstein A.G., Epstein J.B. & Harris L.D. 1977: Conodont color al-

teration – An index to organic metamorphism. U.S. Geol.
Surv. Prof. Pap. 995, 1—27.

Filipović I., Jovanović D., Sudar M., Pelikán P., Kovács S., Less

Gy. & Hips K. 2003: Comparison of the Variscan—Early Al-
pine evolution of the Jadar Block (NW Serbia) and “Bükkium”
(NE Hungary) terranes; some paleogeographic implications.
Slovak Geol. Mag. 9, 1, 23—40.

Flügel H.W. 1990: Das voralpine Basement im Alpin-Mediterranen

Belt – Überblick und Problematik. Jb. Geol. Bundesanst.
Wien 133, 2, 181—221.

Fodor L. & Koroknai B. 2000: Ductile deformation and revised

lithostratigraphy of the Martonyi Subunit (Torna Unit, Rud-
abánya Mts, NE Hungary). Geol. Carpathica 51, 6, 355—369.

Forián-Szabó M. & Csontos L. 2002: Tectonic structure of the Kis-

Fennsík area (Bükk Mountains, NE Hungary). Geol. Carpathi-
ca 53, 4, 223—234.

Garcia-Lopez S., Brime C., Bastida F. & Sarmiento G.N. 1997: Simul-

taneous use of thermal indicators to analyse the transition from
diagenessis to metamorphism: an example from the Variscan Belt
of northwest Spain. Geol. Mag. 134, 3, 323—334.

Gawlick H.-J. & Hopfer N. 1999: Stratigraphie, Fazies und Hoch-

druck-Mitteltemperatur-Metamorphose  der  Hallstätter  Kalke
der  Pailwand  (Nördliche  Kalkalpen,  Österreich).  Z.  Dtsch.
Geol.  Gesell.  150,  4,  641—671.

Gawlick H.-J., Krystyn L. & Lein R. 1994: CAI-paleotemperatures

and metamorphism in the Northern Calcareous Alps – a gen-
eral review. Geol. Rdsch. 83, 644—657.

Grill J., Kovács S., Less Gy., Réti Zs., Róth L. & Szentpétery I.

1984: Geology and evolution of the Aggtelek-Rudabánya Mts.
Földt. Kutatás 27, 4, 49—56.

Grubić A. 1995: Schistes lustres in the Kopaonik area. In: Sym-

posium  “Geology  and  Metallogeny  of  Kopaonik  Mt.”,  June
19—22,  1995.  Kopaonik—Beograd,  159—168  (in  Serbian,
English  abstract).

Grubić A. & Protić Lj. 2000: Deep-water Triassic sediments of the

Vardar Zone and Fruška Gora Mt. In: Karamata S. & Janković
S. (Eds.): Proc. Int. Symp. “Geology and Metallogeny of the
Dinarides and the Vardar Zone”. Acad. Sci. Arts Repub. Srpska,
Collect. Monogr., I, Dep. Nat., Math. Tech. Sci. I, 87—92.

Grubić A., Đoković I. & Marović M. 1995: Tectonic outline of the

Kopaonik area. In: Symposium “Geology and Metallogeny
of Kopaonik Mt.”, June 19-22, 1995. Kopaonik—Beograd,
46—53 (in Serbian, English abstract).

Haas J. 2001: Geology of Hungary. Eötvös Univ. Press, Budapest,

1—317.

Haas J. & Kovács S. 2001: The Dinaridic-Alpine connection – as

seen from Hungary. Acta Geol. Hung. 44, 2—3, 345—362.

Judik K., Árkai P., Horváth P., Dobosi G., Tibljaš D., Balen D.,

Tomljenović B. & Pamić J. 2004: Diagenesis and low-temper-
ature  metamorphism  of  the  Mt.  Medvednica,  Croatia:  Mineral
assemblages  and  phyllosilicate  characteristics.  Acta  Geol.
Hung.  47,  2—3,  151—176.

Karamata S. 1995: The Kopaonik block, its position and genesis.

In: Symposium “Geology and Metallogeny of Kopaonik
Mt.”, June 19—22, 1995. Kopaonik—Beograd, 41—45 (in Ser-
bian, English abstract).

Karamata S., Kemenci R., Filipović I., Sudar M., Milovanović D. &

Gerzina N. 2002: Geology of the NW part of the Vardar Zone.
Manuscript, Excursion Quide, Fac. Min. Geol., Univ. Bel-
grade, 1—63.

Karamata S., Olujić J., Protić Lj., Milovanović D., Vujnović L.,

Popević  A.,  Memović  E.,  Radovanović  Z.  &  Resimić-Šarić  K.
2000: The Western Belt of the Vardar Zone – the remnant of
a  marginal  sea.  In:  Karamata  S.  &  Janković  S.  (Eds.):  Proc.
Int.  Symp.  “Geology  and  Metallogeny  of  the  Dinarides  and
the  Vardar  Zone”.  Acad.  Sci.  Arts  Repub.  Srpska,  Collect.
Monogr., I, Dep. Nat., Math. Tech. Sci. I, 131—135.

Klisić M., Mićić I., Pajić V., Simić D. & Kandić M. 1972: Contribu-

tion to the stratigraphy of the Trepča metamorphic series.

176

SUDAR and KOVÁCS

Zapisnici Srp. geol. druš. za 1968, 1969 i 1970 (Zbor 10. XII
1968), 105—107 (in Serbian, Cyrillic).

Königshof P. 1992: Der Farbänderungsindex von Conodonten (CAI)

in  paläozoischen  Gesteinen  (Mitteldevon  bis  Underkarbon)  des
Rheinischen  Schiefergebirges  Eine  Ergänzung  zur  Vitrinitre-
flexion.  Cour.  Forschungsinst.  Senckenberg  146,  1—118.

Kolar-Jurkovšek T. 1994: Carnian microfossils from Bevško.

Geologija 36, 1993, 61—67 (in Slovenian, English summary).

Kolar-Jurkovšek T. & Jurkovšek B. 1995: Lower Triassic conodont

fauna from Tržič (Karavanke Mts., Slovenia). Eclogae Geol.
Helv. 88, 3, 789—801.

Kolar-Jurkovšek T. & Jurkovšek B. 1996: Contribution to the

knowledge of the Lower Triassic conodont fauna in Slovenia.
Razprave IV. razreda SAZU XXXVII/1, 3—21.

Kovács S. 1986: Conodont-biostratigraphical and microfacies in-

vestigations  in  the  Hungarian  part  of  the  Northeastern  Rud-
abánya  Mts.  Magy.  Áll.  Földt.  Intéz.  Évi  Jelent.  1984-ről.,
193—244  (in  Hungarian,  English  summary).

Kovács S. 1992: Stratigraphy of the Szendrő-Uppony Paleozoic

(Northeastern  Hungary).  In:  Vozár  J.  (Ed.):  Western  Car-
pathians,  Eastern  Alps,  Dinarides.  Spec.  Vol.  to  Paleozoic
Geodynamic  Domains,  IGCP  Project  No.  276,  Dionýz  Štúr
Geol. Inst., Bratislava, 93—108.

Kovács S. & Árkai P. 1987: Conodont alteration in metamorphosed

limestones  from  northern  Hungary,  and  its  relationship  to  car-
bonate  texture,  illite  crystallinity  and  vitrinite  reflectance.  In:
Austin R.L. (Ed.): Conodonts: investigative techniques and ap-
plications.  British  Micropaleontol.  Soc.  Series,  Ellis  Horwood
Lim.,  Chichester,  207—229.

Kovács S. & Árkai P. 1989: Significance of conodont and limestone-

texture  alterations  in  recognition  of  the  boundary  between  di-
agenesis  and  regional  dinamothermal  metamorphism,  based  on
examples  from  the  Aggtelek-Rudabánya  Mts  (NE  Hungary).
Magy. Áll. Földt. Intéz. Évi Jelent. 1987-ről., 216—235 (in Hun-
garian,  English  summary).

Kovács S. & Péró Cs. 1983: Report on stratigraphical investigation

in the Bükkium, Northern Hungary. IGCP Project 5, Newslet-
ter 5, 58—65.

Kovács S., Less Gy., Piros O., Réti Zs. & Róth L. 1989: Triassic

formations of the Aggtelek-Rudabánya Mountains (Northeast-
ern Hungary). Acta Geol. Hung. 32, 1—2, 31—63.

Kovács S., Szederkényi T., Haas J., Buda Gy., Császár G. & Nagy-

marosy  A.  2000:  Tectonostratigraphic  terranes  in  the  pre-Neo-
gene  basement  of  the  Hungarian  part  of  the  Pannonian  area.
Acta  Geol.  Hung.  43,  3,  225—328.

Kozur H. & Mock R. 1977: Conodonts and holothurian sclerites

from the Upper Permian and Triassic of the Bükk Mountains
(North Hungary). Acta Mineral. Petrogr. Szeged 23, 109—126.

Krystyn L., Gawlick H.-J. & Lein R. 1998: Triassic CAI-distribu-

tion patterns and their implications for the tectonic history of
North Slovenia. XVI Congr. CBGA, (30 August—2 September
1998, Vienna), Abstracts, Geol. Surv. Austria, Vienna, 1—320.

Less Gy. 2000: Polyphase evolution of the structure of the Ag-

gtelek-Rudabánya  Mountains  (NE  Hungary),  the  southernmost
element  of  the  Inner  Western  Carpathians  –  a  review.  Slovak
Geol.  Mag.  6,  2—3,  260—268.

Less Gy., Gulácsi Z., Kovács S., Pelikán P., Pentelényi L., Rezessy

A. & Sásdi L. 2002: Geological map of the Bükk Mountains.
1 : 50,000. Hung. Geol. Inst., Budapest.

Mićić I., Urošević D., Kandić M., Klisić M. & Simić D. 1972: Find-

ings  of  Triassic  conodont  fauna  in  the  metamorphic  complex
of  Kopaonik  Mt.  Zapisnici  Srp.  geol.  druš.  za  1968,  1969  i
1970  (Zbor  10.  XII  1968),  103—104  (in  Serbian,  Cyrillic).

Neubauer F. & Friedl G. 1997: Conodont preservation within the

Gurktal nappe complex, Eastern Alps. Zbl. Geol. Paläont. Teil I
(1996) 3, 4, 277—289.

Neubauer F. & von Raumer J.F. 1993: The Alpine Basement – Link-

age  between  Variscides  and  East-Mediterranen  Belts.  In:
von  Raumer  J.F.  &  Neubauer  F.  (Eds.):  Pre-Mesozoic  geol-
ogy  in  the  Alps.  Springer-Verlag,  Berlin,  641—663.

Németh N. & Mádai F. 2003: Early phase ductile deformation ele-

ments in limestones of the Eastern part of the Bükk Moun-
tains I. Földt. Közl. 133, 4, 563—583 (in Hungarian, English
abstract).

Nöth S. 1991: Die Conodontendiagenese als Inkohlungsparameter

und ein Vergleich unterschiedlich sensitiver Diageneseindika-
toren am Beispiel von Triassedimenten Nord-und Mitteldeut-
schlands. Bochumer Geol. u. Geotech. Arb. 37, 1—169.

Palinkaš A.L., Kolar-Jurkovšek T., Borojević S. & Bermanec V.

2000:  Triassic  rifting  magmatism  within  Zagorje-Mid-Trans-
danubian zone, examplified by pillow lavas of Hruškovec, Mt.
Kalnik,  N  Croatia.  In:  Tomljenović  B.,  Balen  D.  &  Saftić  B.
(Eds.):  Pancardi  2000  (Dubrovnik,  Croatia,  1—3.  10.  2000),
Abstracts. Vijesti Hrvat. Geol. Druš. 37, 3, 98—99.

Pamić J. & Tomljenović B. 1998: Basic geologic data from the

Croatian part of the Zagorje-Mid-Transdanubian Zone. Acta
Geol. Hung. 41, 4, 389—400.

Péró Cs., Kovács S., Less Gy. & Fodor L. 2002: Tectonic setting of

the Triassic “Hallstatt” (s.l.) facies in NE Hungary. In: Pro-
ceedings of the XVIIth Congress of the Carpatho-Balkan Geo-
logical Association, Bratislava, Sept. 1—4, 2002, Geol.
Carpathica 53, Spec. Issue, 24—25.

Péró Cs., Kovács S., Less Gy. & Fodor L. 2003: Geological setting

of Triassic “Hallstatt” (s.l.) facies in NE Hungary. In: VI

Alp-

shop Workshop, Sopron, 14—16 Sept., 2003. Ann. Univ. Sci.
Budapest., Sect. Geol. 35, 58—60.

Rejebian V.A., Harris A.G. & Huebner J.S. 1987: Conodont color

and  textural  alteration:  An  index  to  regional  metamorphism,
contact  metamorphism,  and  hydrothermal  alteration.  Bull.
Geol.  Soc.  Amer.  99,  471—479.

Resimić-Šarić K., Karamata S., Popević A. & Balogh K. 2000: The

eastern branch of the Vardar Zone – the scar of the main Var-
dar  Ocean.  In:  Karamata  S.  &  Janković  S.  (Eds.):  Proc.  Int.
Symp.  “Geology  and  Metallogeny  of  the  Dinarides  and  the
Vardar  Zone”.  Acad.  Sci.  Arts  Repub.  Srpska,  Collect.
Monogr., I, Dep. Nat., Math. Tech. Sci. I, 81—85.

Réti Zs. 1985: Triassic ophiolite fragments in an evaporitic mé-

lange, Northern Hungary. Ofioliti 10, 2—3, 411—422.

Sadek Gh., Árkai P. & Nagy G. 1996: Alpine polyphase metamor-

phism of the Szarvaskő complex, Bükk Mountains, Hungary.
Acta Mineral. Petrogr. Szeged 37, 99—128.

Sudar M. 1986: Triassic microfossils and biostratigraphy of the Inner

Dinarides between Gučevo and Ljubišnja Mts., Yugoslavia. Geol.
An. Balk. Poluos. 50, 151—394 (in Serbian, English summary).

Sudar M. & Kovács S. 1998: Alteration of conodonts in metamor-

phosed  Triassic  limestones:  a  case  study  from  the  Kopaonik
Mt.  (Vardar  Zone,  Serbia)  and  from  the  Bükk + Rudabánya
Mts.  (Pelsonia  Composite  Terrane,  NE  Hungary).  In:  G.  Bag-
noli  (Ed.):  ECOS  VII  Abstracts,  Bologna-Modena,  1998.  Ti-
pografia  Compositori,  Bologna,  108—110.

Velledits F. 2000: Evolution of the area from the Berva Valley to

the Hor Valley in the Middle—Upper Triassic. Földt. Közl. 130,
1, 47—93 (in Hungarian, English abstract).

Velledits F. & Péró Cs. 1987: The Southern Bükk (northern Hunga-

ry) Triassic revisited: The Bervavölgy Limestone. Ann. Univ.
Sci. Budapest., Sec. Geol. 27, 17—64.