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Origin and geodynamic evolution of LatePaleogene magmatic associations along thePeriadriatic-Sava-Vardar magmatic beltJakob Pamić a , Dražen Balen b & Marijan Herak c
a Croatian Academy of Sciences and Arts , Ante Kovačiéa 5, 10000 , Zagreb , Croatiab Institute for Mineralogy and Petrology, Department of Geology, Faculty of Science,University of Zagreb , Horvatovac bb, 10000 , Zagreb , Croatiac Department of Geophysics, Faculty of Science , University of Zagreb , Horvatovacbb, 10000 , Zagreb , CroatiaPublished online: 30 May 2012.
To cite this article: Jakob Pamić , Dražen Balen & Marijan Herak (2002) Origin and geodynamic evolution of LatePaleogene magmatic associations along the Periadriatic-Sava-Vardar magmatic belt, Geodinamica Acta, 15:4, 209-231,DOI: 10.1080/09853111.2002.10510755
To link to this article: http://dx.doi.org/10.1080/09853111.2002.10510755
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ELSEVIER Geodinarnica Acta 15 (2002) 209-231
Geodinamica Acta
www.elsevier.comllocate/geoact
Origin and geodynamic evolution of Late Paleogene magmatic associations along the Periadriatic-Sava-Vardar magmatic belt
Jakob Pamic a, Drazen Balen b.*, Marijan Herak c
"Croatian Academy of Sciences and Arts, Ante Kovacica 5, 10000 Zagreb, Croatia bJnstitute for Mineralogy and Petrology, Department of Geology, Faculty of Science, University of Zagreb, Horvatovac bb, 10000 Zagreb, Croatia
c Department of Geophysics, Faculty of Science, University of Zagreb, Horvatovac bb, 10000 Zagreb, Croatia
Received 6 November 2001; accepted 7 June 2002
Abstract
Along the Periadriatic Lineament in the Alps and the Sava-Vardar Zone of the Dinarides and Hellenides, Paleogene magmatic associations form a continuous belt, about 1700 km long. The following magmatic associations occur: (1) Eocene granitoids; (2) Oligocene granitoids including tonalites; (3) Oligocene shoshonite and calc-alkaline volcanics with lamprophyres; (4) Egerian-Eggenburgian (Chattian) calc-alkaline volcanics and granitoids. All of these magmatic associations are constrained by radiometric ages, which indicate that the magmatic activity was mainly restricted to the time span between 55 and 29 Ma. These igneous rocks form, both at surface and in the subsurface, the distinct linear Periadriatic-Sava-Vardar magmatic belt, with three strikes that are controlled by the indentation of Apulia and Moesia and accompanying strike-slip faulting. The geology, seismicity, seismic tomography and magnetic anomalies within this belt suggest that it has been generated in the African-Eurasian suture zone. Based on published analytical data, the petrology, major and trace element contents and Sr, Nd and 0 isotopic composition of each magmatic association are briefly defined. These data show that Eocene and Oligocene magmatic associations of the Late Paleogene Periadriatic-Sava-Vardar magmatic belt originated along a consuming plate margin. Based on isotopic systems, two main rock groups can be distinguished: (1) 87Sr/86Sr = 0.7036-0.7080 and 6 180 = 5.9-7.2%o, indicating basaltic partial melts derived from a continental mantle-lithosphere, and (2) 87Sr/86Sr = 0.7090--72131 and 6180 = 7.3-11.5%o, indicating crustal assimilation and melting. The mantle sources for the primary basalt melts are metasomatized garnet peridotites and/or spinel lherzolites and phlogopite lherzolites of upper mantle wedge origin. The geodynamic evolution of the plutonic and volcanic associations of the Periadriatic-Sava-Vardar magmatic belt was related to the Africa-Eurasia suture zone that was dominated by break-off of the subducted lithospheric slab of Mesozoic oceanic crust, at depths of 90--100 km. This is indicated by their contemporaneity along the 1700 km long belt.© 2002 Editions scientifiques et medicales Elsevier SAS. All rights reserved.
Keywords: Geodynamics; Late Paleogene; Magmatic associations; Periadriatic-Sava-Vardar magmatic belt
1. Introduction
The Alpine mountain system of Europe originated by subduction and collision of Tethys between Africa and Eurasia. The western part of the Alpine-Himalaya includes several mountain systems (se.e index-sketch, Fig. IA), and three of them, the Alps, Dinarides and Hellenides, are
* Corresponding author. E-mail address: [email protected] (D. Balen).
© 2002 Editions scientifiques et medicales Elsevier SAS. All rights reserved. PII: S 0 9 8 5-3 1 I 1 ( 0 2) 0 1 0 8 9- 6
characterized by comparatively large masses of Paleogene plutonic and volcanic rocks [1-4]. In the Alps, these are located in the Periadriatic Lineament area, whereas in the Dinarides and H~llenides, they are found in the Vardar (Axios in Greece) Zone of the Dinarides and Hellenides.
The Periadriatic Lineament and the Sava-Vardar Zone were interpreted as "die Narbenzone" [5,6] separating the south- to southwest-verging "southern" mountain systems (the Southern Alps, Dinarides and Hellenides) from the north- to northeast- to east-verging "northern" mountain systems (the Eastern Alps, Carpathians and Balkan), with the Pannonian Basin in between (see Fig. IA, B). In modem
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Distance along the profile, km
Fig. 1. (A) Index-sketch showing mountain systems of the "southern" and "northern" branch of the Alpine-Himalaya belt. (B) Tectonic sketch map of the Alps, Dinarides and Hellenides showing position of the Periadriatic Lineament and Sava-Vardar suture zone; modified after Aubouin et a!. [12] and Dimitrijevic [108]. I, External units; 2, internal units; 3, Periadriatic-Sava-Vardar Zone; 4, Serbo-Macedonian Massif; 5, Pelagonide; 6, Golija Zone; 7, Zagorje-Mid-Transdanubian Zone; 8, Pannonian Basin. Faults: BL, Balaton; CL, Canavese Line; DF, Drava; GL, Giudicaria; MBF, Main Balkan; PL, Periadriatic; SF, Sava; SN, Sava Nappe; SP, Skadar-Pec; ZZ, Zagreb-Zemplin; P wavp, tomographic P-wave velocity anomaly [24-27]. (C) Contours of the Mohorovicic discontinuity depth (present state) beneath southeastern Europe; after Skoko eta!. [109]. (D) Crustal profile of Canavese-Thessaloniki along the Periadriatic Lineament and Sava-Vardar suture zone (broken line in (C)) and hypocenters of earthquakes (circles) with magnitudes M ~ 4.0 within 30 km of the profile. Earthquake data from the combined CNSS (2000) earthquake catalog [20] and an updated version of the Croatian Earthquake Catalog [21].
geodynamic considerations, the "southern branch" forms the suture zone that evolved in response to the collision of Arabia-Apulia with Tisia-Moesia [7].
The tectonostratigraphic units of the Dinarides link up to the northwest with the Alps. However, the Dinarides/Alps boundary is ill defined. Since Suess [8], it is accepted that the Alps extend continuously southeastward into the Dinarides. However, this is only partly true, as only the Southern Alpine units continue into the External Dinarides, whereas the Internal Dinaridic units wedge out northwestward of the Zagreb-Zemplin Line into the Zagorje-Mid-Transdanubian Zone or the Sava Zone [9,10] (Fig. 1B). On the other hand, all tectonostratigraphic units of the Dinarides continue
southeastward into the Hellenides under different names [11,12].
The Periadriatic Lineament (PL) extends eastward and links up in the subsurface of the Pannonian Basin (PB) with the northeast-trending Balaton Line [13] (Fig. 2B). However, the Periadriatic-Balaton Lineament does not represent a suture zone, but separates two geotectonic units, namely the Tisia and Pelso [13] or Alcapa units [14]. Paleogene magmatic associations can be traced from the PL area southeastward of the Zagreb-Zemplin Line along the dextral strike-slip Sava and the Vardar fault systems or the Main Balkan Fault [15], separating the Dinarides and Hellenides from the South Carpathians and West Balkan [16]. Kossmat
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[ 17] first defined the Vardar Zone, restricting its occurrence to Macedonia and southern Serbia. Afterward, it was recognized that the zone continues northward and northwestward [11] in the area of the Sava River (Fig. lB). For convenience, the zone was recently renamed the Sava-Vardar Zone (SVZ) [18].
In the SVZ, Paleogene magmatic rocks are as common as along the PL, as documented by geophysical, geological, geochronological and petrological data [19]. These Paleogene magmatic rocks form a coherent and prominent Periadriatic-Sava-Vardar magmatic belt (PSVMB), which can be traced along strike for about 1700 km from the Canavese Line in the Alps to Thessaloniki on the Aegean Sea (Fig. lB).
Numerous papers have been published on the geology, geochronology, petrology and geochemistry of the Paleogene Periadriatic tonalites and contemporaneous volcanics. Recently, analytical data, unfortunately not as voluminous and precise as for the PL, have been published for the southeastern prolongation of the PL, i.e., the SVZ of the Dinarides and the Hellenides. The aim of this paper is to review basic geophysical, geological, petrological and geochemical data concerning the Late Paleogene magmatic associations of the PSVMB forming the basis for the geodynamic and petrologic synthesis that follows. Our attention focuses on magmatic associations from the SVZ, for which many papers, addressing separate, small areas, were published, mainly in local languages and journals, and thus are not readily accessible to the international geological community.
2. Geophysical data
The Alpine-Himalayan belt is characterized by high seismicity. However, the seismicity of the PSVMB is moderate and is slightly higher in its southern parts (Fig. lD). This seismic activity is characterized by rather infrequent earthquakes, which, nevertheless, can be of large magnitudes. Events with magnitudes exceeding M = 5.5 in the period since 1960 occurred only in some parts of the PSVMB near Thessaloniki, Guevgueli, Skopje, Mt. Kopaonik and the Sava Depression [20,21]. Strong events occurred earlier also in the area south of Belgrade, in the Zagreb epicentral area and in the area of the Drava Depression, i.e., along the Drava Fault (Fig. lB). All reliably located foci lie in the upper crust.
Along the PSVMB, crustal thickness varies between 25 and 45 km, as shown in Fig. lC and maps for the Mediterranean region [22]. Aljinovic et al. [23] fitted analytical regression surfaces of the first up to the fourth order to the available data on the Mohorovicic depth. The corresponding residual surfaces point out those parts of the Mohorovicic depths that are systematically deeper or shallower than indicated by the "smoothed-out" regression surface. These
residuals generally correlate with surface geological structures and were probably caused by tectonic processes.
Recent seismic delay-time tomography data [24,25] indicate that at 95 and 195 km depths, there is a distinct positive P-wave velocity anomaly extending from the area of the PL and the northern end of the Adriatic Sea southeastward along the northern and southeastern Dinarides as far as the Aegean Sea. These high-velocity anomalies are considered to image the sinking subducted lithospheric slab dipping to the northeast at an angle of about 45° [25-27]. Geographically, this high-velocity region approximately coincides with the area where first-order Mohorovicic-depth residuals are positive. The low-velocity anomaly at about 145 km depth in the Dinarides and the Hellenides suggests that the subducted slab in this region is detached from the overlying lithosphere, whereas further south in the Aegean area and along the Cretan arc, it is still unbroken. Apparently, detachment of the subducted slab from the lithosphere commenced in the Northern Dinarides not earlier than in Oligocene time and has propagated southeastward since then.
The boundaries of the SVZ are well documented by positive and negative magnetic anomalies with intensities of more than 100 nT [28]. The first anomaly zone stretches approximately along the south-southwestern boundary of the SVZ, i.e., along the contact with the Dinaride Ophiolite Zone. The second magnetic anomaly zone runs approximately along the north-northeastern margin of the SVZ and thus corresponds to the boundary of the Dinarides-Hellenides and Moesia-Tisia, i.e., the central and southeastern parts of the PSVMB (Figs. 1 and 2B, C). These magnetic anomalies indicate the presence of granitoid bodies, which are more abundant in the subsurface of the SVZ than those that outcrop at the surface.
3. Geological data
Along the PSVMB, the original contact between Apulia, the European foreland and Tisia and Moesia was a Late Cretaceous/Early Paleogene, S-dipping subduction zone in the Alps and a northeast- and east-dipping subduction zone in the Dinarides and Hellenides. Subsequent Tertiary orogenic processes modified their geometry [29].
Along the PSVMB, the following magmatic associations occur: (1) syncollisional Eocene granitoids; (2) syncollisional Oligocene granitoids and related rocks; (3) Oligocene shoshonite and high-K calc-alkaline volcanics with lamprophyres; (4) Egerian-Eggenburgian (Chattian) calc-alkaline volcanics; and (5) coeval granitoids. All these rocks are unevenly distributed, with a predominance of granitoids along the PL in the Alps and shoshonitic and calc-alkaline volcanics in the SVZ of the Dinarides and Hellenides due to a difference in erosion level. These rocks form a distinctly linear PSVMB, the strike of which was modified by strike-slip faulting during the postorogenic indenting of
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Fig. 2. Simplified geological maps. (A) Croatian and Slovenian parts of the Zagorje-Mid-Transdanubian Zone [110-112] with inset sketch map of the Periadriatic area [2]: I, Eastern Alps; 2, Southern Alps; 3, tonalite plutons. (B) Northwestern part of the Sava-Vardar Zone adjoining South Tisia [46,113]. (C) Southeasternmost part of the Sava-Vardar Zone adjoining the Serbo-Macedonian Massif [3]; faults: SP, Skadar-Pec; VF, Vardar. 1, Neogene and Quaternary sediments ofthe Pannonian Basin; 2, Egerian-Eggenburgian (Chattian) sediments; 3, Egerian-Eggenburgian (Chattian) volcanics (a) and plutonic rocks (b); 4, Oligocene post-syncollisional granitoids, including tonalites; 5, Oligocene shoshonitic volcanics and pyroclastics: (a) outcrops, (b) oil wells; 6, Eocene syncollisional granitoids: (a) outcrops, (b) oil wells; 7, Vardar Zone formations: Cretaceous-Early Paleogene flysch, Paleogene regionally metamorphosed sequences and ophiolite melange: (a) outcrops, (b) oil wells; 8, Dinaridic Ophiolite Zone; 9, allochthonous Paleozoic-Triassic formations underthrust by ophiolites (Golija Nappe); 10, Paleozoic and Triassic formations of the Sava Nappe; 11, Adriatic-Dinaridic carbonate platform; 12, Paleozoic units of South Tisia, Pelagonide, Serbo-Macedonian Massif and Rhodope; 13, Austroalpine domain; 14, fault; 15, nappe. Main faults: DF, Drina; IF, Ilova; JSN, Julian-Savinja Nappe; LF, Lavental; NBLF, Nasice-Banjaluka; NMFSD, northern marginal fault of the Sava Depression; PL, Periadriatic; PBL, Periadriatic-Ba1aton; SF, Sava; SN, Sava Nappe; SMFDD, southern marginal fault of the Drava Depression; SMFSD, southern marginal fault of the Sava Depression; ZZ, Zagreb-Zemplin.
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Apulia and Moesia [29-31]. The following three segments are recognized: (1) an approximately east-west-striking Periadriatic segment; (2) a west-northwest-east-southeastdirected Sava segment; and (3) a north-northwest-southsoutheast- striking Vardar segment (Figs. 1B and 2A-C). The linear nature and the lateral continuity of these Paleogene magmatic associations suggest that they developed along a structure some 1700 krn long. On the other hand, the gradual deflection from the east-west strike in the Periadriatic area to the north-northwest-south-southeast strike of the Vardar-Thessaloniki Zone reflects gradually decreasing effects of Tertiary Apulian north-northwest and Moesian east indentations.
As a consequence, the Dinarides and Hellenides were much less shortened than the Alps [32,33]. Therefore, paleogeographic associations that originated in different Tethyan environments were better preserved in the structure of the Dinarides and the Hellenides (Fig. lB) [11,34]. The SVZ represents the most internal tectonostratigraphic unit, characterized by Cretaceous-Early Paleogene turbidites intruded by Late Paleogene magmatic associations. The basal parts of the Cretaceous-Early Paleogene sediments are locally interlayered with subduction-related basalts and rhyolites and are accompanied by ophiolite melanges that originated in a back-arc basin [34]. The melanges include smaller and larger mappable fragments of Paleozoic-Triassic and Jurassic formations [9,18,34,35]. These subductionrelated units were affected by Eocene (55-45 Ma) compression that was accompanied by (1) termination of Tethyan subduction and tectonization of the ophiolite melange and its obduction; (2) Alpine medium-grade metamorphism of the Cretaceous-Early Paleogene formations and a synkinematic granite plutonism; and (3) final structuration of the Dinarides and Hellenides and their uplift [34,35].
These SVZ units gradually die out northwestward in the Zagorje-Mid-Transdanubian Zone (i.e., transitional Alpine-Dinaridic Zone) [9,36]. Westward along the PL, where Apulian indentation reaches its maximum, these units wedge out (Fig. lB).
3.1. The Periadriatic Lineament area
In the Periadriatic Lineament area, the oldest Late Alpine igneous rocks are Oligocene granitoids (Fig. 2A), which occur within the north-verging Austroalpine domain (e.g., Mt. Pohorje), along the lineament itself (e.g., Mt. Karavanke) and within the Southern Alps (e.g., Adamello) [2]. The Apulian indentation [29] gave rise to 500 km shortening in the Alps [32,33,37] and to a transpressional dextral strike-slip faulting [37]. It commenced in the eastern parts during the Early Miocene (24-17.5 Ma), and after a short period of transtension, during the Karpatian (Burdigalian) (17.5-16.5 Ma), dextral transpression resumed during the Middle Miocene to Pliocene and lasted until Quaternary times [38].
In the westernmost parts of the PL area, the Sesia-Lanzo Zone Oligocene shoshonites, andesites and ultrapotassic lamprophyric dykes also occur. Beside these, numerous Oligocene mafic to acidic dykes have been reported from the entire PL [1,39-41] (Fig. lB).
Published radiometric data (Table 1) show that plutonic activity peaked sharply between 33 and 29 Ma [42] as in the Sesia-Lanzo area [39].
3.2. The Zagorje-Mid-Transdanubian Zone
The Zagorje-Mid-Transdanubian Zone (ZMTZ), or the Sava Zone, is about 30-40 km wide and includes both Alpine and Dinaridic units [9,10]. This zone transects the PSVMB in the area of the Zagreb-Zemplin Line (Fig. 2A).
Oligocene granitoids do not outcrop in the ZMTZ, but they were sampled from oil wells in Hungary [43]. By contrast, andesites and pyroclastics interlayered with Egerian-Eggenburgian (Chattian) clastic sediments are very common. The geological age of the volcanics is supported by concordant K-Ar ages ranging mainly between 26 and 20 Ma (Table 1).
3.3. The Sava segment
The northwestern part of the SVZ is formed by the Sava segment of the North Dinarides (Fig. 2B). This area experienced strong Pliocene (5-4 Ma) shortening, which gave rise to northward thrusting of the North Dinaridic fragments onto the Tisia and the Pannonian Basin, respectively [44-46].
Early and Middle Eocene syncollisional granitoids (Srisochron ages of 55-48.7 Ma; Table 1) crop out only in the western part of the Sava segment and in the basement of the Pannonian Basin [47]. Further eastward in the Mts. Boranja and Cer, Oligocene granitoids (K-Ar ages of 33.7-22 Ma) also crop out (Fig. 2B and Table 1).
In the Sava segment, Early Oligocene shoshonites with subordinate high-K calc-alkaline volcanics (30-28.5 Ma) occur in the Maglaj and Srebrenica areas. Shoshonites (36-29 Ma) in the adjacent north-verging Mt. Fruska Gora klippe (located within the South Pannonian Basin, Fig. 2B), and also found in the surrounding boreholes, belong to the same age group. Moreover, Egerian-Eggenburgian (Chattian) volcanics (K-Ar ages of 25.9-24 Ma) also occur in the Sava segment, as evidenced by boreholes (Table 1).
3.4. The Vardar segment
The north-northwest-south-southeast-stretching Vardar segment of the SVZ extends from Belgrade, southward through Macedonia to Thessaloniki (Fig. 2C). The suture line is defined by the contact between the SVZ and the western margin of the Serbo-Macedonian Massif, representing the eastern margin of Rhodope [35]. This is a dextral
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Tab
le 1
Rad
iom
etri
c ag
es a
nd b
asic
pet
rolo
gica
l si
gnat
ures
of
Lat
e P
aleo
gene
plu
toni
c an
d vo
lcan
ic r
ocks
fro
m t
he P
eria
dria
tic-
Sav
a-V
arda
r m
agm
atic
bel
t
Loc
ality
A
ge (
Ma)
P
etro
grap
hy [
79]
Pet
roch
emic
al a
ffin
ity L
116]
Hrv
atsk
o Z
agor
je-S
love
nia,
ZM
TZ
22
.8-1
9.7
Oil
wel
ls,
Sout
h P
anno
nian
Bas
in,
SS
25.9
-24
Bor
ac,
Sou
thea
st P
anno
nian
Bas
in,
SS
22.8
-22.
7
Mt.
Gol
ija,
VS
Mt.
Zel
jin,
VS
Kav
ala,
RH
Ada
mel
lo S
outh
, PS
A
dam
ello
Nor
th,
PS
Ber
gell
Poh
mje
-Kar
avan
ke
Bie
lla,
PS
Mt.
Bor
anja
, SS
M
t. C
er,
SS
M
t. B
ukul
ja, V
S M
t. K
opao
nik,
VS
Vro
ndou
-Xan
thi,
RH
Tri
s-V
ryse
s, R
H
Lep
toka
ria-
Kir
ki,
RH
Ses
ia-L
anzo
, S
L
Rha
etia
n A
lps
Mt.
Fru
ska
Gor
a, S
S O
il w
ells
, S
outh
Pan
noni
an B
asin
, SS
S
rebr
enic
a-M
agla
j, S
S R
ogoz
na,
VS
Mt.
Kop
aoni
k-Ib
ar,
VS
Zle
tovo
-Kra
tovo
, V
S B
ucim
-Bor
ov D
ol,
VS
Kri
va P
alan
ka,
VS
Doj
ran
Lak
e, V
S So
uth
Rho
dope
, V
S A
lexa
ndro
upol
is,
RH
Cen
tral
Rho
dope
, R
H
Mt.
Mot
ajic
a, S
S
Mt.
Pro
sara
, S
S
Oil
wel
ls,
SS
S
itho
nia,
VS
20--
17.5
24
--17
22
-21
a
43-3
8 b
35-3
1 b
32-3
0 30
--28
31
-29
33.7
-29.
6 33
-22
27
35.3
-29.
8 34
--30
28
.8-2
6.3
b
31.9
-31.
4
35-3
2
33-2
9
32.4
--30
.8
36-3
1.6
31.7
30
.4--
28.5
33
-27
32-2
9 32
-26
27.5
-24.
7 25
.3
33
34--
30
33-2
7
35-2
9
48.7
b
48.7
b
55 b
50.1
--44
.6
b; 5
0.0
a
Ege
rian
-Egg
enbu
rgia
n (C
hatt
ian)
pos
t-sy
ncol
lisi
onal
cal
c-al
kali
ne v
olca
nics
B
asal
t, ba
salt
ic a
ndes
ite,
ande
site
, su
bord
inat
e da
cite
L
ow-K
tho
leii
te-b
asal
t-an
desi
te-d
acit
e D
acite
, an
desi
te,
basa
ltic
tra
chya
ndes
ite
Bas
alti
c an
desi
te-a
ndes
ite-
-dac
ite
Tra
chya
ndes
ite
and
lam
prop
hyre
A
bsar
okit
e-sh
osho
nite
E
geri
an-E
ggen
burg
ian
(Cha
ttia
n) p
ost-
sync
olli
sion
al g
rani
toid
s G
rano
dior
ite,
qua
rtz
mon
zoni
te
And
esit
e-hi
gh-K
dac
ite
Qua
rtz
dior
ite,
ton
alit
e, g
rano
dior
ite
And
esit
e-hi
gh-K
dac
ite
Gra
nodi
orit
e, t
onal
ite,
dior
ite
And
esit
e-hi
gh-K
dac
ite-
rhyo
lite
Ear
ly O
ligo
cene
pos
t-sy
ncol
lisi
onal
gra
nito
ids
Ton
alite
, gra
nodi
orit
e, r
are
dior
ite
Bas
alt-
basa
ltic
and
esit
e-an
desi
te-d
acit
e G
abbr
o, c
umul
itic
hom
blen
dite
T
onal
ite,
gran
odio
rite
, ga
bbro
, cu
mul
itic
hom
blen
dite
T
onal
ite,
gran
odio
rite
, di
orit
e, g
abbr
o G
rani
te,
mon
zoni
te,
syen
ite
Gra
nodi
orit
e, q
uart
z m
onzo
nite
, su
bord
inat
e to
nali
te
Qua
rtz
mon
zoni
te,
gran
odio
rite
, le
ucoc
rati
c gr
anit
e M
onzo
nite
, gr
anod
iori
te,
gran
ite
Qua
rtz
dior
ite,
qua
rtz
mon
zoni
te,
gran
odio
rite
G
abbr
o, m
onzo
nite
± q
uart
z, g
rano
dior
ite,
gra
nite
, qu
artz
sy
enit
e Q
uart
z ga
bbro
, qu
artz
dio
rite
, qu
artz
mon
zoga
bbro
, to
nali
te,
gran
odio
rite
Q
uart
z ga
bbro
, qu
artz
dio
rite
, qu
artz
mon
zoga
bbro
, to
nali
te,
gran
odio
rite
Bas
alt-
basa
ltic
and
esit
e-an
desi
te-h
igh-
K a
ndes
ite-
high
-K d
acit
e H
igh-
K b
asal
tic
ande
site
-hig
h-K
and
esit
e-ba
naki
te
Abs
arok
ite-
shos
honi
te-b
anak
ite
Dac
ite-
high
-K d
acit
e B
anak
ite-
high
-K d
acit
e B
anak
ite-
high
-K d
acit
e H
igh-
K a
ndes
ite-
high
-K d
acit
e B
asal
tic
ande
site
-and
esit
eda
cite
-abs
arok
ite-
bana
kite
-sho
shon
ite-
rhyo
lite
B
asal
t-ba
salt
ic a
ndes
ite-
high
-K a
ndes
ite-
high
-K d
acit
e
Bas
alt-
basa
ltic
and
esit
e-hi
gh-K
and
esit
e-hi
gh-K
dac
ite
Ear
ly O
ligo
cene
pos
t-sy
ncol
lisi
onal
sho
shon
ites
an
d h
igh-
K v
olca
nics
B
asal
t, ba
salt
ic a
ndes
ite,
ande
site
, tr
achy
ande
site
, la
mpr
ophy
re
Bas
alt-
basa
ltic
and
esit
e-hi
gh-K
bas
alti
c an
desi
te-a
ndes
ite-
high
-K
ande
site
-abs
arok
ite-
bana
kite
-sho
shon
ite
Bas
alt,
basa
ltic
and
esite
, an
desi
te
Tra
chya
ndes
ite
Tra
chya
ndes
ite
Tra
chya
ndes
ite,
tra
chyd
acit
e, a
ndes
ite
Dac
ite,
trac
hyan
desi
te
And
esit
e, t
rach
ydac
ite
And
esit
e, t
rach
yte,
dac
ite,
igni
mbr
ite
Tra
chya
ndes
ite,
tra
chyd
acit
e, t
rach
yte,
and
esit
e T
rach
ybas
alt,
trac
hyan
desi
te,
trac
hyte
, tr
achy
daci
te,
rhyo
lite,
an
desi
te,
daci
te
Tra
chyt
e, r
hyol
ite
And
esite
, tr
achy
ande
site
, rh
yoli
te
Bas
alt,
basa
ltic
and
esit
e, a
ndes
ite,
daci
te,
rhyo
lite
Bas
alt,
basa
ltic
and
esite
, an
desi
te,
trac
hyan
desi
te,
trac
hyte
Bas
alti
c an
desi
te-a
ndes
ite-
high
-K a
ndes
ite
Ban
akit
e-sh
osho
nite
B
anak
ite
Hig
h-K
dac
ite-
bana
kite
B
anak
ite-
shos
honi
te
Hig
h-K
bas
alti
c an
desi
te-h
igh-
K a
ndes
ite-
high
-K d
acit
e H
igh-
K a
ndes
ite-
bana
kite
-rhy
olit
e H
igh-
K d
acit
e-ba
naki
te-K
-enr
iche
d rh
yolit
e H
igh-
K d
acit
e-ba
naki
te-K
-enr
iche
d rh
yolit
e
Ban
akit
e-sh
osho
nite
-rhy
olit
e H
igh-
K a
ndes
ite-
high
-K d
acit
e-sh
osho
nite
-rhy
olit
e B
asal
tic
ande
site
-hig
h-K
bas
alti
c an
desi
te-a
ndes
ite-
high
-K
ande
site
-ban
akit
e-da
cite
-hig
h-K
dac
ite-
high
-K r
hyol
ite
Hig
h-K
bas
alti
c an
desi
te-h
igh-
K a
ndes
ite-
high
-K d
acit
e-rh
yoli
te;
Abs
arok
ite-
bana
kite
-sho
shon
ite
Eoc
ene
sync
olli
sion
al g
rani
toid
s G
rano
dior
ite,
mon
zogr
anit
e, q
uart
z di
orit
e, m
onzo
dior
ite
Hig
h-K
dac
ite-
K-e
nric
hed
rhyo
lite
-ban
akit
e A
lkal
i fe
ldsp
ar g
rani
te,
alka
li fe
ldsp
ar s
yeni
te,
rare
dio
rite
H
igh-
K a
ndes
ite-
rhyo
lite
M
onzo
gran
ite,
qua
rtz
dior
ite
Hig
h-K
and
esit
e-hi
gh-K
dac
ite
Gra
nodi
orit
e, t
onal
ite,
gra
nite
, le
ucog
rani
te
Hig
h-K
dac
ite-
high
-K r
hyol
ite
Ela
tia,
RH
50
.0--
47.8
G
rano
dior
ite,
ton
alit
e, q
uart
z di
orit
e, m
onzo
dior
ite
Hig
h-K
and
esit
e-hi
gh-K
dac
ite-
rhyo
lite
PS,
Per
iadr
iati
c se
gmen
t; R
H,
Rho
dope
; SL
, S
esia
-Lan
zo;
SS,
Sav
a se
gmen
t; V
S, V
arda
r se
gmen
t; Z
MT
Z,
Zag
orje
-Mid
-Tra
nsda
nubi
an Z
one.
a
Ar/
Ar.
b R
b/Sr
. A
ll o
ther
s ar
e K
1 Ar
min
eral
and
who
le r
ock
ages
.
"' :p:
Ref
eren
ces
Sim
unic
and
Pam
ic [
110]
P
amic
and
Pec
skay
[ 11
3]
Cve
tkov
ic e
t a!
. [5
9]
Del
aloy
e et
a!.
L 118
] K
aram
ata
eta!
. [3
] D
inte
r et
a!.
[119
];
Chr
isto
fide
s et
a!.
[58]
Del
Mor
o et
a!.
[66]
vo
n B
lanc
kenb
urg
et a
!. [2
] vo
n B
lanc
kenb
urg
et a
!. [ 6
8]
Pam
ic a
nd P
alin
kaS
[70]
B
igio
gerr
o et
a!.
[69]
~
Del
aloy
e et
a!.
[118
] K
neze
vic
eta!
. [6
1]
2' K
aram
ata
et a
!. [ 1
20]
'" c:;~ S
olda
tos
eta!
. [5
6]
~ "'
Kyr
iako
poul
os e
ta!.
[54
] ,....
.....
. D
el M
oro
et a
!. [5
0]
Cl "' 0
Del
Mor
o et
a!.
[50]
; ~
Mav
roud
chie
v et
a!.
[55]
"' '"
Dal
Pia
z et
a!.
[I]
g· ;,. "
Dal
Pia
z at
a!.
[40]
e;
Kne
zevi
c et
a!.
[77]
.....
..., P
amic
[78
] -;::
:, P
amic
eta
!. [
63]
c C
vetk
ovic
et
a!.
[ 64]
~
Kar
amat
a et
a!.
[65]
"' c :E v.
, K
aram
ata
eta!
. [3
] .....
Ele
fthe
riad
is a
nd L
ippo
lt [
53]
Ele
fthe
riad
is e
t a!
. [ 4
]
Ele
fthe
riad
is a
nd L
ippo
lt [
53];
E
left
heri
adis
[52
]
Lan
pher
e an
d P
amic
[47
] P
amic
and
Lan
pher
e [8
3]
Pam
ic a
nd L
anph
ere
[83]
D
'Am
ico
et a
!. [4
8];
Chr
isto
fide
s et
a!.
[ 49]
; D
e W
et e
ta!.
[51
] S
olda
tos
eta!
. [5
7]
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1. Pamic et al. I Geodinamica Acta 15 (2002) 209-231 215
Fig. 3. (A) Variation diagram of CaO vs Fe0,0 , for !-type and S-type granites [114] for collisional granitoids (large crosses: Motajica-Prosara; small crosses: Sithonia) and post-syncollisional granitoids from the Periadriatic segment (open circles), Sava-Vardar Zone (full circles) and Kavala pluton (x). (B) Q-A-P triangle showing compositional differences of the Eocene synkinematic granitoids. Analytical data were used from [49,83,115].
strike-slip fault zone that links up northward with the Sava fault system.
In the northern part of the Vardar segment, Oligocene and Egerian-Eggenburgian (Chattian) granitoids occur. In the southeasternmost parts of the Vardar segment, the large Sithonia Middle Eocene synkinematic pluton (350 km2)
crops out in the Chalkidiki area of Greece. In the Rhodopian framework, the Eocene Elatia and Oligocene Vrondou-Xanthi granitoids and Egerian-Eggenburgian (Chattian) Kavala granodiorites occur. In the northeasterly deflected extension of the SVZ in Thrace, the Oligocene Leptokaria-Kirki-Kassitera and Tris-Vryses-Halasmata granitoid bodies crop out (Figs. 1B and 2C). The age of all these granitoids is constrained by numerous radiometric data (Table 1) [48-58].
In the southeasternmost Pannonian Basin, Egerian-Eggenburgian (Chattian) shoshonites and lamprophyres occur [59]. However, the largest masses of Oligocene shoshonite and high-K calc-alkaline volcanics of the Dinarides-Hellenides, with surface areas of up to 1200 km2
(Zletovo-Kratovo, Fig. 2C), are located further southeastward along the Vardar segment [3,60]. These volcanics, together with associated penecontemporaneous granitoids, are the most widespread Tertiary igneous rocks of the Dinaridic-Hellenidic SVZ [3,4,52,53,61].
Some volcanic bodies of this age group also occur within the adjacent South Pannonian Basin, the Serbo-Macedonian and Rhodope Massifs, respectively, the northernmost area of the allochthonous Golija Zone [62] and in the adjacent Dinaride Ophiolite Zone [63]. Their ages range mainly between 32 and 29 Ma and between 33 and 27 Ma, respectively (Table 1) [4,52,53,64,65].
4. Petrological and geochemical data on Paleogene magmatic associations
4.1. Middle Eocene syncollisional granite bodies
The largest and the most differentiated Elatia and Sithonia plutons are largely composed of granite, granodiorite and tonalite with quartz diorite and monzodiorite. Some smaller plutons and dykes are composed chiefly of monzogranite and granodiorite with quite subordinate quartz monzodiorite and quartz diorite or of alkali-feldspar granite and alkali-feldspar syenite with quite subordinate diorite. The granitoid plutons from the first group belong to the I-type family, and those from the second group to the S family and, to a lesser extent, to their transitional zone (Fig. 3A). Differences in petrography of the Eocene synkinematic granitoids are presented on the Q-A-P triangle (Fig. 3B) and their major element variation intervals in Table 2. Petrochemically, granitoids from the first group are characterized by a high-K andesite to high-K dacite to high-K rhyolite differentiation trend. Those from the second group display a high-K dacite-high-K rhyolite-banakite and high-K andesite-rhyolite differentiation trend (Fig. 4A).
Eocene syncollisional granitoids are not yet known in the PL area.
4.2. Oligocene post-syncollisional granitoids
The Oligocene post-syncollisional granitoids are much more abundant than the syncollisional Eocene granitoids, especially in the PL area. The Periadriatic plutons are mainly composed of tonalite, accompanied by granodiorite
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216 J. Pamic et al. I Geodinamica Acta 15 (2002) 209-231
Table 2 Major ( wt.%) and trace element (ppm) variation intervals and characteristic element ratios for the Eocene syncollisional granitoids and Egerian-Eggenburgian (Chattian) calc-alkaline volcanic and plutonic rocks
Eocene syncollisional granitoids Egerian-Eggenburgian (Chattian) calc-alkaline volcanics
MP MM ST EPL SPB KV
Si02 55.67-74.23 64.67-73.94 59.00-74.97 51.00-60.20 52.57-70.66 61.53-75.56 Ti02 0.10--0.60 0.05-{).45 0.09-{).70 0.65-D.75 0.36-1.29 0.07-D.59 Al20 3 11.78-14.91 12.63-17.48 14.61-17.51 16.41-21.99 15.61-17.15 13.68-16.66 Fe20 3 1.75-6.62 0.57-3.65 0.62-5.81 1.89-5.50 0.98-1.97 0.19-1.54 FeO 0.15-1.57 0.09-2.08 0.62-5.81 1.51-4.92 1.31-7.43 0.41-3.62 MnO 0.01-D.13 0.01-D.14 0.05-D.13 0.06-D.l4 0.02-D.lS 0.05-{).34 MgO 0.20-1.01 0.20-2.29 0.17-3.44 1.24-4.65 1.29-6.46 0.14-3.30 CaO 0.28-1.40 0.40-2.66 1.21-5.30 4.27-11.71 1.48-8.73 1.56-5.29 Na20 3.35-4.85 1.92-4.65 3.49-5.35 2.58-5.49 2.99-4.10 3.60--5.20 K20 2.50-5.75 1.98-5.92 1.99-3.2 0.31-2.67 1.07-3.66 1.99-4.24
P20s 0.02-0.21 0.01-D.19 0.03-D.59 0.09-{).20 0.14-D.34 0.03-D.28 LOI 0.60--2.36 0.61-1.62 0.28-2.05 2.01-4.44 1.03-2.97 0.06-1.68
Rb 79-243 87-133 13-81 25-31 67-211 Ba 56-156 210-900 467-697 130-510 223-626 234-1395 Sr 54-831 140-820 383-935 260-420 226-341 400-1464 Nb 5-19 10-15 6-17 5-13 4-12 8-27
Zr 153-456 50-200 81-160 60-198 81-135 90-420 y 7-65 10-15 13-26 16-39 8-36 37-56
v 10-20 10-30 6-96 40-200 8-36 6-138
Cr 1-29 2-50 5-41 18-68 39-70 6-42
Co 2-7 5-22 7-26 2-37
Ni 1-10 4-11 5-29 2-21 5-17 5-6
La 19.7-33.7 16-47 20.8-32.5 11-37 11.3-74.1
Ce 45.1-75.2 22-95 9.84-35.3 24-63 18.5-134.7
Nd 16.4-30.1 9.26-31.6 21-35 6.6-44.3
Sm 3.83-6.71 2.45-7.51 1.7-8.9
Eu 0.51-D.89 0.84-1.17 0.5-2.0
Gd 3.71-6.37 2.9-7.0 2.3-11.4
Tb 0.68-1.06 0.50-1.12
Tm 0.51-0.71 0.32-D.63
Yb 3.20-4.50 2.02-4.30 1-4 1.6-2.5
Lu 0.48-D.70 0.29-{).59 0.2-D.S
K/Rb 262-196 190-200 198-274 355-980 247-167
K/Ba 371-306 78-55 35-38 20-43 40-49 71-25
Rb/Sr 1.46-D.29 0.23-D.14 0.05-D.19 0.11-D.09 0.17-D.14
Zr/Rb 1.94-1.88 0.93-1.20 4.62-2.44 3.24-4.35 1.34-1.99
Ba/Sr 1.04-0.19 1.5-1.1 1.22-D.75 0.5-1.21 0.99-1.84 0.59-D.95
BalLa 2.84-4.63 29.19-14.83 6.25-15.69 20.27-16.92 20.71-18.83
La/Nb 3.94-1.77 2.67-2.76 4.16-2.50 2.75-3.08 1.41-2.74
La/Sm 5.14-5.02 8.49-4.33 6.65-8.33
La/Y 2.81-D.52 1.23-1.81 1.30-D.83 1.38-1.03 0.31-1.32
Sm/Nd 0.23-{).22 0.26-D.24 0.26-D.20
La/Yb 6.15-7.49 10.30-7.56 11.00-9.25 7.06-29.64
Zr/Y 21.8-7.02 5.0-13.3 6.23-6.15 3.75-5.08 10.13-3.75 2.43-7.50
Sr/Nd 3.29-27.7 28.08-13.29 10.76-9.74 60.61-33.05
Ce/Yb 14.1-16.7 4.87-8.21 24.0-15.75 11.56-53.88
Ce/Rb 0.57-D.31 0.25-{).71 0.76-D.44 0.96-2.03 0.28-{).64
Sr/Zr 0.35-1.82 2.8-4.1 4.73-5.84 4.33-2.12 2.79-2.53 4.44-3.49
Rb/Zr 0.52-{).53 1.07-{).83 0.22-{).41 0.31-D.23 0.74-D.SO
EPL, volcanics from the East Periadriatic area; KV, Kavala; MM, Mt. Motajica; MP, Mt. Prosara; SPB, South Pannonian Basin; ST, Sithonia. Data taken from: Varicak [122]; Pamic and Prohic [115]; Christofides eta!. [49,58,121]; D'Amico eta!. [48]; Pamic and Lanphere [83]; Simunic and
Pamic [110]; Altherr et a!. [84]; Neiva et a!. [80]; Parnic [78].
and rare diorite (with or without quartz); gabbro and cumulitic hornblendite are subordinate [2,66-68]. The Periadriatic granitoid plutons are associated with many acidic to mafic dykes [1,42]. Only the Biella and Novate plutonic bodies are different and are mainly composed of granite,
monzonite and syenite [69]. Their major element variation intervals are presented in Table 3.
Petrochemically, the largest plutons are characterized by the most complete differentiation trends, as shown by low-K tholeiite to basalt to basaltic andesite to medium-K andesite
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J. Pamic et al. I Geodinamica Acta 15 (2002) 209-231 217
_--._ ::!( 0 3.0
~ '-"
0 <'l ~ 2.0
52 56 63 70
Si02 (wt. %)
4.0
0 N
~ 2.0
1.0
52 56 63 70
Si02 (wt. %)
Fig. 4. Simplified linear variations of K20 vs Si02 in the diagram modified after Peccerillo and Taylor [116] for: (A) plutonic rocks: A, Adamello; B, Bergell; BI, Biella; BO, Boranja; CB, Cer-Bukulja; K, Kopaonik-Zeljin; KA, Kavala; M, Motajica; P, Prosara; PK, Pohorje-Karavanke; R, Rensen; S, Sithonia; T, Thrace; (B) volcanic rocks: BB, Bucim-Borov Dol; CR, Central Rhodope; EE, Egerian-Eggenburgian (Chattian); ER, East Rhodope; FG, Fruska Gora; KI, Kopaonik-Ibar; KZ, Kratovo-Zletovo; R, Rogozna; RA, Rhaetian Alps; S, Srebrenica; SL, Sesia-Lanzo. Petrochemical: A, low-K tholeiite; B, calc-alkaline volcanics; C, high-K calc-alkaline volcanics; D, shoshonites.
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218 J. Pamic et al. I Geodinamica Acta 15 (2002) 209-231
Table 3 Major (wt.%) and trace element (ppm) variation intervals for the representative Oligocene plutons from the PSVMB
PK BG AD
Si02 52.40-68.10 47.95-66.30 49.32-67.87 Ti02 0.35-0.83 0.37-1.04 0.52-1.22 Al20 3 6.20-18.00 7.57-18.40 12.15-20.35 Fe20 3 0.90--3.05 0.66-7.33 0.46-3.60 FeO 2.08-4.63 2.15-7.05 2.10-4.75 MnO 0.08-0.25 0.04-0.15 0.07-D.22 MgO 2.99-15.10 1.68-13.26 2.11-10.57 CaO 3.16-17.30 3.09-17.66 4.03-15.86 Na20 1.17-4.26 0.95-3.37 0.89-4.53 K20 0.44-2.38 0.20-4.41 0.46-2.61 PzOs 0.05-0.31 0.06-D.26 0.08-D.25 LOI 0.23-3.19 0.71-3.46 0.43-1.34
Rb 16-90 5-199 6-143 Ba 150-1120 168-852 121-563 Sr 240-920 248-363 213-582 Hf 1.3-5.4 1.3-4.8 Nb 4-16 Zr 54-223 65-236 74-134 Ta 0.26-1.57 Th 0.50--25.0 1.0-18.8 u 0.54-4.28 0.3-11.85 Pb 13-39 Ga 10-21 10-16 v 44-180 70-316 171-296 Cr 60--1800 6-348 10-1068 Co 7-37 3-47 6-24 Ni 4-180 3-68 6-75 Cu 9-14 8-23 7-35 Zn 37-94 39-78 34-74
Sc 6-83 11-98 La 5.87-58.88 2.8-32.9 8.7-39.1 Ce 13.9-111.0 6.4-63.3 15.68-74.7 Nd 14.2-39.8 6.27-27.83 8.86-29.0 Sm 3.4-6.55 2.08-5.61 2.23-5.22 Eu 0.89-1.41 0.50-1.3 0.80-1.45 Gd 3.05-5.60 Td 0.50-D.79 0.30-D.9 0.41-{).78 Dy Ho 0.95 Tm 0.36 Yb 1.26-2.99 1.3-2.9 1.36-2.90 Lu 0.17-{).34 0.2-D.S 0.21-D.43 y 14-25 4-23
RS BI
51.51-68.28 51.28-67.03 0.26-D.88 0.31-1.18
16.69-19.79 10.74-17.51 0.38-2.23 0.65-7.37 1.86-6.00 0.00-6.97 0.06-D.l6 0.05-D.25 0.99-4.33 0.90-6.40 4.49-9.17 2.61-7.83 2.26-3.48 1.78-3.90 1.01-3.28 2.80-6.10 O.Ol-D.24 0.16-1.64 0.81-1.92 0.44-1.59
38-90 63-473 171-568 1048-3406 253-476 433-1339
1.9-3.2 19-44
74-128 221-509 0.44-1.50 9-85 1.8-8.5 57-90
32-46
6.0-43.0 2.7-21.1
3.2-26.0 11.0-33.0 50.1-69.92 18.0--57.0 91.83-134.85 7.3-20.0 32.57-66.21 1.7-4.5 5.80-12.67 0.5-1.3 1.20-3.03
3.77-9.79 0.19-D.68
2.43-6.01
0.3-2.4 1.18-2.66 0.10-D.40 0.19-D.38
15-67 20 a
CB
59.66-67.16 0.30--0.58
15.96-17.68 0.90--3.62 1.67-3.24 0.03-0.13 1.31-2.65 3.04-4.73 1.91-3.96 2.08-4.97 0.14-D.25 O.o?-1.18
70 a 641 a 562 a
9a 187 a
60 a 15 a 35 a 48 a
5 a 13a 20 a
14 a 2.7 a
2a
9.9-45.1
TH
50.71-68.91 0.38-1.01
13.23-23.02 1.25-3.22 1.40-6.52 0.06-0.15 1.51-9.17 3.71-12.16 1.67-3.45 1.02-3.40 0.10-D.39 0.87-2.67
27-211 187-733 284-574
8-29 76-150
4.6-29.0
68-359 8-80
4-32 11-145 21-114
8.99-32.1 10.22-71.9 21.63-33.16
4.39-6.33 . 1.1-1.73
0.57-D.87
2.01-2.97 0.29-D.47
Data taken from Pamic and Palinkas [70] for Pohorje-Karavanke (PK), von Blanckenburg et a!. [68] for the Bergell pluton (BG), Kagami et al. [67] for the Southern Adamello (AD), Bellieni eta!. [123] for the Rensen pluton (RS), Bigiogerro eta!. [69] for the Biella pluton (Bl), Karamata eta!. [120] and Knezevic eta!. [61] for the Cer and Boranja plutons (CB) and Christofides et al. [58] and Neiva eta!. [80] for Tris-Vryses and Leptokaria-Kirki, and Thrace (TH) in Greece.
a Average values (n = 9).
to high-K andesite and to high-K dacite trends [67,70]. In the smaller plutons, this evolutionary trend is not complete, due to the absence of the most mafic rocks [68], with the exception of the Biella pluton displaying calc-alkaline to shoshonite affinities [69] (Fig. 4A).
Oligocene plutons from the northwestern SVZ are largely composed of quartz monzonite, quartz diorite, granodiorite and leucocratic granite with minor tonalite [71-74]. In some plutons, mafic, locally foliated xenoliths are found [65]. These correlate to foliated lenses and irregular smaller bodies of gabbro and diorite found within some PL plutons [70]. The highly differentiated plutons from Thrace in North
Greece are composed of gabbro, quartz diorite with prominent cumulate features, tonalite and granodiorite [58]. Their major element variation intervals are given in Table 3.
The Thrace plutons are similar to the Pohorje-Karavanke plutons in being characterized by the most complete differentiation trend, ranging from basalt to basaltic andesite-andesite, high-K andesite and dacite. Other plutons display an andesite to high-K andesite to high-K dacite trend or a steep dacite to high-K dacite differentiation trend. Some of them display two differentiation trends, firstly from dacite to rhyolite and secondly from rhyolite to banakite (Fig. 4A).
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0 ('I
~ + 0 N C\$
z
Si02 (wt. o/o) Fig. 5. Total alkali-silica diagram for Early Oligocene shoshonites and high-K andesites and dacites from the Sava-Vardar Zone: Srebrenica and Maglaj (•), Fruska Gora (0), Rogozna (•). Kopaonik-Ibar (.~). Kratovo-Zietovo (.A.), Bucim-Borov Dol(+), Kriva Palanka (X), Rhodope (*), Canavese Line(*). East Rhodope ($), Central Rhodope (§) and Egerian-Eggenburgian (Chattian) calc-alkaline volcanics (114). Fields: 1, trachybasalt; 2, basaltic trachyandesite; 3, trachyandesite; 4, trachyte and trachydacite; 5, rhyolite; 6, dacite; 7, andesite; 8, basaltic andesite; 9, basalt [79].
Consequently, despite the varying differentiation trends, most of the Oligocene post-syncollisional plutons that were emplaced along the PSVMB are basically characterized by a typical gabbro-diorite-tonalite-granodiorite-granite calcalkaline affinity, but some of them show distinct shoshonite trends. Most of the Oligocene granitoids, both from the PL area and from SVZ, plot together in the field of I-type granite (Fig. 3A).
4.3. Oligocene shoshonite and high-K calc-alkaline volcanic rocks
Along the PSVMB, Oligocene shoshonite and high-K calc-alkaline volcanic rocks are most frequent within the Vardar segment, the eastern part of the Sava segment and the adjacent South PB [3,63,64,75-78]. In the PL segment, they are much more subordinate [39].
In most of the studied areas of the Dinarides and the Hellenides, Oligocene volcanics were determined as andesites, dacites, latites (or trachyandesites) and quartz latites (or sanidine dacites), always stressing calc-alkaline andesites and dacites. In general, these volcanics are thought to represent a typical andesite-dacite association with calcalkaline affinity that is associated with subordinate latites
[3,76]. A different conclusion is reached from plotting on a total alkali-silica (TAS) diagram (Fig. 5 and Table 4) about 130 major element analyses published on Oligocene volcanic rocks. About two-thirds of the points plot in the fields of trachyandesite, trachyte and trachydacite, rhyolite and, to a lesser extent, trachybasalt and basaltic trachyandesite fields. The remaining points fall in the fields of basalt, andesite, basic andesite and dacite; yet, in their uppermost parts, they are close to the boundaries toward the trachyandesite and trachydacite fields. Accordingly, the Oligocene volcanics are mainly shoshonites with subordinate andesites and dacites.
In the classification diagram for the volcanic rock series, the Oligocene volcanics display either high-K basaltic andesite-andesite-dacite-rhyolite and absarokite-banakiteshoshonite affinities or absarokite-shoshonite-banakiterhyolite affinities. However, most points are concentrated both in the banakite and in the high-K dacite fields. The only exceptions are dyke rocks from the PL area, which display a typical low-K basalt-andesite-dacite calc-alkaline trend (Fig. 4B). Consequently, the Oligocene volcanics of the PSVMB as a whole represent essentially differentiated shoshonite volcanic series with subordinate high-K calcalkaline rocks.
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220 J. Pamif et al. I Geodinamica Acta 15 (2002) 209-231
Table 4 Major (wt.%) and trace element (ppm) variation intervals for the representative samples of Oligocene shoshonite and high-K calc-alkaline volcanics with lamprophyres
SL RA FG RM CRh ERh
Si02 48.58-60.40 51.50-59.60 55.16-57.67 58.17-62.37 48.86-72.32 50.90-74.99 Ti02 0.42-1.61 0.47-{).85 0.54-1.15 0.39-{).69 0.22-1.23 0.22-1.39 Al20 3 8.87-17.60 17.30-18.50 15.97-17.48 13.74-18.31 12.92-17.49 13.11-17.47 Fe20 3 0.69-5.76 0.59-3.63 3.71-5.12 1.87-5.53 1.34-10.68 1.56-8.78 FeO 0.60-6.68 2.81-5.13 2.31-3.35 1.34-2.25 1.34-10.68 1.56-8.78 MnO 0.07-D.18 0.07-D.18 0.03-{).19 0.06-D.IO O.o3-D.18 0.01-0.20 MgO 10.90-1.88 1.97-4.19 1.70-2.31 0.93-3.86 0.54-6.06 0.50-4.70 CaO 2.26-8.82 4.12-8.82 5.20-8.05 3.55-5.92 1.26-12.38 1.65-9.10 Na20 0.85-3.64 2.69-4.09 3.03-4.11 1.53-2.74 1.86-4.30 2.22-3.81 K20 0.93-9.60 0.98-2.28 4.27-4.94 2.35-5.40 1.67-5.84 1.12-5.58 P20s 0.18-1.40 0.12-D.24 0.33-0.42 0.25-0.77 0.10-{).44 0.07-3.11 LOI 1.60-5.24 1.40-4.96 1.58-2.19 0.84-4.94 1.10-4.09
Rb 23-569 130-247 230-247 129-312 49-265 55-231 Ba 1154-1607 502-2030 538-1268 Sr 250-1242 719-988 564-666 703-978 433-703 Hf 2.38-21.60 Nb 8-54 10-17 13-14 6-18 Zr 106-854 128-180 214-223 149-201 138-280 101-212 Ta 0.40-2.71 Th 6.19-135 20-17 12-42 u 2.5-34.5 Pb Ga v 20-315 54-208 Cr 16-839 60-178 9-98 4-51 Co 11-60 Ni 10-460 13-21 3-28 7-27 Cu 4-91 3-36 Zn 59-123 y 20-50 20-26 35-37 21-42
Sc 8-31 La 21.9-164 25.65-50.28 10.00-60.00 Ce 32.1-152 54.72-88.61 41.70-85.50 Nd 22.6-227 27.10-44.81 Sm 4.5-11.1 5.37-7.65 3.50-8.90
Eu 1.11-7.65 1.50...Q.52 0.52-3.35
Gd 5.7-8.4 4.18-5.96
Tb 0.61-2.91 Tm 0.36-{).78 Yb 1.70-4.14 1.98-3.04 0.82-3.20
Lu 0.19-{).50 0.30-{).48
Data taken from DalPiaz et al. [I] and Venturelli eta!. [39] for the Sesia-Lanzo Zone (SL), DalPiaz eta!. [40] for the Rhaetian Alps (RA), Kndevic et al. [77] for Mt. Fruska Gora (FG), Karamata et al. [65] for Mt. Rogozna (RM), Eleftheriadis eta!. [52] for Central Rhodope (CRh) and Eleftheriadis et al. [4] for East Rhodope (ERh).
4.4. Egerian-Eggenburgian (Chattian) calc-alkaline volcanic rocks
The Egerian-Eggenburgian (Chattian) calc-alkaline volcanic rocks are less abundant than the Oligocene shoshonites. On a TAS diagram [79], the volcanics largely plot in the andesite and basaltic andesite fields and, to a lesser extent, in the fields of basalt and dacite (Fig. 5). Their major element variation intervals are given in Table 2. According to the K20/Si02 diagram, the rocks range from subordinate low-K basalt to more common low-K to medium-K andesite and medium-K dacite. Most basic rock samples, however, have an unequivocal tholeiitic affinity.
4.5. Egerian-Eggenburgian (Chattian) granitoids
Egerian-Eggenburgian (Chattian) granitoids are the most subordinate rocks among all the Late Paleogene igneous rocks within the PSVMB. The Kavala granitoids from the South Rhodopes are the only ones that were analyzed by modem analytical techniques [80]. This pluton is mainly composed of granodiorite, monzogranite, tonalite and dior ite, all with 1-type characteristics (Fig. 3A). According to the K20/Si02 diagram, the Kavala granitoids are characterized by a low-K andesite to high-K dacite to rhyolite differentiation trend (Fig. 4A). The Mt. Zeljin pluton (56 km2
) from
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the northern part of the Vardar segment is mainly composed of I-type quartz diorite, tonalite and granodiorite [81].
5. Trace element data
5.1. Eocene syncollisional granitoids
Eocene syncollisional granitoids are unevenly documented (Table 2). Some trace elements display a positive correlation, as exemplified by Cr and Ni ranging between 2 and 50 ppm and 4 and 29 ppm, respectively. However, there is no positive correlation for most trace elements, as exemplified by Zr, Y and Ba. In spite of that, there is a positive correlation in some characteristic element ratios, as, for example, K/Rb ranging from 190 to 262, typical of active margin granitoids [82], Rb/Sr (0.2-1.5), Zr/Rb (0.9-1.9), Ba!Sr (0.2-1.5), La/Nb (1.8-3.9), Ce/Rb (0.3-0.7) and Rb/Zr (0.5-1.1).
REE data for the Sithonia, Elatia and Prosara granitoids are characterized by uniform REE patterns with variable LREE/MREE, a moderate negative Eu anomaly and flat HREE patterns [57,83]. The steep La/Yb slope for these three plutons indicates strong fractionation of hornblende, weak Eu anomaly reflects minor fractionation of plagioclase, and the flat slope for HREE indicates either fractionation of clinopyroxene or less residual amphibole or garnet.
5.2. Oligocene post-syncollisional granitoids
Generally, the variations of incompatible trace elements and high-valency elements of the analyzed rocks are within the range of values of orogenic calc-alkaline volcanics of the same Si02 content [82] (Table 3). Most trace elements display a strong positive correlation between each other in several characteristic element ratios. This applies particularly to incompatible trace elements: K/Rb mainly between 220 and 315, which is typical of active margin granitoids, and also for some REE element ratios: La/Sm mainly 1.4-9.0, Sm/Nd = 0.2-0.3 and Ce/Yb = 4.9-37.1 (Table 5).
Compatible trace elements show great variations, ranging from 4 to 180 ppm for Ni, 3 to 37 ppm for Co, 6 to 1800 ppm for Cr and 44 to 359 ppm for V, indicating that fractional crystallization of mafic minerals played an important role. Some granitoids are rich in Th (up to 90 ppm) and U (up to 46 ppm), indicating a significant contribution from the continental crust, which is also supported by a high BalLa ratio reaching nearly 60.
The REE patterns of all analyzed samples show that LREE are enriched relative to HREE (Table 3). Most of the Periadriatic plutons display similar REE signatures, as indicated by: (1) steep LREE patterns, which are almost parallel to each other, indicating strong fractionation of hornblende; (2) a weak Eu anomaly, particularly in acidic rocks, due to weak fractionation of feldspar; and (3) a comparatively flat pattern for HREE, indicating either
fractionation of clinopyroxene or less residual amphibole or garnet [70]. The REE patterns for the Oligocene Rhodope plutons are very similar to that of the Periadriatic ones, but with slightly steeper LREE lines, indicating decreased hornblende fractionation [58].
5.3. Oligocene post-syncollisional shoshonite and high-K calc-alkaline volcanics
Generally, these rocks have enriched LILE concentrations and low HFSE with increased LREE, but with distinct variations from area to area, depending on the proportions of shoshonite and calc-alkaline volcanics (Tables 4 and 5)). They contain increased values of incompatible trace elements, which is a common characteristic of most modem subduction-related volcanics [82]. Much lower concentrations of compatible trace elements display variations, and most of the REE show equal variation intervals, except for La and Ce. Variations in Th (6-42 ppm) and U (2-35 ppm) indicate significant crustal contamination.
Characteristic element ratios show fairly uniform variations (Table 5), and the only discrepancy is in the K/Rb ratio, which mainly ranges between 144 and 283; this is typical for active margin andesites [40].
The REE patterns show that the LREE are enriched relative to HREE, probably due to the fractionation of hornblende. All analyzed samples have negative Eu anomalies, which are smallest in K-rich volcanics [4,52]. Excep tions are REE patterns for the Sesia-Lanzo volcanics, which display fractionated lines without Eu anomalies [1].
5.4. Egerian-Eggenburgian (Chattian) post-syncollisional granitoids and penecontemporaneous calc-alkaline volcanics
There is a fairly good correlation in compatible trace elements (Table 2). However, there is a negative correlation in incompatible trace elements between volcanics and granitoids. These differences suggest that crustal contamination of plutonic rocks was stronger than that of the volcanic ones.
Despite this discrepancy in trace element variations, there is a positive correlation between most characteristic element ratios, as exemplified by K/Rb mainly 167-274, which is typical for active margin andesites and many other ratios (Table 2).
The REE patterns show that the granitoids are strongly enriched in LILE with respect to HREE [80]. These patterns are subparallel with a distinct negative Eu anomaly. However, the volcanic equivalents display flat patterns, with an Eu anomaly that increases with increasing Si02 content [84].
In conclusion, trace element distribution and characteristic element ratios for both plutonic and volcanic associations along the PSVMB show that the Late Paleogene magmatic activity took place along the active continental
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~
Tab
le 5
C
hara
cter
isti
c el
emen
t ra
tios
for
the
Ear
ly O
ligo
cene
gra
nito
id a
ssoc
iati
on a
nd E
arly
Oli
goce
ne s
hosh
onit
e an
d hi
gh-K
cal
c-al
kali
ne a
ssoc
iati
on
Ear
ly O
ligo
cene
gra
nito
id a
ssoc
iati
on
Ear
ly O
ligo
cene
sho
shon
ite
and
calc
-alk
alin
e as
soci
atio
n
PK
B
G
AD
R
S
BI
CB
T
il
SL
R
A
FG
R
M
CR
h E
Rh
~
;:;o
K/R
b 22
8-21
9 33
2-18
4 63
6-15
1 22
0-21
9 36
9-10
7 24
7-58
9 31
3-13
4 3
36
-14
0
63
-77
15
4--1
66
151-
144
283-
183
169-
200
~-K
/Ba
24.3
-17.
6 9.
9-43
.0
31.6
-38.
5 49
.0-3
4.8
22.2
-14.
9 27
.0-6
4.4
45.3
-38.
5 16
.9-2
7.9
27.6
-23.
9 17
.3-3
6.5
"' ~ R
b/S
r 0.
07--
0.10
0.
02--
0.55
0.
03--
0.25
0.
15--
0.19
0.
15--
0.35
0.
12--
0.12
0.
10--
0.37
0.
09--
0.46
0.
18--
0.25
0.
41--
0.37
0.
18--
0.32
0.
11--
0.38
"'
Zr/
Rb
3.38
-2.4
8 13
.0-1
.19
12.3
3-0.
94
1.95
-1.4
2 3.
51-1
.08
2.67
-2.6
7 2.
81--
0.71
4.
61-1
.50
0.98
--0.
73
0.93
--0.
90
1.16
-{).
64
2.82
-1.0
6 1.
84--
0.92
,....
. .....
. B
a/S
r 0.
63-1
.22
0.68
-2.3
5 0.
57-0
.97
0.68
-1.1
9 2.
42-2
.54
1.14
-1.1
4 0.
66-1
.28
1.64
-1.6
4 1.
16-2
.89
C'l "'
Bal
La
25.5
5-19
.02
60.0
-25.
9 13
.9-1
4.4
15.5
5-17
.21
20.9
2-48
.71
20.8
0-22
.83
19.5
7-40
.37
53.8
0-21
.13
c !? L
a/N
b
1.47
-3.6
8 2.
64--
1.59
1.
12-1
.11
2.74
--3.
04
4.28
-2.7
9 "'
La/
Sm
1.
73-9
.00
1.35
-5.8
6 3.
90-7
.49
6.47
-7.3
3 8.
64-5
.52
2.05
-5.0
7 4.
87-1
4.77
4.
78--
6.57
2.
86--
6.74
;:!
La/
Th
11.7
4--2
.36
2.8-
1.75
6.
11-3
.88
0.88
-{).
78
1.95
-1.1
1 3.
54--
1.21
2.
14--
1.20
rr
La/
Y
0.42
-2.3
6 0.
70-1
.43
0.73
-{).
49
2.51
-3.5
0 1.
10-3
.28
1.22
-1.2
0 :..
" S
m/N
d 0.
24--
0.16
0.
33-0
.20
0.25
-0.1
8 0.
23-{
).23
0.
18--
0.19
0.
19--
0.19
0.
20-{
).19
0.
20-0
.05
0.20
--0.
17
iS
......
La/
Yb
4.66
-19.
69
2.15
-11.
34
6.40
-13.
48
36.6
7-13
.75
42.4
6-26
.29
4.47
-10.
81
12.8
8-39
.61
12.9
5-16
.54
12.2
0-18
.75
v.
Zr!
Y
3.86
-8.9
2 16
.25-
10.2
6 4.
93-1
.91
11.0
5-25
.45
18.8
9-4.
15
5.30
-17.
08
6.40
-6.9
2 6.
11--
6.03
6.
57--
6.67
-;::
;
Sr/
Nd
16.9
0-23
.12
39.5
5-13
.04
24.0
4-20
.07
34.6
6-23
.80
13.2
9-20
.22
40.1
4-40
.14
13.1
3-17
.31
11.0
6-5.
47
15.9
8-15
.69
~ C
e!Y
b 11
.03-
37.1
2 4.
92-2
1.83
11
.53-
25.7
6 60
.0-2
3.75
77
.82-
50.7
0 5.
08-2
4.31
18
.8-3
6.71
27
.64-
-29.
15
50.8
5-26
.72
N <::>
Ce/
Rb
0.87
-1.2
3 1.
28--
0.32
2.
61--
0.52
0.
47-{
).63
1.
46--
0.29
0.
38--
0.34
1.
40--
0.27
1.
12--
0.33
0.
76--
0.37
'f
S
r/Z
r 4.
44-4
.13
3.82
-1.5
4 2.
88-4
.34
3.42
-3.7
2 1.
96-2
.63
3.01
-3.0
1 3.
74-3
.83
2.36
-1.4
5 5.
62-5
.49
2.64
--2.
99
4.72
-4.8
7 3.
14--
2.51
N
"" ......
Rb/
Zr
0.30
-0.4
0 0.
08-0
.84
0.08
-1.0
7 0.
51-{
).70
0.
29--
0.93
0.
37-{
).37
0.
36-1
.41
0.22
-0.6
7 1.
02-1
.37
1.07
-1.1
1 0.
87-1
.55
0.36
--0.
95
0.54
--1.
09
PK
, P
ohm
je-K
arav
anke
; B
G,
Ber
gell
; A
D,
Ada
mel
lo;
RS
, R
ense
n; B
I, B
iell
a; C
B,
Cer
-Bor
anja
; T
il,
Thr
ace;
SL
, S
esia
-Lan
zo Z
one;
RA
, R
haet
ian
Alp
s; F
G,
Mt.
Fru
ska
Gor
a; R
M,
Mt.
Rog
ozna
; C
Rh,
C
entr
al R
hodo
pe;
ER
h, E
ast
Rho
dope
.
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J. Pamic et al. I Geodinamica Acta 15 (2002) 209-231 223
Fig. 6. Spider diagrams for Eocene syncollisional granitoids, Oligocene plutonic rocks, Oligocene shoshonite <:nd calc-alkaline volcanic rocks and Egerian-Eggenburgian (Chattian) calc-alkaline plutonic and volcanic rocks. (A) and (B) MORB normalized after Pearce [126]; (C) and (D) chondrite-normalized REE diagrams after Sun and McDonough [127].
margin, i.e., the syncollisional area. This is best exemplified by the BalLa (20-25), La/Nb (1.5-3.7) and La/Th (2.4-11.7) and some other ratios, which show positive correlation with the same ratios in volcanic rocks of recent back-arc basins [85,86]. This conclusion is also supported by MORE-normalized trace and chondrite-normalized REE spider diagrams (Fig. 6), which display patterns consistent with active continental margin setting [82].
6. Strontium, neodymium and oxygen isotopic compositions
The Sr, Nd and 0 isotope compositions of Late Paleogene magmatic associations are summarized in Table 6 and diagrammatically presented in Fig. 7A, B. These diagrams indicate that the three isotopic systems display common signatures and that all samples, regardless of differences in composition, geographic position and ages, plot in the lower part of the magmatic associations of island arc and active margin settings. This coherent field can be divided into two
main parts, characterized by: (1) 87Sr/86Sr = 0.7036-0.7080, 143Nd/144Nd = 0.512440-0.51284 and 6 180 = 5.9-7.2%o, indicating basalt partial melts derived from the continental mantle-lithosphere; and (2) 87Sr/86Sr = 0.7090-0.72131, 143Ndi144Nd = 0.512132--0.512408 and 6180 = 7.3-11.5%o, indicating crustal assimilation and melting. For the PL area, von Blanckenburg et al. [2] calculated that widespread (up to 70% ), partial melting of continental crust could be expected.
This combined continental mantle-lithosphere and crustal partial melting model fits with the results from the PL area [2,67,87,88]. The Periadriatic plutons show that the mantle-lithospheric source was heterogeneous in major and trace element contents and isotope compositions. Such a heterogeneous source can produce variable melt types, ranging from calc-alkaline compostttons with 87Sr/86Sr = 0.704-0.706 and 6 180 = 6-7%o to alkaline and K-rich compositions with 87Sr/86Sr = 0.708-0.720 and 6180 > 7.5%o. It is generally believed that mafic members of the granitoid associations are close in composition to primitive melts of the plutons [2].
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224 J. Pamic et al. I Geodinamica Acta 15 (2002) 209-231
A
B
""" "' ~ 0
:=": 00
..... ~ 0.5124
("') ~ .....
0.703
13
12
11
10
9
8
7
6
field
0.705
• + ...
•
South Sandwich ~ arc
D back-arc
-0.707 0.709 0.711
87srf86sr
+ II Adamello • ,/
• I !lpohorje-Karavanke
.702 .704 .706 .708 .710 .712 .714 .716 .718
B7srtB6sr
Fig. 7. (A) Plot of 143Nd/144Nd vs 87Sr/86Sr corrected for years marked in Table 6: Eocene syncollisional granitoids (.A.); Oligocene postsyncollisional granitoids (.); Egerian-Eggenburgian (Chattian) rocks ( + ). (B) Plot of 6180 vs 87Sr/86Sr corrected for years marked in Table 6; symbols are the same as in (A).
7. Discussion
During Eocene times (55-45 Ma) the Tethys Ocean was closed, oceanic subduction ceased, and the Dinarides-Hellenides formed by the collision of Tisia and Moesia with Apulia. Collision was accompanied by granitoid plutonism associated with medium-grade regional metamorphism,
which was controlled by transition from subduction to collision (Fig. 8C).
Eocene syncollisional plutons are related to fractional melts, derived from the continental mantle as indicated by lower 87Sr/86Sr ratios (Table 6). Based on correlation with recent convergent margins [82], and according to the above-presented geophysical, geological, petrological and geochemical data for the Dinarides and the Hellenides, Eocene and subsequent Oligocene magmatic processes were controlled by: (1) the subducted Mesozoic-Early Paleogene Tethyan oceanic crust; (2) a metasomatized upper mantle wedge; and (3) the overlying Eurasian continental margin, i.e., Tisia and Moesia [70] .
In such a scenario, it is difficult to connect the southdipping subduction zone of the Central Alps with the northand northeast-dipping subduction in the Dinarides and Hellenides. In the present structural framework of the PL area, there are no outcrops of Alpine subduction- and collision-related magmatic associations [32]. However, SVZ lithologies occur in the westernmost parts of the Zagorje-Mid-Transdanubian Zone, namely the transitional Alpine-Dinaridic Zone [36], only a few tens of kilometers to the south of the PL. This ambiguous and unresolved problem of a possible Alps/Dinarides connection has been considered elsewhere [18]. According to current opinion [89], the Piedmont Ocean (Alpine Tethys) and the Vardar Ocean (Dinaridic-Hellenidic Tethys) were never connected; however, their sutures were finally brought close to each other in the final stages of Alpine convergence, thus giving an apparent continuity between the two features. However, it should be emphasized that Oligocene plutonic and volcanic associations form a continuous belt along the entire PSVMB, together with their generic roots, as indicated by seismic tomography data [25].
In the Dinarides-Hellenides, the Eocene syncollisional plutonism was followed, after a magmatic break of about 10 Ma, by Oligocene granitoid plutonism and shoshonite and calc-alkaline volcanism, products of which are correlative in geochronology and petrology to Periadriatic tonalites and associated volcanics. In conjunction with the indentation of Apulia, this magmatism was paralleled by strong dextral strike-slip faulting and transpressional processes. Convergence velocity of ca 5 em/year is probably based on the difference between the peak deformation of the Dinarides-Hellenides (ca 50 Ma) and onset of Oligocene magmatism (ca 40 Ma), with melt generation at depths of 80-100 km [90]. This fits with seismic tomography data on the Dinarides-Hellenides subduction zone, which is indeed characterized by convergence rates of the order of centimeters to a few meters per year [25].
Consequently, it is concluded that the main Eocene SV suture zone was transformed during the Oligocene into the dextral strike-slip fault system that controlled postsyncollisional magmatic activity. It could be assumed that by reaching this evolutionary stage, the SVZ reached the same geotectonic setting as the PL area.
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Tab
le 6
S
elec
ted
Sr
and
Nd
isot
ope
com
posi
tion
(pp
m)
and
1i18
0 (%
o) v
alue
s fo
r L
ate
Pal
eoge
ne m
agm
atic
ass
ocia
tion
s al
ong
the
PS
VM
B
Loc
ality
R
b Sr
R
b/Sr
87
Srf8
6 Sr
Age
Sm
N
d 14
7Sm
f144
Nd
143N
df14
4Nd
ENd
1)18
0 R
efer
ence
(M
a)
Eoc
ene
sync
olli
sion
al g
rani
toid
s M
t. M
otaj
ica
225-
399
56-8
06
0.8-
1.8
0.70
645-
D.7
2024
48
.7
9.8-
10.2
Lan
pher
e an
d Pa
mic
[47
] 0.
7060
c M
t. Pr
osar
a 29
-115
11
4-42
2 0.
44-0
.87
0.70
497-
D.7
0812
48
.7
7.3-
9.3
Lan
pher
e an
d Pa
mic
[47
] Si
thon
ia
68-1
43
276-
1026
0.
20-1
.50
0.70
590-
D.7
0781
50
.4
0.65
4-D
.066
1 0.
5125
02-D
.512
524
-1.5
/-2.
2 Ju
teau
eta
!. [
124]
; C
hris
tofi
des
eta!
. [4
9]
91-3
91
16-3
91
44-5
0.
7055
-D.7
071
c
Oli
goce
ne p
ost-
sync
olli
sion
al g
rani
toid
s R
e di
Cas
tello
29
-155
13
1-14
83
0.94
-3.4
0.
7057
1-D
.708
55
30
0.45
-5.3
1 2.
77-2
6.36
0.
0966
-D.1
317
0.51
2363
-D.5
1282
5 5.
9-9.
2 C
orte
cci
et
a!.
[87]
; D
el M
oro
et
a!.
[66]
; A
dam
ello
K
agam
i et
a!.
[67]
29
-143
62
-521
0.
16-1
.17
0.70
40-D
.707
0 B
erge
ll 4-
199
55-3
63
0.19
-D.8
3 0.
7055
30-D
. 711
078
30
1.44
-6.2
3 3.
94-2
7.83
0.
2215
-D.I
I66
0.5!
2841
-D.5
1230
0 2.
39-6
.60
6.7-
9.1
von
Bla
ncke
nbur
g et
a!.
[68]
~
Poh0
1je
21-9
0 44
0-92
3 0.
13-0
.28
0.70
6659
-D.7
0759
9 40
~ T
rave
rsel
la
128
731
0.50
75
0.71
088
30
8.87
6 49
.38
0.10
87
0.51
2189
-7
.82
6.7-
7.9
von
Bla
ncke
nbur
g et
a!.
[2]
Nov
ate
Ill
549
0.71
002
30
2.59
1 12
.96
0.12
08
0.51
2156
-8
.57
"' K
arav
anke
66
-77
140-
283
0.67
-D.9
3 0.
7079
2-D
.708
12
40
8.1-
8.3
Pam
ic a
nd P
alin
kas
[70]
~ "
0.70
7504
-D.7
0753
0 c
,.... '
Bie
lla
91-3
62
570-
1377
0.
41-1
.21
0.70
926-
D.7
1138
30
B
igio
gerr
o et
a!.
[ 69]
C
l 0.
7089
0-D
.711
17 c
"'
Cer
Bor
anja
12
5-24
1 84
-908
0.
42-D
.48
0.70
808-
D.7
213l
5.
7-9.
8 34
.4-5
3.0
0.94
72-1
.088
7 0.
5123
66-D
.512
373
-9/-
11
Kar
amat
a et
a!.
[ 120
] ~
122-
142
0.70
6637
-D.7
0864
-9
/20
;!
Eas
t Thr
ace
25-1
25
252-
574
O.IO
-D.2
2 0.
7056
9-D
.707
47
35
D'A
mic
o et
a!.
[48]
; D
el M
oro
eta!
. [5
0]
r;· "
Vro
ndou
18
-198
53
7-81
6 0.
08-1
.39
0.70
624-
D.7
0835
29
-32
0.97
8-D
.l057
0.
5123
81-D
.512
440
-3.9
/-5.
0 Ju
teau
eta
!. [
124]
; C
hris
tofi
des
eta!
. [5
8]
;:... "
0.33
-D.8
5 0.
7069
10-D
.706
916
iS
3-22
6 26
1-83
7 0.
05-0
.26
0.70
520-
D.7
079
29-3
2 0.
978-
D.I
057
0.51
2381
-0.5
1244
0 -3
.9/-
5.0
..... '"" -;::,
Oli
goce
ne p
ost-
sync
olli
sion
al s
hosh
onit
e an
d hi
gh-K
cal
c-al
kali
ne v
olca
nics
§
Ses
ia-L
anzo
0.
7072
-D.7
123
Ven
ture
lli e
t a!
. [3
9]
Lug
ano
30-2
32
27-3
81
0.28
0.
7082
8-D
.718
22
5.65
-9.0
8 26
.56-
46.9
1 0.
1175
-0.1
551
0.51
2250
-D.5
1231
4 St
ille
and
Bul
etti
[ 125
] ...,
Rha
etia
n A
lps
0.70
67-0
.710
6 31
D
al P
iaz
et a
l. [ 4
0]
~ Fr
uska
Gor
a 25
1-26
7 79
1-87
9 0.
32-0
.30
0. 7
0940
-D. 7
0944
34
8.
65-9
.01
41.2
-42.
1 O
.l294
8-D
.l300
6 0.
5124
08-D
.512
420
Kne
zevi
c et
a!.
[77]
"" .....
R
ogoz
na
141-
313
884-
978
0.42
-1.0
7 0.
7074
4-D
.707
51 C
AL
29
K
aram
ata
et a
!. [6
5]
0.70
847-
D.7
0850
SH
C
entr
al
6.4-
7.4
380-
1230
0.
05-D
.l9
0.70
852-
D.7
0929
35
-29
6.2-
11.5
E
left
heri
adis
[52
] R
hodo
pe
0.70
85 c
Ege
rian
-Egg
enbu
rgia
n (C
hatt
ian)
pos
t-sy
ncol
lisi
onal
gra
nito
ids
Kav
a! a
93-2
11
400-
748
0.23
-D.2
8 0.
7067
-D.7
093
22
10.5
-11.
4 N
eiva
eta
!. [
80];
Chr
isto
fide
s et
a!.
[58]
73
-199
30
6-70
6 0.
24-0
.28
0.70
674-
0.70
780
Ege
rian
-Egg
enbu
rgia
n (C
hatt
ian)
pos
t-sy
ncol
lisi
onal
cal
c-al
kali
ne v
olca
nics
So
uth
0.70
551-
D.7
0743
28
-18
26.4
-30.
4 0.
5123
64-D
.512
602
-D.7
-5.3
Pa
mic
[78
] Pa
nnon
ian
Bas
in
Bor
ac
171
0.48
2 0.
7057
78
22
10.8
63
0.
1035
1 0.
5126
16
-0.2
C
vetk
ovic
et
al.
[59]
c-ca
lcu
late
d v
alue
s; C
AL
-cal
c-al
kal
ine;
SH
-sh
osh
on
ite;
em
pty
cell
s-n
o p
ubli
shed
dat
a.
N ~
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226 J. Pamic et al. I Geodinamica Acta 15 (2002) 209-231
A. Upper Jurassic intra-oceanic subduction (138-135 Ma)
B. Middle Cretaceous- Early Paleogene subduction (130-50 Ma)
C. Eocene collision and Oligocene and Neogene transpression and extension (45-lOMa)
Fig. 8. Tentative models of the Alpine geodynamic evolution of the Dinarides, modified after Pamic et al. [117]. ADCP, Adriatic-Dinaridic carbonate platform; BAB, back-arc basin; DOZ, Dinaride Ophiolite Zone; iO, accretionary wedge (intra-oceanic obducted ophiolites); PCM, passive continental margin; SPB, South Pannonian Basin; SSF, strike-slip faults; SVZ, Sava-Vardar Zone.
There are several opinions on the mode of origin of the Periadriatic Oligocene magmatic associations, which could be also adopted for the entire PSVMB. These are as follows: (1) subduction zone melting at active continental margin [67,91]; mantle melting was stimulated by the introduction of fluids from subducted sediments; (2) back-arc extension melting and sea floor spreading [92,93]; (3) detachment of the lithospheric thermal boundary layer inducing syn- to post-syncollisional melting of the mantle-lithosphere and crust [94,95]; and (4) slab break-off inducing asthenosphere upwelling and melting of the mantle-lithosphere, with ascending melts being contaminated by the continental crust [42,90].
The Sr, Nd and 0 isotopic data for Oligocene magmatic formations of the PSVMB (Table 6) favor the slab-break-off model, implying that primary basaltic partial melts were derived from the continental mantle and its asthenosphere. This is indicated by low 87Sr/86Sr ratios (0.7040-0.706659), accompanied by low 0180 values (6%o and 7%o). The primitive basaltic melts were contaminated to various degrees by the continental crust, as indicated by higher 87Sr/86Sr ratios ranging from 0.7079 to 0.71108 and by increased values of 0180 ranging from 7%o to 9.2%o. However, some plutons crystallized mainly from crustal melts, as indicated by 87Sr/86Sr ratio ranging from 0.70808 to 0.72131 (Table 6).
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J. Pamic et al. I Geodinamica Acta 15 (2002) 209-231 227
Although differing from granitoid plutons mainly in major and trace element chemistry, the contemporaneous shoshonites with lamprophyres and subordinate calcalkaline volcanics show similar 87Sr/86Sr variations. However, the largest 87Sr/86Sr values of shoshonite and calcalkaline associations (0.71822) are not as large as those for Eocene (0.72024) and Oligocene (0.72131) granitoid associations; this can be explained by differences in their crystallization levels.
After a short break of about 5-6 Ma, the next magmatic activity followed, which produced the Egerian-Eggenburgian (Chattian) calc-alkaline volcanism with subordinate plutonic equivalents and sparse shoshonites with lamprophyres. The volcanic rocks are characterized by comparatively small 87Sr/86Sr variations: 0.70551-0.70743 and 0.7067-0.70780, indicating mantle-lithosphere primitive basalt melts with slight crustal contamination (Table 6).
The most common ultramafic xenoliths from Tertiary volcanics of the Pannonian Basin are spinel lherzolites, some of them containing interstitial metasomatic amphibole and phlogopite, and subordinate depleted harzburgite [96,97]. The spinel lherzolites with or without amphibole and phlogopite represent the most potential candidates for the source rocks that underwent partial melting. This conclusion is also supported by the Ce/K vs Ce diagram [98], demonstrating that mafic rocks from Late Paleogene magmatic associations of the SVZ plot close to curve A, which represents the accumulated fractional melts of a pargasitebearing lherzolite (Fig. 9A).
On the other hand, Ulmer [99] experimentally documented that the primary partial mafic melt of the Periadriatic Adamello batholith was in equilibrium with garnet peridotite. Therefore, it is accepted that garnet peridotite with some metasomatic amphibole is a source rock for the Periadriatic granitoid plutons [2]. Melting of amphibole was also suggested by the same Ce/K vs Ce diagram for the Mts. Pohorje-Karavanke plutons. However, different degrees of melting, also controlled by garnets as a residual phase, can be observed on REE-chondrite-normalized plots [70]. Consequently, it seems that the mantle-lithosphere along the PSVMB was heterogeneous in its major and trace elements and isotopic compositions. Source rocks for late Paleogene primitive melts were largely garnet peridotite with some phlogopite peridotite along the PL segment and spinel lherzolite with phlogopite lherzolite in the SVZ segment.
Major and trace element data (Tables 2-4) indicate that processes of fractional crystallization played the most important role in the petrogenesis of Late Paleogene magmatic associations along the PSVMB, as demonstrated by the MgO vs Fe0101 diagram (Fig. 9B). This diagram displays a slightly increasing trend, regardless of age differences of the magmatic associations and reflecting a normal differentiation trend with or without contamination, i.e., AFC processes [100]. The vertical trend could be accounted for by the precipitation of mafic minerals at a pertinent degree of fractional crystallization (see bold arrows 1 and 2 in Figs.
A
B
Fig. 9. (A) Plot for Ce/K vs Ce (ppm) for Tertiary magmatic associations of the Dinarides; Eocene syncollisional granitoids (.A.); Early Oligocene post-syncollisional granitoids <•); Early Oligocene post-syncollisional shoshonite and high-K calc-alkaline volcanics (0); curve A represents the accumulated fractional melts of an amphibole-bearing lherzolite source whose first 6% melting is controlled by amphibole [98]. (B) Plot of MgO vs Fe0,0 , for plutons from Boranja and Cer (X), Pohorje and Karavanke (0), Rensen (+), Adamello (M. Bergell (D), Thrace (•) and Biella <*).
4A and 9B). This is best exemplified by the Egerian-Eggenburgian (Chattian) volcanic association, which distinctly displays both the slightly increasing fractionation line and the vertical trend, indicating separation and removal of mafic minerals. The Mt. Boranja plutonic rocks display similar, but less prominent, trends.
However, data-points for the Fruska Gora shoshonites are gathered in small, limited fields without any increasing trend. This is in accord with experimental data, suggesting that absarokite magma was generated by melting of the mantle phlogopite lherzolite [101]. This suggests that the Oligocene Fruska Gora shoshonites may have crystallized directly from a shoshonite melt. This is supposed by the fact that the same phenocryst and groundmass mineralogy appears in these rocks. By contrast, the Mt. Rogozna high-K calc-alkaline volcanics and shoshonites lie along the same
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increasing differentiation line with vertical separation trend, suggesting their common origin from one primitive magma as indicated by high Cr (up to 300 ppm) and Ni (up to 200 ppm) concentrations (Table 3 and 4). Apart from this, both shoshonites and high-K calc-alkaline volcanics have the same mineral assemblage and can occur in the same volcanic body [64]. Hence, shoshonites may also be products of fractional differentiation from primary basic magma. It is experimentally documented that shoshonites may also be derived from calc-alkaline basalt melts with K20 > 0.3% by fractionation of plagioclase, clinopyroxene, orthopyroxene and magnetite under relatively dry conditions [102].
In conclusion, the Late Paleogene magmatic associations of the PSVMB were generated in the Africa-Eurasia suture zone that was dominated by slab break-off of the subducted lithospheric slabs at depths of 90-100 km, regardless of whether these slabs were originally related to north- or south-dipping subduction zones. This is indicated by the contemporaneous occurrence of these magmatic associations along the 1700 km long PSVMB, and the compatibility of all geophysical, geological, geochronological, petrological and geochemical data available, and particularly Sr, Nd and 0 isotopic compositions. Concerning the PL, it could be postulated that in this area, original subductionand collision-related magmatic formations disappeared in the interior along the Eocene terminal subduction zone [103].
Upon termination of the Paleogene transpression and related magmatic activity, the area to the north and northeast of the uplifted Dinarides-Hellenides and to the southeast of the Alps was affected by crustal extension related to eastward escape of the Alcapa (Pel so) and Tisia blocks and upwelling of the asthenosphere during the Miocene phases of the Carpathian orogeny [104,105]. This controlled the evolution of the Pannonian Basin, the initial stages of which were accompanied by synsedimentary rift volcanism. The evolution of the southern margin of the Pannonian Basin was strongly controlled by the SVZ, i.e., the southeastern parts of the Alpine suture zone. The accompanying volcanism produced Karpatian (Burdigalian) shoshonites, a Badenian calc-alkaline basalt-andesite-dacite-rhyolite suite and Late Miocene alkali basalts which have been considered in detail elsewhere [78,106,107].
Acknowledgements
The authors are indebted to P. Ziegler, G. Eleftheriadis, K. Stiiwe and V. Cvetkovic for critical reading of the manuscript and support in its preparation. We appreciate the review comments of H. Downes and J.-P. Burg, which have significantly improved the manuscript. This research was financially supported by the Ministry of Science and Technology of the Republic of Croatia (grants 195004, 119304 and 119298).
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