GeolCarp_Vol66_No1_37

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, FEBRUARY 2015, 66, 1, 37—50 doi: 10.1515/geoca-2015-0009

The thermal history of the Miocene Ibar Basin (Southern

Serbia): new constraints from apatite and zircon fission

track and vitrinite reflectance data

NEVENA ANDRIĆ

, BERNHARD FÜGENSCHUH

, DRAGANA ŽIVOTIĆ

and

VLADICA CVETKOVIĆ

University of Belgrade, Faculty of Mining and Geology, Đušina 7, 11000 Belgrade, Serbia;

nevena.andric@rgf.bg.ac.rs; dragana.zivotic@rgf.bg.ac.rs; cvladica@rgf.bg.ac.rs

University of Innsbruck, Faculty of Geo- and Atmospheric Sciences, Institute of Geology, Innrain 52f, 6020 Innsbruck, Austria;

bernhard.fuegenschuh@uibk.ac.at

(Manuscript received January 16, 2014; accepted in revised form December 10, 2014)

Abstract: The Ibar Basin was formed during Miocene large scale extension in the NE Dinaride segment of the Alpine-
Carpathian-Dinaride system. The Miocene extension led to exhumation of deep seated core-complexes (e.g. Studenica
and Kopaonik core-complex) as well as to the formation of extensional basins in the hanging wall (Ibar Basin). Sedi-
ments  of  the  Ibar  Basin  were  studied  by  apatite  and  zircon  fission  track  and  vitrinite  reflectance  in  order  to  define
thermal events during basin evolution. Vitrinite reflectance (VR) data (0.63—0.90 %Rr) indicate a bituminous stage for
the  organic  matter  that  experienced  maximal  temperatures  of  around  120—130 °C.  Zircon  fission  track  (ZFT)  ages
indicate provenance ages. The apatite fission track (AFT) single grain ages (45—6.7 Ma) and bimodal track lengths
distribution indicate partial annealing of the detrital apatites. Both vitrinite reflectance and apatite fission track data of
the studied sediments imply post-depositional thermal overprint in the Ibar Basin. Thermal history models of the detritial
apatites reveal a heating episode prior to cooling that began at around 10 Ma. The heating episode started around 17 Ma
and lasted 10—8 Ma reaching the maximum temperatures between 100—130 °C. We correlate this event with the domal
uplift of the Studenica and Kopaonik cores where heat was transferred from the rising warm footwall to the adjacent
colder hanging wall. The cooling episode is related to basin inversion and erosion. The apatite fission track data indicate
local thermal perturbations, detected in the SE part of the Ibar basin (Piskanja deposit) with the time frame  ~ 7.1 Ma,
which may correspond to the youngest volcanic phase in the region.

Key words: Balkan Peninsula, Ibar Basin, low-temperature thermochronology, core-complex, basin inversion, organic matter.

Introduction

The process of lithospheric extension is characterized by ex-
humation of middle to lower continental crust along crustal-
scale detachments (Lister & Davis 1989). The exhumation of
the high-grade metamorphic rocks in the footwall of the de-
tachment is followed by subsidence and development of sed-
imentary (supra-detachment) basins on the hanging wall
(Friedmann & Burbank 1995).

In general, the thermal evolution of supra-detachment ba-

sins  is  influenced  by  the  interplay  of  several  factors  related
to  detachment  activity:  i)  temperature  contrast  between  the
rapidly exhuming warm footwall and the cold hanging wall;
ii) burial history of the basin; iii) magmatism ± hydrothermal
activity and iv) basin inversion and exhumation (Dunkl et al.
1998; Kounov et al. 2004; Márton et al. 2010). The thermal
state of the supradetachment basins is potentially affected by
rapid  exhumation  of  the  warm  footwall  along  the  detach-
ment. The heat advection leads to an elevated thermal gradi-
ent  in  the  footwall  and,  subsequently,  this  heating  was
transferred by conduction to the hanging wall (Grasemann &
Mancktelow 1993).

The Miocene Ibar Basin is located 200 km south of Bel-

grade, covering an area of approximately 320 km

(Fig. 1). It

is a northwest-southeast elongated tectonic depression with a
maximum length of 20 km and width of 12 km.

The Ibar Basin is supra-detachment basin, which provides

the opportunity to study the thermal influence of the exhum-
ing core on the basin fill in the hanging wall of the active de-
tachment.  The  Ibar  Basin  belongs  to  the  group  of  Lower
Miocene intramontane basins called the Dinaridic lake system
(Krstić et al. 2003; Harzhauser & Mandić 2008). The forma-
tion  of  these  basins  was  contemporaneous  with  the  exten-
sional  collapse  of  the  Alpine  orogenic  wedge  and  back-arc
Pannonian extension in the Miocene (Tari et al. 1992; Ilić &
Neubauer 2005; Horváth et al. 2006; Leew et al. 2012), which
was  accompanied  by  exhumation  of  the  metamorphic  core-
complexes (Tari et al. 1999; Ustaszewski et al. 2010; Matenco
&  Radivojević  2012;  Stojadinović  et  al.  2013).  The  subsid-
ence of the hanging wall of these detachments was accompa-
nied by the formation of basins on the top.

Previous studies of the Ibar Basin were related mostly to

stratigraphy, and exploration of mineral resources (coal, bo-
ron minerals, and magnesite). However, none of the earlier
studies focused on elucidating the basin’s evolution in more
detail, especially in terms of its high heat flow regime. This
study aims at providing new information about the thermal
history of the Ibar Basin. Additionally, our data shed light on

THERMAL HISTORY, FISSION TRACK AND VITRINITE REFLECTANCE (MIOCENE IBAR BASIN, SERBIA)

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the time and magnitude of paleo-thermal episodes in the Ibar
Basin, including the phases of basin inversion and regional
uplift (i.e. exhumation).

Geological setting

The Ibar Basin belongs to the eastern/south-eastern parts of

the inner Dinarides (Fig. 1). It is situated on top of a Late Cre-
taceous to Eocene Adria-derived nappe stack which formed in
the course of the Adria-Europe collision (Schmid et al. 2008).
The  collision  was  preceded  by  ophiolite  obduction  onto  the
distal Adriatic continental margin during the Late Jurassic as
well  as  by  subsequent  closure  of  the  last  Neotethys  oceanic
realm  forming  the  Sava  suture  zone  (Pamić  et  al.  2002;
Schmid  et  al.  2008;  Ustaszewski  et  al.  2009).  Later  on,  the
ophiolites were involved in out-of-sequence thrusting forming
composite  nappes  along  with  the  Adria  derived  continental
units in the lower position. The composite nappes namely the

Drina-Ivanjica and Jadar-Kopaonik units consist of non-
metamorphosed to slightly metamorphosed Upper Paleozoic—
Lower Jurassic sediments of the distal Adria margin overlain
by Late Jurassic ophiolites (Fig. 1 – Dimitrijević 1997;
Karamata 2006; Schmid et al. 2008; Schefer et al. 2010).

In the Ibar area these composite nappes are represented by

the  Kopaonik  Metamorphic  Series  or  Jadar-Kopaonik  com-
posite nappe (Fig. 1). During the Late Oligocene post-orogenic
phase  these  series  were  intruded  by  the  I-type  granitoids  of
Drenje (31.7—31.2 Ma – Schefer et al. 2011) and Kopaonik
(30.9—30.7 Ma – Schefer et al. 2011). The dacite- andesite
extrusions and volcanoclastic rocks (31 Ma – Cvetković et
al.  1995)  intruded  and/or  overlaid  ophiolites  (Cvetković  et
al. 1995; Schefer et al. 2011). In the Miocene the study area
underwent  N-S  extension  (Schefer  2010),  which  led  to  the
exhumation of the Studenica and Kopaonik domes starting at
around  21—17 Ma  as  indicated  by

Ar/

Ar ages on biotite

(Schefer 2010) and ending around 10 Ma (AFT and ZFT
data – Schefer et al. 2011). The tectonic omission was

Sample

Local coordinates

(MGI Balkans 7)

(m)

Latitude–
longitude
(decimal
degrees)

Altitude

(m)

Depth (m)

Lithology

Location

Method of
investigation

IBM-1/1

7472377.63
4804201.05

N 43.38174
E 20.65376

409.50 43.5–44.5 Shale

Piskanja deposit

IBM-1/2

406.10 47.0–47.9 Shale

IBM-1/3

387.20 63.2–66.8 Shale

IBM-1/4

330.10 122.8–123.9 Shale

IBM-1/6

325.80 127.0–128.2 Shale

IBM-1/7

257.40 195.4–196.6 Shale

IBM-1/8

226.40 226.3–227.6 Shale

IBM-1/23

147.40

302.5–306.6

Sandstone

AFT, ZFT

IBM-1/24

134.30

318.3–319.7

Sandstone

AFT, ZFT

IBM-1/25

110.30 342.1–343.7 Conglomerate

AFT,

ZFT

IBM-1/27

109.50 344.2–344.5 Shale

IBM-1/28

101.80

344.5–352.2

Sandstone

AFT, ZFT

IBM-1/29

100.80 352.2–353.2 Shale

IBM-1/30

79.70

373.5–374.3

Sandstone

AFT, ZFT

IBM-1/31

72.00 381.9–382.0 Coal

fragments

shale

IBM-1/22

46.80

409.3–409.5

Conglomerate

AFT, ZFT

IBM-2/15

7472179.85
4804237.84

N 43.38207

E 20.65132

114.53

318.5–320.1

Sandstone

AFT, ZFT

IBM-2/17

74.98

359.05–359.95

Sandstone

AFT, ZFT

IBM-2/19

53.73

379.4–381.2

Sandstone

AFT, ZFT

IBM-2/21

39.73 394.7–395.2 Shale

IBM-4/41

7471435.92
4803862.07

N 43.37865
E 20.64216

250.46

149.4–152.3

Sandstone

AFT, ZFT

IBM-4/44

90.06

309.1–312.7

Sandstone

AFT, ZFT

Tadenje 11

7469179
4809748

N 43.43155
E 20.61397

457.40 47.6–48.6 Coal

Tadenje
underground
coal mine

Tadenje 12

457.20

48.6–48.8

Sandstone

AFT, ZFT

Tadenje 14

455.70 49.6–50.3 Coal

Tadenje 15

437.60

68.2–68.4

Sandstone

AFT, ZFT

Tadenje 1

437.40 68.4–68.6 Coal

Tadenje 13

436.40

69.5–69.6

Sandstone

AFT, ZFT

Tadenje 10A

435.30 70.5–70.7 Coal

Tadenje 10B

435.00 70.7–71.0 Coal

1-Biljanovac

7472085
4807161

N 43.40837
E 20.65000

383.00

Surface

Volcanoclastite

Biljanovac

AFT, ZFT

8-Pruga

7471207
4802855

N 43.36958
E 20.63938

399.00 Surface

Andesite/
volcanoclastite

Pruga

AFT, ZFT

4-Kremići

7477304
4800615

N 43.34963
E 20.71471

1140.00 Surface

Granodiorite

Kremići

AFT, ZFT

9-Kremići

7474777
4800961

N 43.35266
E 20.68352

808.00 Surface

Hydrothermally altered
andesite

AFT, ZFT

3-Drenje

7483607
4806320

N 43.40115
E 20.79228

740.00

Surface

Granodiorite

Drenje

AFT, ZFT

Table 1: Locality and lithology of the samples. VR – vitrinite reflectance, AFT – apatite fission track, ZFT – zircon fission track.

ANDRIĆ, F

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and CVETKOVIĆ

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about  10 km  (Schefer  2010).  The  core-complex  formation
was  coeval  with  the  emplacement  of  the  S-type  Polumir
granite  (18.1—17.4 Ma),  Golija  granite  (20.6—20.2 Ma)  and
exhumation of the older Oligocene I-granitic rocks of Kopa-
onik and Drenje (Schefer et al. 2011). The Miocene volcanic
activity  is  represented  by  effusives  and  pyroclastites  of
quartz-latitic  composition.  The  Miocene  volcanics  occur
south-west  of  the  Kopaonik  intrusives  and  in  the  surround-
ings of the Golija pluton (Cvetković & Pécskay 1999; Cvet-
ković 2002).

The Ibar Basin was formed in the hanging wall of the

Studenica core-complex, but it also possibly records a brittle
phase (mainly E-W directed, and subordinately N-S) of exhu-
mation of the Kopaonik Metamorphic Series (Schefer 2010).
Deposition  started  with  continental  alluvial,  syn-kinematic
breccio-conglomerates,  sandstones  and  marlstones  interca-
lated with up to nine bituminous coal seams (Anvelković et
al. 1991; Ercegovac et al. 1991). This succession is overlain
by laminated dolomitic marlstones and claystones, deposited
in  a  lacustrine  environment.  The  overall  present  day  thick-
ness  of  the  sediments  deposited  in  the  Ibar  Basin  is  around
1500 m (based on geophysical exploration – Anvelković et
al. 1991). The basin is characterized by the presence of bitu-
minous coals (%Rr up to 0.91 – Ercegovac et al. 1991), bo-
ron  mineralization  (borates  and  howlite  –  Obradović  et  al.
1992), magnesite deposits (Falick et al. 1991) and travertine
(noticed  during  field  observation).  Other  intramontane  coal
basins  in  Serbia,  which  cover  the  same  stratigraphic  range,
did not exceed the subbituminous stage of coalification (%Rr
~

0.45 – Ercegovac et al. 2006; Životić et al. 2008, 2010).

The relatively high rank of Cenozoic coals from the Ibar Ba-
sin according to Ercegovac et al. (1991) is due to the thermal
influence of andesitic extrusion.

The age of sediments is not well constrained. According to

correlation of sediments from other intra-montane basins in
the  Dinaridic  lake  system  it  could  be  inferred  that  alluvial
deposition  started  around  19—17 Ma  (Prysjazhnjuk  et  al.
2000; Krstić et al. 2001) and lasted until 16—15 Ma when a
typical  lacustrine  environment  was  established  (Kochansky
&  Slisković  1981).  Combining  geodynamic  (Schefer  2010)
and  paleontological  lines  of  evidence  (Prysjazhnjuk  et  al.
2000;  Krstić  et  al.  2001)  in  the  following  discussion  we
adopt 19 Ma as the age of the onset of sedimentation in the
Ibar  Basin.  Today  the  Ibar  Basin  can  be  characterized  as  a
composite basin which is formed by four sub-basins (Fig. 1):
Tadenje, Ušće, Jarando, and Gradac (Ercegovac et al. 1991).
The sediments studied here from the Piskanja deposits repre-
sent the south-eastern part of the Jarando sub-basin.

Sampling strategy and analytical methods

The thermal history of the Ibar Basin has been studied by

means of vitrinite reflectance and detritial apatite and zircon
fission track data targeting the maximum paleotemperatures
and duration of the thermal event, cooling manner (slow/
fast) from maximal paleotemperatures, respectively.

The majority of samples were collected from boreholes in

the Piskanja deposit and Tadenje underground coal mine.

Table 2: Vitrinite reflectance data and estimated paleotempera-
tures.

Tpeak = (ln (VRr) + 1.68)/0.0124, burial heating (Barker &

Pawlewicz 1986), ± 0.10 – standard deviation, (n = 50) – number
of measurements.

Vitrinite reflectance was measured on dispersed organic

matter on eleven shale samples (seven are positioned in
lacustrine and four in alluvial facies; Table 1) from the Pis-
kanja deposit and five coal samples from the Tadenje under-
ground coal mine (Tadenje sub-basin).

For the fission track analysis fifteen core samples (conglom-

erate  and  sandstone)  from  three  boreholes  (IBM-1,  IBM-2,
and  IBM-4)  in  the  Piskanja  deposit,  and  three  channel  sand-
stone  samples  between  coal  layers  in  the  Tadenje  sub-basin
were collected (Table 1, Fig. 2). Five samples of andesite, hy-
drothermally altered andesite, granodiorite and volcanoclastic
rocks, were taken from outcrops in the surrounding area in or-
der to study the tectono-thermal history (cooling and exhuma-
tion) of the basin margin and its relation to basin fill.

The detrital apatite and zircon may be derived from di-

verse sources, meaning that they carry information about the
thermal history of the sediment’s provenance regions. After
deposition the thermal history of the sediments can follow at
least  three  possible  scenarios:  i)  experienced  temperatures
were  not  high  enough  (above  the  partial  annealing  zone
(PAZ, 60 °C—120 °C) to cause annealing of the fission track
so that all the AFT single ages will be equal/slightly younger
or  older  than  the  depositional  age;  ii)  experienced  tempera-
tures were higher than PAZ for  ~ 10

Ma to cause total reset-

ting of the AFT single ages so that all the AFT single ages
are younger than the depositional age and iii) experienced
temperatures were in the range of the PAZ for a shorter period
of time > 10

Ma producing partially annealed grains with

AFT single ages older and younger than the age of deposi-
tion (Gleadow et al. 1986; Laslett et al. 1987; Wagner & van
den Haute 1992).

Vitrinite reflectance (VR)

For rank determination, the laminated dolomitic marl sam-

ples were cut, mounted in epoxy resin and polished, while
coal samples were crushed to a maximum particle size of

Sample Depth

(m)

Average vitrinite

reflectance %Rr

Estimated

paleotemperature (

IBM-1/1

43.5–44.5

0.66±0.10 (n=50)

102

IBM-1/2

47.0–47.9

0.68±0.11 (n=50)

104

IBM-1/3

63.2–66.8

0.71±0.08 (n=50)

108

IBM-1/4

122.8–123.9 0.76±0.09 (n=50)

113

IBM-1/6

127.0–128.2 0.69±0.09 (n=50)

106

IBM-1/7

195.4–196.6 0.77±0.09 (n=50)

114

IBM-1/8

226.3–227.6 0.77±0.09 (n=50)

114

IBM-1/27

344.2–344.5 0.76±0.09 (n=50)

113

IBM-1/29

352.2–353.2 0.74±0.08 (n=50)

111

IBM-1/31

381.9–382.0 0.69±0.07 (n=50)

106

IBM-2/21

394.7–395.2 0.63±0.06 (n=50)

Tadenje 11 47.6–48.6

0.87±0.03 (n=50)

125

Tadenje 14 49.6–50.3

0.86±0.03 (n=50)

124

Tadenje 1

68.4–68.6

0.90±0.02 (n=50)

127

Tadenje 10A 70.5–70.7

0.90±0.03 (n=50)

127

Tadenje 10B 70.7–71.0

0.90±0.03 (n=50)

127

THERMAL HISTORY, FISSION TRACK AND VITRINITE REFLECTANCE (MIOCENE IBAR BASIN, SERBIA)

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able 3:

Fission

track

results

from

the

Ibar

Basin.

–

apatite,

–

zircon,

–

number

counted

grains

per

sample,

ρρρρρ

(Nd)

–

density

dosimeter

tracks

(number

counted

dosimeter

tracks),

ρρρρρ

(Ns)

–

density

spontaneous

tracks

(number

counted

spontaneous

tracks),

ρρρρρ

(Ni

)

–

density

induced

tracks

(number

counted

induced

tracks),

χχχχχ

)

–

the

probability

obtaining

values

for

degrees

freedom

where

n=number

crystals-1.

Central

age

±1

(Ma)

(Galbraith

Laslett

1993),

MTL

±1

σσσσσ

(µm)

–

mean

track

length,

(µm)

(N)

–

standard

deviation

(number

horizontal

confined

tracks

measured),

Dpar

(µm)

–

mean

track

pit

length,

conc.

–

concentration

ppm.

ANDRIĆ, F

ÜGENSCHUH, ŽIVOTIĆ

and CVETKOVIĆ

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EOL

EOLOGICA CARPA

OGICA CARPA

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THICA, 2015, 66, 1, 37—50

1 mm, mounted in epoxy resin and polished. The reflectance
measurements were performed under a monochromatic light
of 546 nm using a Leitz MPV microscope and optical stan-
dards having a reflectance of 0.8999 % and 1.6999 % in oil,
following  the  procedures  outlined  by  Taylor  et  al.  (1998).
The  rank  was  determined  by  measuring  the  random  reflec-
tance on colotelinite B. The reflectance measurements were
performed  at  the  Department  für  Angewandte  Geowissen-
schaften und Geophysik, Montanuniversität Leoben.

During burial diagenesis of organic matter, the optical re-

flectivity of vitrinite increases as a result of increasing tem-
peratures.  As  vitrinite  reflectance  is  not  susceptible  to
retrograde alteration, it may be considered a geothermometer
for  maximum  paleotemperatures.  According  to  different  ki-
netic  models  and  field  studies,  vitrinite  reflectance  may  be
used with caution to estimate absolute maximum paleotem-
peratures,  as  shown  by  Barker  &  Pawlewicz  (1986).  They
published different vitrinite reflectance temperature correla-
tions  for  long-term  (burial)  and  short-term  (hydrothermal)
heating. Maximum paleotemperatures were calculated accord-
ing  to  the  methodology  explained  in  Barker  &  Pawlewicz
(1986) for burial heating, and the results are given in Table 2.

Apatite and zircon fission track analysis

The samples were mounted in epoxy resin (apatite) and

PFA  Teflon  (zircon)  after  conventional  mineral  separation
(crushing,  sieving,  magnetic,  and  heavy  liquid  separation)  at
the  University  of  Belgrade  and  partly  at  the  University  of
Innsbruck.  Etching  of  apatite  mounts  were  done  in  6.5%
HNO

at 20 °C for 40 s. Zircon mounts were etched in a

NaOH—KOH eutectic melt for 4—8 h at 235 °C. Induced tracks
in  external  detector  muscovite  were  etched  in  40%  HF  for
45 min at 20 °C. Irradiation was carried out at FRMII Garching
(Technische  Universität  München,  Germany).  Neutron  flux
was monitored using CN5 and CN1 dosimeter glasses for apa-
tite  and  zircon,  respectively.  Densities  of  spontaneous,  in-
duced  tracks  and  for  the  apatites  confined  horizontal  lengths
and Dpar measurements were performed on a Zeiss Axioplan
microscope  equipped  with  Autoscan

, System at 1250

magnification, dry objective at

the University of Innsbruck.

All  samples  have  been  analysed  using  an  external  detector
(Gleadow  1981).  The  fission-track  central  ages  were  deter-
mined  using  zeta  approach  (Hurford  &  Green  1983)  with
zeta factors of 330 ± 9.45 for the apatite (CN5 dosimeter glass)
and 144 ± 12.89 for the zircon, (CN1 dosimeter glass) (analyst
Nevena Andrić). The AFT and ZFT central ages are reported
with 1

σ error (Galbraith & Laslett 1993). The TRACKKEY

program, version 4 was used in data processing (Dunkl 2002).
The homogeneity of the age population was determined by
Chi (

) test (Gleadow et al. 1986; Galbraith & Laslett 1993).

The Dpar method (Donelick 1993; Burtner et al. 1994) was
used as a proxy for annealing properties. For identification
of different age components or peak ages for the samples
with spread ages, the binomial peak-fitting method was used
(Galbraith & Green 1990; Brandon 2002 ).

The analytical results are given in Table 3 and location of

the samples in Fig. 2. Due to the quality of the apatite and
zircon grains it was not possible to obtain the age pairs (AFT

Fig. 3. Vitrinite ref-
lectance. a – IBM-1
borehole,

Piskanja

deposit, b – Tadenje
underground

coal

mine (Tadenje sub-
basin).

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Fig. 4. a – The ZFT single grain age
distribution  in  the  Piskanja  deposit,
b  –  Frequency  distribution  of  the
apatite  single-grain  ages  from  the
Piskanja  deposit  with  statistically
separated  detritial  populations,  using
the  BinomFit  software  (Brandon
2002), vertical thick black line repre-
sents  stratigraphic  age

19 Ma

(Prysjazhnjuk et al. 2000; Krstić et al.
2001). Zr – zircon, Ap – apatite.

and ZFT) for each sample. Modelling of the apatite age and
track-length  distribution  data  was  carried  out  with  the  pro-
gram  HeFTy  (Ketcham  et  al.  2003).  The  input  parameters
were  AFT  age  data,  track  length  distributions  and  etch  pit
diameters  (Dpar).  Time-temperature  boxes  were  defined  by
additional input constraints for the model, namely: ZFT and
AFT central, single ages and geological constraints. The par-
tial annealing zone (PAZ) of apatite is constrained between
120 °C and 60 °C (Laslett et al. 1987) and of zircon ~ 200 °C
and 320 °C (Tagami et al. 1998). The present day tempera-
ture on the surface was set to 20 °C. The generation of time-
temperature  paths  was  done  using  the  inverse  Monte  Carlo
algorithm (Ketcham 2005). The c-axis projections were cor-
rected  using  the  annealing  model  of  Ketcham  et  al.  (2007).
The modelling results were statistically evaluated by the good-
ness of fit (GOF) of measured and modelled data. The value
> 0.5 between modelled and measured data was considered a
“good” fit, while a value of 0.05 or higher was “acceptable”.

Results

Vitrinite reflectance data

The vitrinite reflectance results vary from 0.63 to 0.90 %Rr

(Table 2) implying a bituminous stage of organic matter. In
the boreholes IBM-1 and IBM-2 (Piskanja deposit) the vitrin-

ite reflectance values do not show a pronounced depth trend.
The  data  are  spread  between  0.63 %  and  0.77 %Rr,  whereas
most  values  are  overlapping  within  one  standard  deviation
(0.11—0.07 %;  Table 2,  Fig. 3).  The  vitrinite  reflectance  in
coal  seams  from  the  Tadenje  sub-basin  (northern  part  of  the
basin)  increases  from  0.86 %  at  47.60 m  to  0.90 %Rr  at
71.00 m.  Typical  coalification  temperatures  for  the  bitumi-
nous coals with such vitrinite reflectance values are approxi-
mately  100—130 °C  (Barker  &  Pawlewicz  1986).  The  higher
values in the Tadenje sub-basin indicate higher maximum pa-
leotemperatures than in the Piskanja deposit.

Zircon and apatite fission track data

The samples in the Piskanja deposit yielded ZFT central

ages from 28.7 ± 2.8 Ma to 31.5 ± 3.1 Ma (Table 3, Fig. 4a).
All samples pass the

test indicating single grain age popu-

lation of zircons (P (

) > 5 %, Galbraith 1981). The AFT

central ages range between 21.5 ± 2.2 Ma and 30.4 ± 2.5 Ma,
whereas  single  grain  ages  range  from  6.7 Ma  to  45.0 Ma
(Table 3,  Fig. 5).  The  mean  track  length  varies  from
12.32 ± 2.23 µm to 10.11±1.97 µm (Table 3, Fig. 6). The sam-
ples  IBM-1/22,  IBM-1/30,  IBM-2/15,  IBM-2/17,  IBM-2/19,
and IBM-4/44 contain one apatite single grain age population,
meaning that they pass the

test (P (

) > 5 % – Galbraith

1981). The samples IBM-1/23, IBM-1/24, IBM-1/25, IBM-1/28
and IBM-4/41 failed the

test (P (

) < 5% – Galbraith

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1981), suggesting more than one single grain age population.
Samples  IBM-1/23,  IBM-1/25,  IBM-1/28,  and  IBM-1/30
contain two subpopulations, statistically separated (Fig. 4b).
The  first  subpopulation  comprises  peaks  at  17.1 ± 1.7 Ma
(IBM-1/23),  7.1 ± 2.1 Ma  (IBM-1/25)  and  13.2 ± 2.5 Ma
(IBM-1/28)  which  are  younger  than  the  age  of  deposition
(Fig. 4b). The second subpopulation is characterized by peaks
older  than  the  age  of  deposition,  34.8 ± 2.3 Ma  (IBM-1/23),
28.2 ± 2.3 Ma (IBM-1/25) and 27.9 ± 2.7 Ma (IBM-1/28).

In the Tadenje sub-basin the ZFT central ages are

18.0 ± 1.7 Ma  and  20.0 ± 2.1 Ma  (Table 3,  Fig. 6).  The  AFT
central ages are 16.6 ± 1.4 Ma and 19.9 ± 2.0 Ma (Fig. 5) with
mean  track  lengths  of  9.90 ± 2.45 µm  and  11.44 ± 2.59 µm.
All  samples  (apatite  and  zircon)  pass  the

test, indicating

that all single grains belong to the same population (P (

)

> 5% – Galbraith 1981). Thermal modelling of these sam-
ples (Tadenje 12 and Tadenje 15) revealed post-depositional
heating with maximum temperatures around 100 °C (Fig. 8).
The heating lasted from 18—17 to 10—8 Ma. Cooling started
at about 10—8 Ma and reached the present-day temperature
of 28 °C at a depth of 70 m.

The ZFT central ages of the outcropping magmatic rock in

the  basin  margin  range  from  17.8 ± 1.9 Ma  to  25.3 ± 2.5 Ma
(Table 3). The AFT central ages range between 15.3 ± 1.3 Ma
and  18.2 ± 1.6 Ma  (Table 3).  The  samples  have  mean  track
length  between  12.19 ± 2.51 µm  and  14.21 ± 1.05 µm.  With

Fig. 5. The AFT single grain age distribution in Piskanja and Tadenje deposit. Vertical thick black line represents stratigraphic age ~ 19 Ma
(Prysjazhnjuk et al. 2000; Krstić et al. 2001).

the exception of 9-Kremići, all samples pass the

test indi-

cating a homogenous population (P (

) > 5 % – Galbraith

1981).  The  fission  track  analysis  of  the  Biljanovac  volcano-
clastites gave similar zircon and apatite ages, of 19.2 ± 2.1 Ma
and 18.4 ± 1.5 Ma, respectively and relatively long mean track
length, 13.21 ± 1.73 µm (Table 3, Figs. 6, 7). Thermal model-
ling reveals that 1-Biljanovac sample underwent fast cooling
through  both  zircon  and  apatite  PAZ,  from  20 Ma  to  18 Ma
(Fig. 8).  The  cooling  history  of  sample  4-Kremići  indicated
rapid  cooling  from  above  ZPAZ,  namely  300 °C  to  around
80 °C (20—17 Ma), followed by slower cooling to the surface
temperatures  (Fig. 8).  This  scenario  is  reflected  in  identical
zircon and apatite ages (17.8 ± 1.9 Ma and 17.1 ± 1.4 Ma) and
long mean track length (14.21 ± 1.05 µm).

Discussion

Compilation of new VR, AFT, ZFT data and literature data

enabled reconstruction of the Ibar basin’s evolution, empha-
sizing its thermal history. The low temperature thermochro-
nology  and  new  vitrinite  reflectance  data  on  the  Miocene
syn-kinematic  sediments  of  the  Ibar  supradetachment  basin
documented  post-depositional  thermal  overprint  and  pro-
posed mechanism that controlled the thermal state of the ba-
sin. The correlation between AFT and ZFT ages of basement

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rocks and ages of basin fill indicated synchronous basement
(source area) exhumation and deposition in the basin.

The ZFT central ages of the sediments from Ibar Basin are

similar to the depositional age (Table 3). This means that the
zircons  have  preserved  the  information  about  the  cooling
history  of  the  source  region  from  where  they  were  eroded
(Hurford  &  Carter  1991;  Wagner  &  van  den  Haute  1992).
The  presence  of  andesitic  fragments  in  conglomerates  and
sandstones  from  Piskanja,  together  with  ZFT  age  distribu-
tion  suggests  Oligocene  andesite  as  one  of  the  dominant
sediment  sources  (Figs. 5,  6,  7).  In  the  Tadenje  sub-basin
ZFT  single  age  spectra  in  the  sandstones  correspond  to  the
age  spectra  of  outcropping  volcanoclastites  (1-Biljanovac,
Fig. 6a). The andesites and their volcanoclastic counterparts
formed  the  paleorelief  in  this  part  of  the  basin,  which  fur-
thermore  implies  that  these  rocks  were  most  probably  the
source for sediments. This is further supported by the pres-
ence of apatite grains with subhedral shape and black inclu-
sions (Fig. 6b), which are observed only in the 1-Biljanovac
volcanoclastite  and  sandstones  from  the  Tadenje  sub-basin.
The close ages between the detritial grains and age of depo-

sition suggest fast exhumation of the basement source rocks
during the Early Miocene and synchronous erosion and sedi-
mentation. The thermal modelling of the 4-Kremići grano-
diorite sample supports that conclusion (Fig. 8).

In the Ibar Basin AFT central ages are older (Piskanja) or

slightly  younger  (Tadenje)  than  the  age  of  deposition
(Fig. 5).  The  apatite  single  grain  age  spectra  of  the  studied
sediments showed spread AFT single grain ages with a sig-
nificant number of grains, which are younger than the age of
deposition (Fig. 5). This implies that the apatites in the sedi-
ments are partially annealed (Green et al. 1986; Laslett et al.
1987;  Wagner  &  van  den  Haute  1992)  due  to  post-deposi-
tional  thermal  overprint  supported  by  vitrinite  reflectance
data. Although the apatites were exposed to maximum paleo-
temperatures of  ~ 120 °C (vitrinite reflectance data), the de-
tritial  apatites  still  contain  older  age  components  and  broad
track  length  distribution  as  evidence  of  partial  resetting
(Figs. 5, 6, 7). This implies that the apatites must have experi-
enced elevated temperatures for a relatively short time, given
that after 10 Ma at such temperatures total annealing of fission
tracks  in  apatites  should  have  occurred  (Laslett  et  al.  1987).

Fig. 6. a – Single grain age distribution of zircon (zr) and apatite (ap) in selected samples. Vertical thick black line represents stratigraphic
age ~ 19 Ma (Prysjazhnjuk et al. 2000; Krstić et al. 2001), b – Apatite morphology in samples 1-Biljanovac, Tadenje 12 and Tadenje 15.

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The thermal modelling supports this conclusion that the apa-
tites were annealed between 17 Ma and 10—8 Ma (Fig. 8).

In the Piskanja deposit the evidence of the post-deposi-

tional thermal overprint ( ~ 100—120 °C, vitrinite reflectance;
Table 2)  is  noticed  only  in  the  AFT  samples  from  borehole
IBM-1  and  from  the  deepest  parts  of  IBM-2  (IBM-2/17,
IBM-2/19).  The  samples  from  IBM-4  and  IBM-2/15  holes
seem to be unaffected by the thermal overprint. The thermal
overprint intensity in the boreholes decreases laterally from
IBM-1  to  IBM-4  and  this  implies  decreasing  temperatures
towards the basin center. That could, tentatively, suggest this
thermal overprint was more local influencing only the mar-

Fig. 7. Apatite fission track length distribution in the studied sediments. MTL – mean track length, SD – standard deviation, n – num-
ber of tracks.

gin of the Piskanja deposit. Again tentatively, the time frame
of this thermal perturbation could be inferred from the
youngest AFT peak age subpopulation in the borehole IBM-1,
~

7.1 Ma (Fig. 4b).

In the Tadenje sub-basin, the current overburden of 70 m

is  very  much  less  than  that  required  to  explain  the  deduced
paleotemperatures (120—130 °C, Table 2) and significant an-
nealing of the apatites in the sediments (Fig. 5). In the case
of the present day average geothermal gradient ( ~ 25—30 °C/km
–  Milojević  1993;  Lenkey  et  al.  2002)  the  expected  over-
burden  necessary  for  such  paleotemperatures  is  between  4
and 5 km. This overburden should be considered as a maxi-

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Fig. 8.

–

Modelled

thermal

history

basement

rocks

(Kremići

granitoid

and

Biljanovac

volcanoclastics).

The

black

boxes

represents

delling

constraints,

ZFT

and

AFT

ages

including

their

errors within zircon

(

200

°C and 320

°C – Tagami et al. 1998) and apatite (between 60

°C and 120

°C – Laslett et al. 1987) partial annealing zone,

– Modelled thermal histories

detrital

AFT

data

the

Tadenje

deposit.

The

starting

T-t

boxes

are

established

the

onset

deposition

2 Ma,

when

samples

were

forced

the

surface

and

(partially)

annealed

AFT

single

grain

ages

including

their 1

errors

when

samples

were

within

the

APAZ.

APAZ

–

apatite

partial

annealing

zone.

The

light

grey

envelopes

represent

acceptable

and

the

dark

grey

ones

good

fits

between

modelled

and

measured

data.

Vertical

thick

black

line

represents

stratigraphic

age

19 Ma

(Prysjazhnjuk

al.

2000;

Krstić

al.

2001).

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mum estimate, based on assumed higher geothermal gradi-
ents due to intense magmatic activity during the Miocene in
this region.

The formation of the Ibar Basin is related to the exhuma-

tion  of  the  Studenica  and  Kopaonik  core-complexes  during
the  Early  Miocene  (from  21—17 Ma  to  10 Ma  –  Schefer
2010). This stage was characterized by rapid decompression
and  by  normal-shearing  within  the  detachment  evident  by
syn-deformational  emplacement  of  the  Polumir  granitoid
(Schefer  2010).  In  the  same  period  ( ~ 19 Ma)  the  hanging
wall subsided along the detachment creating accommodation
space for the basin fill.

The provenance ZFT ages in the studied sediments suggest

contemporaneous fast exhumation, erosion and sedimentation.
The  deposition  was  followed  by  heating  from  around  17 Ma
reaching  the  maximal  paleotemperatures  of  ~ 120—130 °C
around 10—8 Ma when subsequent cooling to the present day
temperatures started (Fig. 8). This heating phase is contem-
poraneous with the juxtaposition of the warmer lower crustal
rocks  (Studenica  and  Kopaonik  metamorphic  domes)  with
the upper crust (including the Ibar Basin). The thermal evo-
lution of the footwall, based on t-T paths of the Kremići (this
study),  Kopaonik,  Željin,  Drenje,  and  Polumir  plutons
(Schefer  et  al.  2011),  indicates  continuous  rapid  cooling
between  ~ 16  and  10 Ma  from  ~300 °C  to  60 °C  (Fig. 8;
4-Kremići  sample).  Along  the  contact  between  warm  foot-
wall  and  cold  hanging  wall  thermal  gradient  is  the  highest,
enabling  heat  transfer  by  conduction  affecting  the  basin  fill
(Souche et al. 2012).

Higher vitrinite reflectance values and a higher degree of

partial  resetting  in  apatites  in  the  Tadenje  sub-basin  com-
pared to the Piskanja deposit could be the result of a different
primary  stratigraphic  position  of  the  samples.  On  the  other
hand, gradual exhumation of the metamorphic dome can cre-
ate an asymmetry of temperatures in the basin which increases
towards the detachment (Souche et al. 2012). This tempera-
ture asymmetry can produce differences in thermal overprint
within  the  basin.  The  cooling  in  the  basin  after  10—8 Ma  is
probably  related  to  the  basin’s  inversion  and  erosion.  The
more local heat source which only affected the Piskanja de-
posit, mostly along its margin, could be additionally attributed
to nearby magmatic and/or hydrothermal activity, the effects
of which are seen from stratabound mineralizations of boron,
magnesite and travertine. The inferred time for this activity
perfectly overlaps with the youngest phase of high-K calc-al-
kaline  to  shoshonitic  and  ultrapotassic  volcanic  activity  in
Serbia (Cvetković et al. 2004).

Conclusion

The result of vitrinite reflectance and apatite fission track

data helped to quantify the thermal overprint of the Ibar Ba-
sin, reaching the maximum paleotemperatures of around
120—130 °C. The higher values of vitrinite reflectance in the
Tadenje sub-basin indicate higher maximum paleo-tempera-
tures than in the Piskanja deposit. The modelled thermal his-
tory of the detrital apatites indicates heating episode from
around 17 Ma ago to around 10—8 Ma when cooling began.

In the Piskanja deposit (southeastern part of the Ibar Basin) a
local heat source may have caused an additional thermal per-
turbation around ~ 7.1 Ma.

The ZFT ages in the studied sediments suggest contempo-

raneous rapid tectonic exhumation, erosion and sedimenta-
tion during the Early Miocene time.

The thermal history of the Ibar Basin was controlled by

exhumation  and  cooling  of  the  Studenica  and  Kopaonik
core-complex. The rapid cooling of the Studenica and Kopa-
onik  footwall  transferred  heat  to  the  basin  in  the  hanging
wall. The termination of the heating episode in the hanging
wall units and the onset of cooling (10—8 Ma) imply changes
in  tectonic  settings  from  extension  to  basin  inversion  and
erosion.

The thermal evolution of the Inner Dinarides was most

likely controlled by the Miocene extension accompanied by
crustal melting, mass and heat transfer via detachments and/or
due to volcanism ± hydrothermal activity.

Acknowledgments:  This  research  was  financed  by  the
DOSECC  Research  Grant  and  by  the  Ministry  of  Education
and  Science  of  the  Republic  of  Serbia  (Projects 176019,
176016  and  176006)  which  is  gratefully  acknowledged.  We
are also grateful to PD Dr. Alexandre Kounov, Doc. Rastislav
Vojtko,  and  the  anonymous  reviewer  whose  helpful  sugges-
tions and comments greatly benefited this paper. The authors
are grateful to Prof. Vladimir Simić for his support, construc-
tive comments, and suggestions, and to the RKU Ibarski Rud-
nici uglja (Ibar Coal Mines) for providing cores and samples
from the Tadenje and Jarando sub-basins.

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