Pan-African magmatism in the Menderes Massif: …icpms.ustc.edu.cn/laicpms/publications/2012-KoralayE-IJES.pdf · Pan-African magmatism in the Menderes Massif: ... the Massif is made

ORIGINAL PAPER

Pan-African magmatism in the Menderes Massif:geochronological data from leucocratic tourmalineorthogneisses in western Turkey

O. E. Koralay • O. Candan • F. Chen •

C. Akal • R. Oberhansli • M. Satır •

O. O. Dora

Received: 7 April 2011 / Accepted: 31 March 2012 / Published online: 3 May 2012

� Springer-Verlag 2012

Abstract The Menderes Massif, exposed in western

Anatolia, is a metamorphic complex cropping out in the

Alpine orogenic belt. The metamorphic rock succession of

the Massif is made up of a Precambrian basement and

overlying Paleozoic-early Tertiary cover series. The Pan-

African basement is composed of late Proterozoic me-

tasedimentary rocks consisting of partially migmatized

paragneisses and conformably overlying medium- to

high-grade mica schists, intruded by orthogneisses and

metagabbros. Along the southern flank of the southern

submassif, we recognized well-preserved primary contact

relationship between biotite and leucocratic tourmaline

orthogneisses and country rocks as the orthogneisses rep-

resent numerous large plutons, stocks and vein rocks

intruded into a basement of garnet mica schists. Based on

the radiometric data, the primary deposition age of the

precursors of the country rocks, garnet mica schist, can be

constrained between 600 and 550 Ma (latest Neoprotero-

zoic). The North Africa–Arabian-Nubian Shield in the

Mozambique Belt can be suggested as the possible

provenance of these metaclastics. The intrusion ages of the

leucocratic tourmaline orthogneisses and biotite orthogneis-

ses were dated at 550–540 Ma (latest Neoproterozoic–earliest

Cambrian) by zircon U/Pb and Pb/Pb geochronology. These

granitoids represent the products of the widespread Pan-

African acidic magmatic activity, which can be attributed

to the closure of the Mozambique Ocean during the final

collision of East and West Gondwana. Detrital zircon ages

at about 550 Ma in the Paleozoic muscovite-quartz schists

show that these Pan-African granitoids in the basement

form the source rocks of the cover series of the Menderes

Massif.

Keywords Menderes Massif � Leucocratic tourmaline

orthogneisses � Pan-African magmatism � Zircon U/Pb

and Pb–Pb ages � Mozambique Ocean � Gondwana

Introduction

The Menderes Massif (MM) is divided from north to south

into three submassifs: Demirci-Gordes (northern), Odemis-

Kiraz (central) and Cine submassif (southern), by E–W

trending active graben systems, and is surrounded by the

Alpine high-P tectonic zones of the Anatolides (Fig. 1a;

Sengor and Yılmaz 1981; Okay 1984; Candan et al. 2005;

Rimmele et al. 2006; Pourteau et al. 2010). Traditionally, it

is divided into a polymetamorphic Precambrian basement

(core series) and unconformable overlying Paleozoic–early

Tertiary cover series (Sengor et al. 1984; Candan et al.

2011a), both of which underwent intense Alpine defor-

mation and regional metamorphism in early Tertiary times

due to the closure of the northern branch of the Neotethyan

Ocean (Sengor et al. 1984; Rimmele et al. 2003).

O. E. Koralay (&) � O. Candan � C. Akal � O. O. Dora

Department of Geology, Engineering Faculty, Dokuz Eylul

University, Tınaztepe Campus, 35160 Buca, Izmir, Turkey

e-mail: [email protected]

F. Chen

School of Earth and Space Sciences, University of Science

and Technology of China, Hefei 230026, Anhui Province, China

R. Oberhansli

Institute of Earth and Environmental Sciences, University of

Potsdam, Karl Liebknecht Strasse 24, 14476 Potsdam, Germany

M. SatırDepartment of Geosciences, University of Tubingen,

Wilhelmstraße 56, 72074 Tubingen, Germany

123

Int J Earth Sci (Geol Rundsch) (2012) 101:2055–2081

DOI 10.1007/s00531-012-0775-2

The basement is composed of late Proterozoic clastic

metasedimentary rocks consisting of partially migmatized

paragneisses and conformably overlying medium- to high-

grade mica schists (Dora et al. 2001). This thick meta-

clastic sequence is intruded by orthogneisses and meta-

gabbros-metanorites metamorphosed under eclogite facies

conditions (Oberhansli et al. 1997, 2010; Candan et al.

2001). Recent studies reveal that the orthogneisses were

derived from calcalkaline, peraluminous, S-type and syn-

to post-collisional granitoids (Bozkurt et al. 1995; Loos and

Reischmann 1999; Erdogan and Gungor 2004; Koralay

et al. 2004). Based on the primary mineralogical composition

and textural evidence, different types of orthogneisses, bio-

tite orthogneiss, leucocratic tourmaline orthogneiss and

amphibole orthogneiss, have recently been recognized in the

MM (Bozkurt 2004; Candan et al. 2011a). For the orthog-

neisses, the existing radiometric U–Pb and Pb/Pb data clearly

point to latest Neoproterozoic to early Cambrian intrusion

ages between 570 and 520 Ma with a major event at about

550 Ma (Hetzel and Reischmann 1996; Loos and Reisch-

mann 1999; Koralay et al. 2004; Gessner et al. 2004; Has-

ozbek et al. 2010). Nevertheless, there are still some

controversies, especially, on the leucocratic tourmaline or-

thogneisses (Erdogan and Gungor 2004; Bozkurt 2004;

Bozkurt et al. 2006; Candan et al. 2011a), which have not

been dated radiometrically yet. Based on the general geo-

logical characteristics and kinematic indicators, a ‘Tertiary’

protolith age is postulated for these orthogneisses (Bozkurt

2004; Bozkurt et al. 2006).

The time interval of intrusion ages of these granitoids

(520–570 Ma) coincide with both Cadomian (Linnemann

et al. 2008) and Pan-African (Stern 1994) events. In latest

Neoproterozoic–early Paleozoic paleogeographic recon-

structions, Turkey is accepted as a peri-Gondwanan con-

tinental fragment and is placed at the northernmost end of

the Mozambique Belt (East African Orogeny). Here, we

present our new geological and geochronological data on

the intrusion ages of leucocratic tourmaline orthogneisses

Fig. 1 a General distribution of core and cover series of the Menderes

Massif, surrounded by tectonic zones of the Anatolides; b generalized

geological map of the southern (Cine) submassif (compiled from Dora

et al. 2005; Candan et al. 2011a). Rectangles NE of Yatagan and south of

Kocarlı show the locations of the study areas (Figs. 2, 5). Localities of

dated samples are also marked

2056 Int J Earth Sci (Geol Rundsch) (2012) 101:2055–2081

123

and biotite orthogneisses. This paper has a special focus on

possible genetic relations between this granitic magma and

the late Neoproterozoic–early Paleozoic evolution of the

Mozambique Ocean and Cadomian arc magmatism. Addi-

tionally, some long-lasting controversial subjects will be

discussed such as the deposition age of the country rocks of

the leucocratic tourmaline orthogneisses along the southern

gneiss–schist boundary of the southern submassif and the

possible source rocks of the cover series.

Geological framework of southern submassif

(Cine submassif)

The northern part of the southern submassif is dominated

by Pan-African basement units. To the south, these are

surrounded by Paleozoic–early Tertiary cover series that

forms a continuous, more than 200 km long, E–W trending

strongly folded and imbricated zone. Along the southern

border of the MM, the cover series are tectonically overlain

by the Lycian nappes, which were derived from the

northern part of the Anatolide-Tauride platform and em-

placed southwards over the MM (Fig. 1b).

Orthogneisses are the dominant rock types of the base-

ment in the southern submassif. The oldest units are late

Proterozoic high-grade metaclastics consisting of parag-

neisses and conformably overlying mica schists (Dora et al.

2001). These metaclastics occur either as partly migma-

tized bodies in orthogneisses or as a zone along the

southern gneiss/schist boundary. The para- and orthog-

neisses contain more than 70 individual metagabbro bodies

with amphibolitic marginal zones that occur as stocks and

veins up to 300 m long.

Geology of the study areas

In order to define the basic regional characteristics of the

leucocratic tourmaline orthogneiss, two localities have

been selected and studied in detail: the Seykel/Yatagan

area (Fig. 2) along the southern gneiss/schist boundary and

the Culhalar/Kocarlı area (Fig. 3), 40 km north of this

boundary. As it can be seen in Fig. 4, both areas are made

up of identical units and show a similar lithostratigraphy.

Seykel area

The Seykel area, located 10 km north of Yatagan (Fig. 1b),

was studied previously by Bozkurt (2004). His study was

based on rock types, contact relations, and ages and divided

the metamorphic rocks into two major groups: i) an acidic

meta-igneous complex showing well-preserved primary

intrusive contacts with the surrounding late Proterozoic

metaclastics (Pan-African basement) and ii) Paleozoic

metaclastics and metacarbonates (cover series; Figs. 2, 4).

The contact between these two units is a thrust fault gen-

erated during the Alpine imbrication.

The cover series are completely free of acidic meta-

igneous rocks and consists of metaquartzarenite and phyl-

lite with metacarbonate layers. Although there is no direct

fossil evidence from Seykel, a Permo-Carboniferous age

can be inferred based on the limited paleontological evi-

dence from the same phyllite–marble intercalation in the

MM (Okay 2001). The acidic meta-igneous rocks occur

enclosed in medium-grade mica schists, extending more

than 150 km east–west between Bafa Lake and Babadag as

a continuous unit of variable thickness (Fig. 1b). These

metasediments predominantly comprise garnet mica schists

with subordinate biotite-albite schists derived, respectively,

from mudstone and subarkosic sandstones.

Two types of orthogneisses—biotite orthogneiss and

leucocratic tourmaline orthogneiss—can be distinguished

based on their mafic mineral contents. The biotite orthog-

neisses cropping out in the east and southeast of the study

area occur as numerous large plutons to the north and

northeast of Seykel (Candan et al. 2011a). In low-strain

domains, two types of biotite orthogneiss can be texturally

distinguished. A blastomylonitic biotite orthogneiss, tradi-

tionally called ‘augen gneiss’, was derived from coarse-

grained porphyritic granites (Fig. 5a). ‘Granitic gneisses’

with randomly oriented biotite flakes in an equigranular

quartz and feldspar matrix represent primary coarse-

grained granites with granoblastic texture (Fig. 5b). Both

are two-mica orthogneisses with biotite (more than 15 %)

and muscovite.

Leucocratic tourmaline orthogneisses are light gray to

completely white rocks with high tourmaline content. Their

typical mineral assemblage is K-feldspar, plagioclase,

quartz, muscovite and tourmaline. They locally may con-

tain small individual biotite crystals, \2 vol. %. They

generally occur as large plutons (15 9 10 km), stocks

(1 9 2 km) or aplitic veins in the southern submassif

cutting the basement units (Bozkurt 2004) and represent

the latest stage of Pan-African magmatic activity (Candan

et al. 2011a). A large variety of primary textures of granitic

precursor can still be recognized (Fig. 5c, d), but medium-

to coarse-grained granoblastic granites form the dominant

rock types. Less frequently, they also show coarse-grained

porphyritic textures, which can cause them to be confused

with biotite orthogneisses (augen gneiss). However, the

absence of biotite and their pronounced white color are

distinctive (Fig. 5e). Their most common and diagnostic

mafic phase is tourmaline, which may reach 17 vol.%. It

usually occurs as disseminated small euhedral tourmaline

crystals (Fig. 5d) or less frequent as tourmaline rosettes of

up to 3 cm diameter (Fig. 5f). Tourmaline–quartz nodules

are commonly observed, especially in fine-grained aplitic

Int J Earth Sci (Geol Rundsch) (2012) 101:2055–2081 2057

123

Fig. 2 Geological map of

Seykel area, north of Yatagan

and the localities of the dated

samples. The tectonic contact

between the Pan-African

basement and the Paleozoic

cover series is indicated by a

heavy line. See Fig. 1b for

general location


123

veins (Fig. 5g). Throughout the southern submassif, leuc-

ocratic tourmaline orthogneisses are frequently cut by up to

1 km long, completely white, aplitic veins (Fig. 5h).

In most places, the contact relations between leucocratic

tourmaline orthogneiss and biotite orthogneiss are diffuse,

representing subsequent intrusion of the former into the

Fig. 3 Geological map of

Culhalar area, south of Kocarlıand the locality of the dated

sample. The tectonic contact

between Pan-African Basement

and Paleozoic cover series is

indicated by heavy line. See

Fig. 1b for general location


123

latter, prior to complete solidification. Furthermore, the

leucocratic tourmaline orthogneisses locally display very

sharp, late-stage primary intrusive relations with the biotite

orthogneisses (Fig. 6a). The best preserved intrusive con-

tact relationships can be seen on the Yatagan–Cine high-

way (Fig. 6b, c). There is no structural and textural

evidence of localization of deformation toward, or of ver-

tical offset along the contact. Partly assimilated schist

enclaves with pronounced foliation within completely

undeformed orthogneisses (Fig. 6d) clearly verify the

existence of an earlier phase of deformation and meta-

morphism that can be attributed to a Pan-African event.

Furthermore, a pronounced restriction of garnetiferous

nodules in the mica schist along the contact can be inter-

preted as a moderate contact metamorphic effect of the

granitic precursor of the orthogneisses.

Two sets of the kinematic indicators, top-to the-N–NNE

and top-to-the-S–SSW, are recognized in the Seykel area.

Top-to-the-N movements affected all basements and cover

series units and resulted in the dominant penetrative foli-

ation and lineation. Kinematic indicators in the cover series

include winged calcite inclusions in mylonitic marbles,

oblique foliation in metaquartzarenites and mica fishes in

medium-grained quartz-rich schists and imply non-coaxial

flow with a consistently top-to-the north shear sense. The

indicators can be attributed to the late stage of Alpine

metamorphism and associated internal imbrication. Late-

stage top-to-the-S shear bands that formed under green-

schist facies conditions affected all metasedimentary rocks.

Mica fish with tails showing stair-stepping parallel to

the main foliation, syn-tectonic garnet porphyroblasts

with spiral-shaped quartz inclusion pattern and tourmal-

inite sigmoids are the main kinematic indicators of the

metaclastics of the basement. These top-to-the-N shear

indicators are overprinted by top-to-the-S chloritic C’-type

shear bands with retrograde peak-metamorphic assem-

blages and textures. Top-to-the-N shear sense indicators

are also commonly observed in orthogneisses of the

basement. Due to the nature of their primary textures,

most of the kinematic indicators preferentially formed in

the porphyritic orthogneisses (both biotite- and tourma-

line-rich varieties). These are typical blastomylonites

characterized by a well-developed mylonitic foliation

indicating a top-to-the-N shear sense (Fig. 7a, b). How-

ever, sense of shear indicators is poorly developed in

those biotite- and tourmaline-rich orthogneisses that were

derived from granites with original medium-grained

Fig. 4 The generalized lithostratigraphy of Seykel and Culhalar areas

Fig. 5 Field photographs showing the general characteristics of

biotite and tourmaline orthogneisses. a Primary porphyritic texture in

low-strain domains of biotite orthogneiss; b coarse-grained granob-

lastic texture in biotite orthogneisses, which is defined by randomly

oriented biotite flakes in an equigranular quartzo-feldspathic matrix;

c coarse-grained primary porphyritic textures in slightly deformed

leucocratic orthogneiss; d leucocratic tourmaline orthogneisses

derived from coarse-grained equigranular granites with granoblastic

texture. Black spots are individual tourmaline crystals or aggregates;

e general view of leucocratic orthogneiss consisting of quartz and

feldspars; f tourmaline rosettas in leucocratic orthogneisses; g spher-ical tourmalinite nodules with core of tourmaline–quartz intergrowth

and a quartzo-feldspathic rim; h albite-rich, fine-grained leucocratic

veins in tourmaline leucocratic orthogneiss. Note that the contact is

diffusive representing emplacement of the leucocratic veins before

the complete solidification of the country rock (north of Comakdag)

c


123


123

equigranular polygonal textures. In the orthogneisses, the

main foliation is transected by locally developed, late-

stage shear zones indicating top-to-the-S sense of shear

(Fig. 7c).

Culhalar area/Kocarlı

The Culhalar area is situated at the northwestern edge of

the southern submassif and, similar to the Seykel area,

Fig. 6 Field photographs showing the contact relationships between

biotite and tourmaline orthogneisses and Pan-African metaclastics.

a sharp contact between biotite orthogneiss and tourmaline leuco-

cratic orthogneiss (Cine-Yatagan highway); b biotite orthogneisses,

which are cut by the aplitic vein rock of the leucocratic tourmaline

orthogneisses (Cine-Yatagan highway); c well-preserved primary

intrusive relationships between tourmaline leucocratic orthogneiss

and Pan-African metaclastics (north of Mesken); d partly assimilated

and randomly oriented schist xenoliths in undeformed biotite

orthogneiss, which demonstrate the original intrusive relationship

between biotite orthogneiss and already metamorphosed Pan-African

clastics (Servialan river, 7 km northeast of Seykel); e aplitic vein

rocks of the leucocratic tourmaline orthogneisses in Pan-African

schists (south of Culhalar); f close-up view of cross-cutting relation-

ships between tourmaline leucocratic orthogneiss and schists (south of

Culhalar). bog biotite orthogneiss, s schist, tog tourmaline leucocratic

orthogneiss


123

made up of a Pan-African basement tectonically overlain

by the Paleozoic cover series (Figs. 3, 4). The Paleozoic

units are dominated by black phyllites (*85 %) with

minor amounts of black marbles and yellowish white

metaquartzarenite horizons. The Alpine mineral assem-

blage of the phyllites is quartz, biotite, muscovite, garnet,

staurolite, kyanite and chloritoid with zircon and apatite

as accessory minerals. The contact between core and

cover series is a low-angle ductile shear zone, where the

mylonitic foliation usually dips between 15� and 25�. The

leucocratic tourmaline orthogneiss veins, 3 m below this

contact, were converted to ultramylonites. Evidence for

continuous ductile–brittle deformation is lacking in these

rocks. Thus, this tectonic contact with top-to-the-N sense

of shear can be interpreted as a deep level of a thrust

fault, related to northward thrusting and internal imbrica-

tion of the core–cover series during Alpine compressional

deformation.

The basement consists of a homogeneous metaclastic

sequence and orthogneisses that intruded into it. Over 70 %

of the metaclastics are made up of biotite-albite schists,

characterized by homogenously distributed, isolated biotite

flakes (up to 3 mm) in a quartzo-feldspathic matrix. Garnet

mica schists compose the second lithology. As in the

Seykel area, two orthogneisses types can be distinguished

in this area. Biotite orthogneisses (*80 %) display a my-

lonitic foliation associated with a pronounced NNE–SSW-

to NNW–SSE-trending stretching lineation. Leucocratic

tourmaline orthogneisses occur as a stock-like body

(1.5 9 1 km) and as numerous veins that are up to 300 m

long (Fig. 6e). As described above, they differ markedly

from the biotite orthogneiss by their pronounced white

color and high tourmaline content reaching up to 8 %. The

contact between biotite and leucocratic tourmaline or-

thogneisses is generally not sharp and defined by a pro-

nounced change of biotite and tourmaline contents within a

5- to 15-m-wide zone. However, both orthogneisses display

well-preserved primary intrusive contacts with the sur-

rounding late Proterozoic schists (Fig. 6f). Numerous veins

of black, massive tourmalinites (tourmaline–quartz rocks)

with thicknesses ranging from 10 to 50 cm occur in the

country rocks.

Fig. 7 Kinematic indicators in orthogneisses. a Large orthoclase

porphyroclasts with tails of recrystallized feldspars in blastomylonitic

biotite orthogneiss; b orthoclase porphyroclasts with stair-stepping

trails parallel to main foliation of tourmaline leucocratic orthogneiss.

Black crystals are tourmaline aggregates; c late-stage shear bands

overprinting the main fabric in tourmaline leucocratic orthogneisses;

d sigmoidally curved tourmaline–quartz inclusion derived from

tourmalinite nodules by ductile deformation in tourmaline leucocratic

orthogneiss. Kinematic indicators in (a–b–d) and (c) suggest top-to-

the north and top-to-the south sense of shear, respectively


123

Kinematic indicators in this area indicate a consistent

top-to-the-N shear sense. These older structures are cut by

very rare shear bands showing top-to-the-S movements.

The most common kinematic indicators in the Paleozoic

phyllites of the cover series are syntectonic garnets and rare

syntectonic staurolites implying top-to-the-N shearing, as

well as mica fish textures. Except for very rare, late-stage

top-to-the-S shear bands, only one deformation phase that

formed during Alpine metamorphism and associated

deformation can be recognized in both orthogneiss types.

Deformation intensity in the orthogneisses is heterogeneous

and selectively prefers the granites with porphyritic texture.

They typically have blastomylonitic textures reflecting

deformation under upper green schist to lower amphibolite

facies conditions. In high-strain zones, tourmalinite nodules

in the leucocratic tourmaline granites are flattened and show

common sigmoid shapes (Fig. 7d). The sense of shearing in

both biotite and leucocratic tourmaline orthogneisses is

identical, and all kinematic evidence indicates a consistent

top-to-the-N sense of shear.

U–Pb and Pb/Pb zircon geochronology

Samples

Two leucocratic tourmaline orthogneisses samples (Seykel:

04-65 and Culhalar: 07-31), one biotite orthogneiss (Sey-

kel: 01-201), two garnet mica schists from the Pan-African

basement (Seykel: 02-10 and Bucak: 04-71) and four

muscovite-quartz schist samples from the cover series

(Bucak: 04-190, 05-8, Virankoy: 04-66 and Seykel: 04-72)

with clear geological relationships were selected and dated

(Fig. 1b).

Analytical techniques

Whole-rock powders were obtained by crushing and

splitting ca. 15-kg rock samples. The selected representa-

tive zircons were separated at the Department of Geology

Engineering, Dokuz Eylul University-Turkiye. Zircons

were isolated from crushed rocks by standard mineral sep-

aration techniques and were finally handpicked for analysis

under a binocular microscope. Zircon grains studied by

cathodoluminescence (CL) were mounted in epoxy resin

and polished down to expose the grain centers. CL images

were obtained on a microprobe CAMECA SX51 in Institute

of Geology and Geophysics, Chinese Academy of Sciences

(IGG CAS).

Two different methods were applied for zircon dating.

Zircons from six samples (01-201, 04-65; 02-10, 04-71;

04-66, 04-72) were dated by the single-zircon evaporation

technique using a Finnigan MAT 262 mass spectrometer at

the University of Tubingen. For detailed analytical proce-

dures for the evaporation method see Koralay et al. (2004).

Isotope measurements of zircons from samples 04-190 and

05-08 were dated by the single-zircon evaporation tech-

nique using a GV IsoProbe-T mass spectrometer in the

Laboratory of Radiogenic Isotope Geochemistry of the

Institute of Geology and Geophysics, Chinese Academy of

Sciences, Beijing. The GV IsoProbe-T mass spectrometer

is equipped with a configuration of seven ion-counters.

Beam intensities of 204Pb, 206Pb, 207Pb and 208Pb were

statically measured using four ion-counters. Measurement

of Pb isotopic ratios was simultaneously performed during

heating of the zircon grain, without time-consuming

evaporation-deposition cycles, as compared to conven-

tional evaporation dating technique. Standard solution

materials (NBS982 and NBS981) were measured to nor-

malize difference in efficiency of each ion-counter. Com-

mon Pb contribution was corrected for by using values of

Stacey and Kramers (1975). Using this technique, varia-

tions of 207Pb/206Pb and 208Pb/206Pb ratios can be directly

observed during the simultaneous evaporation and mea-

surement run. These variations are related to the crystalli-

zation history and the U/Th ratio of zircon grain. More

details of the analytical techniques are given in Wang et al.

(2006) and Li et al. (2007). Uncertainties on individual

analyses are reported at a 2 r level, and mean ages for

pooled Pb/Pb analyses are quoted with 95 % confidence

interval. Data reduction was carried out using the Isoplot/

Ex 3.0 program (Ludwig 2003).

Zircon dating of sample 07-31 was performed by laser

ablation ICP-MS at University of Science and Technology

of China in Hefei, using an ArF excimer laser system

(GeoLas Pro, 193-nm wavelength) and a quadruple ICP-

MS (PerkinElmer Elan DRCII). The analyses were carried

out with a pulse rate of 10Hz, beam energy of 10 J/cm2,

and a spot diameter of 60 lm, sometimes 44 lm where

necessary. Uncertainties in isotope ratios are quoted at the

1r level, and uncertainties in ages are reported at the 95 %

confidence level. Detailed analytical procedure is similar to

that of Yuan et al. (2004). Standard zircon 91500 was

analyzed to determine the mass discrimination and ele-

mental fractionation; the U/Pb ratios were processed using

a macro program LaDating@Zrn written in Excel spread-

sheet software. Common Pb was corrected by ComPb

corr#3-18 (Andersen 2002).

Results

Biotite orthogneisses

01-201: This sample was taken from northeast of Seykel,

2 km northwest of Kadıkoy (coordinate: 0606685/4148145)


123

where primary intrusive contact relations between biotite

orthogneisses and garnet mica schist are observed best

(Figs. 1, 2). The sample is coarse-grained with typical bla-

stomylonitic texture and is composed of quartz, orthoclase,

plagioclase, biotite (19 %), muscovite, apatite and zircon.

The zircons are euhedral, predominantly colorless, pink,

transparent, short- and long-prismatic with generally 2:1 and

3:1, rarely 4:1 and 5:1 length/width ratios. The CL photo-

graphs indicate multiple growth stages, and zircons showing

oscillatory zoning indicate a magmatic origin. The cores

generally show zoning with oscillatory bands or sectors and

unzoned domains (Fig. 8a). Magmatic rims with a relatively

strong luminescence surround inherited cores with weaker

luminescence (Fig. 8a, grain 4–6).

Five prismatic single-zircon grains were evaporated and

have very similar ages of 551 ± 5 to 554 ± 6 Ma (Table 1),

yielding a weighted mean age of 552 ± 2 Ma (Fig. 9a). This

age can be interpreted as the most accurate representation of

the intrusion age of the magmatic protolith.

Leucocratic tourmaline orthogneisses

The zircons of leucocratic tourmaline orthogneisses are

characterized by euhedral, elongated shapes and sizes

greater than 200 lm. Aspect ratios range from stubby (1:1

aspect ratio) to elongated (5:1) and are predominantly fall

between 2:1 and 3:1. They are predominantly translucent,

colorless, white and have morphologies that point to an

igneous origin. Pitted surfaces are particularly common in

sample 07-31. In CL images of samples 04-65 and 07-31,

zircons display oscillatory zoning characterized by strong

variation in CL-emission (Fig. 8b, c), as commonly observed

in magmatic zircons. Some zircons have subhedral cores

with oscillatory zoning (Fig. 8b, grains 2–4; Fig. 8c, gr-3).

04-65: Sample 04-65 was taken along the Cine-Yatagan

highway, 2 km west of the Seykel village (coordinate:

0601136/4142493; Figs. 1, 2) where sharp intrusive contact

relations between leucocratic tourmaline and biotite ortho-

gneisses are obvious (Fig. 6a). This sample is a medium-

grained, massive to weakly foliated leucocratic tourmaline

orthogneiss with granoblastic texture composed of quartz,

K-feldspar, plagioclase, muscovite, tourmaline (6 %) and

opaque oxides. Four prismatic zircon grains were evaporated

individually. They yielded very similar ages of 544–547 Ma

(Table 1) and give a weighted mean age of 546 ± 3 Ma,

which can be interpreted as intrusion age (Fig. 9b).

07-31: Sample 07-31 was collected 4.5 km south of the

Culhalar village (coordinate: 0559525/4172810; Figs. 1b,

3). It occurs as a stock-like body with a pronounced

intrusive contact with garnet mica schist (Fig. 3). This

sample is a typical coarse-grained, whitish leucocratic

orthogneiss with high tourmaline content (12 %). Eigh-

teen-point analyses were performed by LA-ICP-MS. Cor-

rected isotope data and ages are presented in Table 2. From

18 zircon analyses, 14 cluster around 550 Ma and yielded

concordant ages. Considering only these fourteen analyses

yields a 206Pb/238U weighted mean age of 552 ± 7 Ma

(Fig. 10) and similarly a 207Pb/235U weighted mean age of

553 ± 8 Ma can be calculated.

Metasedimentary rocks

Garnet mica schists of Pan-African basement

The zircons from basement rocks are somewhat heteroge-

neous in terms of shape, size and color. The majority of the

zircons, however, form euhedral and subhedral groups of

prismatic and subrounded grains that are relatively trans-

parent and clear of alteration. They are predominantly

colorless and have generally 3:1 and 2:1 length/width

ratios. Both prismatic and subrounded grains showing

oscillatory zoning are magmatic in origin. There are very

few metamorphic zircons. CL images reveal that some

have resorbed inner cores (Fig. 8d, grains 1, 6 and 7) and

metamorphic rims with a relatively strong luminescence

(Fig. 8d, grains 1 and 3).

02-10: This sample was collected 250 m east of Seykel

(coordinate: 0603371/4142851; Figs. 1b, 2). It is well

foliated and consists of quartz, plagioclase, muscovite,

biotite, chlorite, garnet, tourmaline, zircon and opaque

oxides. The zircons are predominantly colorless, yellowish,

brownish, clear and transparent with rounded and variably

eroded prismatic faces. Nine single-detrital zircons were

analyzed (Table 1). The ages range from 610 ± 5 to

876 ± 5 Ma. Grain 6 from this sample yielded different

ages for the range of evaporation temperatures and does not

show a flat pattern of 207Pb/206Pb ratios. This is interpreted

as being due to the presence of an inherited core. Grain 7 of

sample 02-10 gave 476 ± 7 Ma for the first, low-temper-

ature (1,390 �C) evaporation step due to some Pb loss from

the outer parts of the grain. We have accepted a 610 ± 5

Ma crystallization age for this grain.

04-71: Sample 04-71 was taken from the Bucak (Gol-

yaka) locality (coordinate: 0548212/4149227; Fig. 1b) and

consists of quartz, plagioclase, muscovite, biotite, chlorite,

garnet, tourmaline, zircon and opaque oxides. The zircons

are predominantly colorless, pink, white, clear, translucent

and transparent with rounded and variably eroded short-

and long-prismatic. Nine single-detrital zircon grains from

this sample were dated (Table 1). The youngest zircon

yielded an age of 601 ± 7 Ma and the oldest zircon

2,455 ± 5 Ma. Grain 5 gave an age from one heating step

only and has therefore been excluded.


123

Fig. 8 Cathodoluminescence

(CL) images of selected zircons

from a biotite orthogneisses

(01-201); b, c leucocratic

tourmaline orthogneisses (04-65

and 07-31); d Pan-African

metasediment (04-71); e, fPaleozoic metasediments (04-66

and 05-08). Spots on zircons

represent areas (40 lm) of

LA-ICPMS analyses for

sample 07-31


123

Table 1 Radiogenic 207Pb/206Pb ratios of evaporated grains and corresponding ages (sp short-prismatic, lp long-prismatic, r rounded, srsubrounded, cl colorless, b brown, p pink, w white, y yellow, c clear, t transparent, tl translucent, 2:1- length: width)

Sample/ Zircon description Number of ratio Evaporation temperature 207Pb/206Pb ratios 207Pb/206Pb age

grain no (�C)/number of steps (mean) (Ma) (2rm)

01-201: Biotite orthogneiss

1 sp, cl, c, t, 2:1 356 1,390–1,430 0.058551 ± 033 551 ± 5

2 sp, cl, c, t, 2:1 118 1,400–1,440 0.058620 ± 053 553 ± 5

3 sp, p, c, t, 2:1 136 1,380–1,420 0.058611 ± 112 553 ± 6

4 sp, cl, c, t, 2:1 125 1,380–1,440 0.058569 ± 118 551 ± 6

5 lp, cl, c, t, 3:1 258 1,380–1,440 0.058631 ± 079 554 ± 6

Mean Grains 1,2,3,4,5 552 ± 2

04-65: Leucocratic tourmaline orthogneiss

1 lp, cl, c, t, 3:1 215 1,380–1,420 0.058406 ± 065 545 ± 5

2 lp, cl, c, t, 3:1 149 1,380–1,400 0.058460 ± 118 547 ± 6

3 lp, cl, c, t, 3:1 251 1,380–1,420 0.058383 ± 390 544 ± 5

4 lp, cl, c, t, 3:1 101 1,380–1,400 0.058456 ± 101 547 ± 6

Mean Grains 1,2,3,4 546 ± 3

02-10: Garnet-mica schist

1 r, y, c, t, 3:1 71 1,400 0.060886 ± 819 635 ± 8

2 r, cl, c, t, 3:1 118 1,400–1,440 0.060580 ± 391 624 ± 5

3 r, cl, c, t, 3:1 136 1,380–1,420 0.060237 ± 368 612 ± 5

4 lp, cl, c, t, 3:1 125 1,380–1,440 0.060829 ± 504 633 ± 6

5 sp, cl, c, t, 2:1 258 1,380–1,440 0.060192 ± 476 611 ± 5

6 sr, cl, c, t, 2:1 139 1,380 0.098892 ± 257 1,604 ± 5

61 1,500 0.162540 ± 528 2,482 ± 6

7 sr, cl, c, t, 2:1 101 1,390 0.056587 ± 175 476 ± 7

38 1,430 0.060172 ± 138 610 ± 5

8 sp, b, c, tl, 2:1 152 1,380–1,420 0.060655 ± 342 627 ± 5

9 sp, b, c, t, 2:1 193 1,390–1,430 0.068254 ± 371 876 ± 5

04-71: Garnet-mica schist

1 sp, w, c, tl, 3:1 52 1,420 0.060072 ± 195 606 ± 8

2 lp, cl, c, t, 3:1 515 1,430–1,470 0.069428 ± 044 912 ± 5

3 lp, cl, c, t, 2:1 57 1,400–1,420 0.066748 ± 154 830 ± 5

4 lp, cl, c, t, 2:1 76 1,400–1,420 0.059914 ± 140 601 ± 7

5 sr, p, c, t, 3:1 217 1,400–1,440 0.159953 ± 221 2,455 ± 5

6 sr, cl, c, t, 3:1 145 1,380–1,400 0.059994 ± 045 603 ± 5

7 lp, w, c, t, 3:1 72 1,420 0.060205 ± 102 611 ± 6

8 sp, cl, c, t, 2:1 49 1,400 0.076135 ± 184 1,099 ± 7

‘‘ 45 1,420 0.083561 ± 168 1,282 ± 6

04-190: Muscovite-quartz schist

1 sp, p, c, t, 2:1 80 1–2 0.083706 ± 32 1,286 ± 7

59 3–4 0.097603 ± 58 1,579 ± 11

2 r, w, c, tl, 3:1 50 1 0.076785 ± 140 1,116 ± 36

57 1 0.094353 ± 160 1,515 ± 32

112 3–4 0.113745 ± 85 1,860 ± 14

3 sr, cl, c, t, 4:1 166 4 0.058897 ± 36 563 ± 13

4 sp, cl, c, t, 2:1 236 5 0.058654 ± 22 554 ± 8

5 sp, cl, c, t, 2:1 147 3 0.068040 ± 40 870 ± 13

6 lp, p, c, t, 3:1 39 1 0.113615 ± 77 1,858 ± 12

102 2–3 0.119765 ± 37 1,953 ± 6


123

Paleozoic cover series

Zircons showing a variety of morphologies (prismatic to

rounded) were separated from three muscovite-quartz

schists (04-72, 04-190 and 05-8) and a phyllite (04-66) of

the cover series. They are heterogeneous, predominantly

colorless, pink, white, translucent, transparent, rounded,

subrounded and short- to long-prismatic with general

aspect ratios of 2:1, rarely 3:1. Some of these detrital

zircons are stubby to oval-shaped with rounded edges.

Most of the euhedral, prismatic zircons show no evidence

of rounding, and some grains have well-preserved crystal

faces with only weakly rounded edges. CL studies of

samples 04-66 and 05-08 show typical oscillatory zoning,

and some zircons have xenocrystic cores, which have

mostly rounded shapes and oscillatory zoning indicative of

magmatic origins (Fig. 8e, grains 2, 5–7; Fig. 8f, grains 2,

3, 5 and 7). Some of these detrital magmatic zircons rarely

Table 1 continued

Sample/ Zircon description Number of ratio Evaporation temperature 207Pb/206Pb ratios 207Pb/206Pb age

grain no (�C)/number of steps (mean) (Ma) (2rm)


1 r, cl, c, t, 3:1 34 1 0.112198 ± 42 1,835 ± 7

167 1–2 0.116583 ± 26 1,905 ± 4

2 sr, cl, c, t, 3:1 29 1 0.071569 ± 100 974 ± 29

3 r, p, c, t, 3:1 75 2 0.067077 ± 35 840 ± 11

4 sr, cl, c, t, 3:1 34 1 0.157199 ± 140 2,426 ± 15

52 1 0.166163 ± 110 2,519 ± 11

39 1 0.171153 ± 100 2,569 ± 10

5 sr, cl, c, t, 3:1 54 1 0.064065 ± 83 744 ± 27

48 1 0.070140 ± 45 933 ± 13

6 lp, cl, c, t, 4:1 77 2 0.058741 ± 44 558 ± 16

7 lp, cl, c, t, 4:1 110 2 0.073099 ± 57 1,017 ± 16

8 lp, cl, c, t, 3:1 100 2 0.075467 ± 36 1,081 ± 10

9 lp, cl, c, t, 3:1 53 1 0.058655 ± 70 554 ± 26

10 lp, cl, c, t, 3:1 136 3 0.062830 ± 39 703 ± 13


1 sp, cl, c, t, 2:1 141 1,410–1,430 0.065390 ± 116 787 ± 6

2 sp, p, c, t, 2:1 24 1,420 0.087653 ± 1093 1,375 ± 101

3 lp, cl, c, t, 3:1 180 1,380–1,400 0.119061 ± 104 1,942 ± 5

4 lp, cl, c, t, 3:1 21 1,420 0.058893 ± 497 563 ± 19

5 sr, cl, c, t, 3:1 19 1,400 0.069359 ± 345 910 ± 11

6 sp, p, c, t, 2:1 299 1,420–1,440 0.110383 ± 54 1,806 ± 5

7 lp, p, c, t, 3:1 259 1,400–1,440 0.069094 ± 53 902 ± 5

8 lp, cl, c, t, 3:1 21 1,400 0.062618 ± 202 695 ± 8

9 lp, p, c, t, 3:1 22 1,400 0.058191 ± 312 537 ± 13

10 lp, s, c, t, 3:1 63 1,420 0.069792 ± 215 922 ± 8

11 sp, p, c, t, 2:1 89 1,400–1,440 0.070399 ± 70 940 ± 5


1 sr, p, c, t, 4:1 90 1,400–1,420 0.071963 ± 87 985 ± 5

2 sr, cl, c, t, 3:1 35 1,400 0.060626 ± 131 626 ± 6

3 r, cl, c, t, 3:1 36 1,420 0.060493 ± 171 621 ± 7

4 r, cl, c, t, 3:1 204 1,430–1,450 0.175185 ± 134 2,608 ± 5

5 sr, cl, c, t, 3:1 15 1,430 0.068604 ± 496 887 ± 16

6 lp, cl, c, t, 4:1 163 1,430–1,455 0.073394 ± 101 1,024 ± 5

7 lp, cl, c, t, 4:1 69 1,420–1,440 0.092533 ± 117 1,478 ± 5

8 r, cl, c, t, 3:1 30 1,420 0.061901 ± 317 671 ± 11

9 sp, w, c, tl, 2:1 307 1,380–1,420 0.056703 ± 47 480 ± 5

10 lp, w, c, tl, 3:1 102 1,380–1,400 0.107104 ± 105 1,751 ± 5


123

show corroded metamorphic overgrowths less than 25 lm

wide (Fig. 8f, grain 6). The crystal surfaces of some grains

appear to be corroded and pitted (Fig. 8e, grains 2–7;

Fig. 8f, grains 2, 4, 5 and 7).

04-72: This sample was collected 2 km southwest of

Seykel (coordinate: 0603848/4142295; Figs. 1b, 2), and the

mineralogical composition is quartz, muscovite, apatite,

zircon and opaque oxides. Eleven zircon grains were

evaporated from this sample, yielding ages ranging from

537 ± 13 to 1,942 ± 5 Ma (Table 1).

04-190: This sample was collected 1 km south of Bucak

(Golyaka) (coordinate: 0547849/4148452; Fig. 1b) and is

composed of quartz, muscovite, apatite and zircon. Six zir-

cons were evaporated, and the youngest age is 554 ± 8 Ma,

while the oldest zircon is 1,953 ± 6 Ma (Table 1).

05-8: This sample was taken 2 km south of Kayadibi

(Virankoy) (coordinate: 0558765/4145542; Fig. 1b) and

consists mainly of quartz, muscovite, apatite and zircon.

The zircons are predominantly colorless, clear, transparent,

subrounded and long-prismatic. Ten zircons were evapo-

rated individually and yielded ages between 554 ± 26 and

2,569 ± 10 Ma (Table 1).

04-66: The sample was taken from 750 m southeast of

Seykel village, along the Cine-Mugla highway, (coordi-

nate: 0602148/4141130; Figs. 1b, 2) and consists mainly of

quartz, muscovite, biotite, chlorite and zircon. Ten zircons

were evaporated individually and ages range from 480 ± 5

to 2,608 ± 5 Ma (Table 1).

Interpretation and discussion

Ages of leucocratic tourmaline orthogneisses and their

country rocks

In recent years, many orthogneisses of the MM have been

dated by different methods. All zircon dating methods

yielded more or less identical ages, restricted to a time span

between 570 and 520 Ma with a major event at about

550 Ma (Table 3). Based on the morphology and zoning

pattern of zircons, these ages have been interpreted as

intrusion ages of the granitic precursor of the orthogneisses

(Hetzel and Reischmann 1996; Loos and Reischmann

1999; Gessner et al. 2001, 2004; Koralay et al. 2004;

Hasozbek et al. 2010). In contrast, in some publications, all

these zircon ages were interpreted as inherited from the

sedimentary source rocks of the granites. Late Cretaceous

to early Cenozoic intrusion ages have been postulated for

these granitoids (Erdogan and Gungor 2004) and late Oli-

gocene-early Miocene ages for the leucocratic tourmaline

orthogneisses (Bozkurt 1996, 2004; Bozkurt and Park

1994, 1997a, b, 2001; Bozkurt et al. 1995, 2006).

Most of the previous dating studies suffer from serious

classification confusion for the dated gneisses due to the

fact that their primary mineralogical and textural charac-

teristics were not considered properly. Different names

such as metagranites, granitic gneisses, augen gneiss, and

orthogneiss have been used for the same rock types. In our

study, leucocratic tourmaline orthogneisses and biotite or-

thogneisses were separated as distinct granite types

Fig. 9 Histograms showing

distribution of 207Pb/206Pb ratios

vs. number of 207Pb/206Pb ratios

derived from evaporation of

zircons from a biotite gneiss

(01-201) and b tourmaline

leucocratic orthogneiss (04-65)


123

Ta

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b/2

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gr

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123

occurring as individual intrusions in several localities of

the MM. They have been dated for the first time by dif-

ferent radiometric methods. In order to determine the

intrusion age of the leucocratic tourmaline orthogneiss and

compare it with that of the biotite orthogneiss, one biotite

orthogneiss (01-201) and one leucocratic tourmaline or-

thogneisses (04-65) from the Seykel area were dated by the

Pb/Pb method. They yielded almost identical Pan-African

ages (552 ± 2 Ma for biotite orthogneiss 01-201 and

546 ± 3 Ma for leucocratic tourmaline orthogneiss 04-65);

the ca. 6-Ma difference is supported by the relative ages as

established from contact relations observed in the field

(Fig. 6a, b). Another leucocratic tourmaline orthogneiss

from the Culhalar area yielded ages (552 ± 7 Ma, sample

07-31) consistent with those from Seykel. Based on mor-

phology and zoning profiles of the selected zircon grains,

these Pan-African ages can be interpreted as intrusion ages

of the granitic precursors of both the biotite and leucocratic

tourmaline orthogneisses. Finally, our field evidence and

isotope data clearly show that the intrusion ages of the

leucocratic tourmaline orthogneisses as well as those of the

biotite orthogneisses are latest Neoproterozoic to earliest

Cambrian (550–545 Ma) and that different orthogneiss

types of the MM represent differentiated products of the

same widespread Pan-African acidic magmatic activity.

The lowest levels of the metamorphic sequence along

the southern flank of the southern submassif are dominated

by metaclastics consisting of garnet mica schist and over-

lying garnet–chloritoid phyllites with thin calc-schist and

muscovite-quartz schist horizons (Fig. 1b; Okay 2001;

Whitney and Bozkurt 2002; Candan et al. 2011a).

Recently, well-preserved intrusive contacts between or-

thogneisses and garnet mica schists have been reported

from along the gneiss-schist boundary, over a distance of

more than 100 km, that are similar to those in other parts

of the MM (Erdogan and Gungor 2004; Bozkurt 2004;

Koralay et al. 2004; Candan et al. 2011a). However, the

primary deposition age of the country rocks of the or-

thogneisses and the existence of a stratigraphical and/or

structural discontinuity within this metaclastic sequence

along the southern flank of the southern submassif have

been subject of a long-lasting debate (Bozkurt 2007 and

references therein).

In order to obtain geochronological data from these

metaclastics, detrital zircons from two garnet mica schists

were dated by single-zircon evaporation method (Fig. 1b).

The garnet mica schists show well-preserved primary

intrusive contact relations with Pan-African orthogneisses,

and the four muscovite-quartz schists occur as horizons in

the phyllites overlying the garnet mica schists along the

gneiss–schist boundary. In the Bafa area, nine zircons from

a garnet mica schist (sample 04-71) yielded scattered ages

between 2,455 and 600 Ma. These garnet mica schists are

intruded by orthogneisses dated at 541 ± 14 Ma (Gessner

et al. 2004). Additionally, in the Seykel area, garnet mica

schists (02-10) intruded by both biotite orthogneiss

(552 ± 2 Ma, sample 01-201) and leucocratic tourmaline

orthogneiss (546 ± 3 Ma, sample 04-65) yielded similar

old detrital zircon ages between 610 Ma and 876 Ma.

Muscovite-quartz schists overlying the garnet mica schists

contain zircons having ages of ca. 550 Ma (04-190: 563

and 554 Ma; 05-08: 557 and 554 Ma; 04-72: 537 and 563

Ma). From the same muscovite-quartz schist horizons,

zircon ages between 526 and 556 Ma have been docu-

mented previously by Loos and Reischmann (1999). These

ca. 550 Ma ages are fully consistent with the intrusion ages

of the orthogneisses (Table 3). The intrusion ages of the

orthogneisses and the youngest detrital zircon age from the

garnet mica schists suggest that the primary deposition age

of the country rocks of the orthogneisses can be con-

strained between 600 Ma and 550 Ma (latest Neoprotero-

zoic). Therefore, they belong to the Precambrian basement

of the MM. The existence of ca. 550-Ma-old zircons in

muscovite-quartz schists (Fig. 11) directly overlying the

garnet mica schists of the basement supports the idea that

there should be a Pan-African unconformity (Sengor et al.

1984; Candan et al. 2011a) and/or an Alpine structural

discontinuity (Selimiye shear zone, Regnier et al. 2003)

between these two metaclastic series. The Pan-African

basement of the MM of orthogneisses and their country

rocks (garnet mica schists) constitute the source rocks of

the Paleozoic cover series, which were deposited on the

northern passive continental margin of the Gondwana. In

conclusion, our field observations and geochronological

data from both the orthogneisses and their country rocks

clearly preclude the view of a close genetic link between

syn-tectonic intrusion of the precursor of the leucocratic

Fig. 10 U–Pb concordia diagram of tourmaline leucocratic orthog-

neiss sample 07-31 in Culhalar area


123

Table 3 Relative and geochronological ages of the orthogneisses occurring in the Pan-African basement of the Menderes Massif

Type of orthogneiss

Location References Original nomenclature This study Method Ages (Ma)

Geochronological ages

Demirci-Gordes submassif

SE of Simav

SW of Demirci

Demirkopru Dam

Dannat (1997) Augen gneiss – Pb/Pb

evapor

541.4 ± 2.5

537.2 ± 2.4

544.1 ± 4.3

S of Kula Dora et al. (2002) Granitic gneiss Biotite gneiss Pb/Pb

evapor

549.7 ± 7.6

N of Simav Hasozbek et al. (2010) Augen gneiss Biotite gneiss Pb/Pb

evapor

550–607

U–Pb

isotope

dill

543.0 ± 10

Odemis-Kiraz submassif

NE of Kuyucak

W of Buldan

SD of Kiraz

Dannat (1997) Augen gneiss

Augen gneiss

Augen gneiss

–

–

Biotite gneiss

Pb/Pb

evapor

528.0 ± 4.3

528.1 ± 1.6

538.1 ± 2.6

S of Alasehir Koralay et al. (2004) Orthogneiss Biotite gneiss Pb/Pb

evapor

561.5 ± 0.8

570.5 ± 2.2

Cine submassif

– Dora (1975, 1976) – – Rb–Sr wr 490 ± 90

SW of Cine Sengor et al. (1984); Satır and

Friedrichsen (1986)

Metagranite – Rb–Sr wr 470 ± 9

N of Selimiye Hetzel and Reischmann (1996) Augen gneiss Tourmaline leucocratic

orthogneiss

Pb/Pb

evapor

546.0 ± 1.6

546.4 ± 0.8

N of Selimiye Loos and Reischmann (1999) Granitic gneiss Tourmaline leucocratic

orthogneiss

Pb/Pb

evapor

563 ± 3, 536 ± 9

572 ± 7, 521 ± 8

556 ± 4, 546 ± 5

551 ± 5

SW of Cine Gessner et al. (2001) Metagranite Tourmaline leucocratic

orthogneiss

Pb/Pb

evapor

547.2 ± 1.0

N of Yatagan Gessner et al. (2004) Metagranite Tourmaline leucocratic

orthogneiss

U–Pb

SHRIMP

541 ± 14

SW of Cine Metagranite Biotite gneiss U–Pb

SHRIMP

566 ± 9

N of Yatagan Dora et al. (2005) Granitic gneiss Biotite gneiss Pb/Pb

evapor

552.1 ± 2.4

NW of

Kavaklıdere

Porpyritic metagranite Leucocratic

metagranite porphyr

Pb/Pb

evapor

551.5 ± 2.9

N of Yatagan Tourmaline leucocratic

orthogneiss

Tourmaline leucocratic

orthogneiss

Pb/Pb

evapor

545.6 ± 2.7

N of Yatagan Tourmaline leucocratic

orthogneiss


orthogneiss

U–Pb

isotope

dill

549 ± 26

NW of Karacasu Koralay et al. (2007) Amphibole gneiss Amphibole gneiss Pb/Pb

evapor

530.9 ± 5.3

Relative ages

N of Selimiye Bozkurt and Park (1994) Augen gneiss Tourmaline leucocratic

orthogneiss

Late oligocene

N of Selimiye Bozkurt et al. (1995) Augen gneiss Tourmaline leucocratic

orthogneiss

Late oligocene/

early miocene


123

tourmaline orthogneiss along a Tertiary detachment fault

that was situated between the orthogneisses and the garnet

mica schists, and the Oligo-Miocene exhumation of the

southern submassif along this fault (Bozkurt 1996, 2004;

Bozkurt and Park 1994; Bozkurt et al. 2006).

Detrital zircon age spectra from the garnet mica schists

show that the majority of zircon ages define a Neoprote-

rozoic population (15 grains, 83 %; Fig. 11). The oldest

detrital ages of 2,455 ± 5 Ma and 2,482 ± 6 Ma indicate

the presence of a Paleoproterozoic component for the

source rocks of the garnet mica schists. The age groups of

the detrital grains obtained from the garnet mica schists of

the southern submassif (17 analyses) reflect input from

sources with ca. 600–635 Ma, ca. 830–910 Ma, 1,282 Ma

and ca. 2,455–2,482 Ma ages. Such an age pattern is

similar for Gondwanan sources(Loos and Reischmann

1999; Keay and Lister 2002; Gessner et al. 2004; Sunal

et al. 2006) and, more specifically, can be correlated with

N-NE Africa (Fig. 11). The existence of a significant

Neoproterozoic detrital zircon population (83 %, 600–

1000Ma) in garnet mica schists of the MM indicates a

possible provenance from the Saharan Metacraton/Ara-

bian-Nubian Shield, hence the correlation with the

Mozambique Belt where such an age range is common

(Figs. 11, 12; Stoeser and Camp 1985; Tadese-Alemu

1998; Teklay et al. 1998, 2001; Cosca et al. 1999; Kebede

et al. 2001; Kuster and Liegeois 2001; Abdelsalam et al.

2002; Moghazi 2002; Yibas et al. 2002; Eyal et al. 2004;

Andersson et al. 2006; Vogt et al. 2006; Andresen et al.

2010; Liegeois and Stern 2010; Shang et al. 2010; Grantham

et al. 2011).

Tectonic setting of the granitic precursors

of the orthogneisses

Based on the latest Neoproterozoic–early Cambrian

paleogeographic reconstruction of the continents, Turkey

as well as the MM are placed at the northern margin of

Gondwana (Sengor et al. 1984, Stern 1994; Kroner and

Stern 2005; Monod et al. 2003) where the nearly coeval,

late Precambrian–earliest Paleozoic Cadomian and Pan-

African magmatic–metamorphic events left clear marks

(Fig. 13). Although both orogenic events are characterized

by regional metamorphism and associated voluminous

granite generation, they display some striking diversities.

In general, the 750- to 530-Ma Cadomian Orogeny was an

Andean type, subduction-related peripheral orogeny at the

margin of Gondwana and was characterized by widespread

I-type, arc-related magmatic activity (Linnemann et al.

2008). In contrast, the East African Orogeny (Mozambique

Belt) contains voluminous S-type granitic magma gener-

ated during continental collision of East and West

Gondwana along the Mozambique Ocean (Stern 1994),

resulting in the final amalgamation of Gondwana. Fur-

thermore, as major crustal thickening, subduction of con-

tinental crust and continent–continent collision did not take

place during the Cadomian Orogeny (Linnemann et al.

2008), Cadomian terranes underwent only greenschist to

upper amphibolite facies metamorphism. In contrast, the

Mozambique Belt is characterized by the common evi-

dence for granulite (Stern 1994) and, more rarely, eclogite

facies metamorphism (Ring et al. 2002).

Neoproterozoic to early Paleozoic tectonic elements

extend as discontinuous exposures in central crystalline

basement of Europe and from the Alps to Turkey in the

Alpine–Mediterranean mountain belt (Neubauer 2002). In

the Alps, Cadomian units with ca. 570–520 Ma basic to

acidic intrusions have been documented from the Penninic

and Austroalpine zones (Muller et al. 1995; Eichhom et al.

1999; Neubauer 2002). Additionally, granitic intrusions,

ascribed to the Cadomian event, have been reported from

the Variscan basement of central Europe (Armorican

Massif, 573–581 Ma, Inglis et al. 2005, 572 Ma, D’Lemos

et al. 2001; Iberian Massif, 570–580 Ma, Bandres et al.

2004; Bohemian Massif, 541 Ma, Dorr et al. 2002; 567

Ma; Friedl et al. 2004; 533–548 ± 9 Ma; Zelazniewicz

et al. 2004), the southern Carpathians (567 ± 3 Ma; Lie-

geois et al. 1996), the Bulgarian sector of the Sebro–

Macedonian Massif (550 and 545 Ma; Neubauer 2002), as

well as the Pelagonian Zone (546 ± 10 Ma; Anders et al.

Table 3 continued

Type of orthogneiss

Location References Original nomenclature This study Method Ages (Ma)

N of Yatagan Erdogan and Gungor (2004) Augen gneiss Tourmaline leucocratic

orthogneiss

Late cretaceous/

early cenozoic

N of Yatagan Bozkurt (2004) Tourmaline leucocratic

orthogneiss


orthogneiss

Late oligocene/

early miocene

South of Cine

submassif

Bozkurt et al. (2006) Tourmaline leucocratic

orthogneiss


orthogneiss

Tertiary


123


123

2007). Linnemann et al. (2008) suggest that during the

period 570–520 Ma, these vast amounts of calc-alkaline,

dominantly I-type granitoids formed along an Andean-type

active margin/island arc and reflect subduction of an oce-

anic crust beneath Gondwana.

In Turkey, granitoids with intrusion ages between 520

and 590 Ma have been documented from the Istanbul Zone,

Sandıklı area, Afyon Zone, Bitlis Massif and MM

(Fig. 13). Granites and associated volcanics in the base-

ment of the Istanbul Zone (eastern part of the Istanbul

Zone: 560–590 Ma, Chen et al. 2002; Bolu Massif:

576 ± 6 Ma and 565 ± 2 Ma, Ustaomer et al. 2005; and

western part of Armutlu peninsula: 570 Ma, Okay et al.

2008) have been reported. These calc-alkaline and I-type

intrusions are interpreted as the products of mantle derived

and crustally contaminated arc-type magmas that

Fig. 11 Probability density distribution histogram of the ages from

the MM and age distribution from Saharan Metacraton, Arabian-

Nubian Shield and MM. c data from Hetzel and Reischmann (1996),

Dannat (1997), Loos and Reischmann (1999), Gessner et al. (2001,

2004), Koralay et al. (2004), Dora et al. (2002, 2005), Hasozbek et al.

(2010); Candan et al. (2011a); d data from Loos (1995), Loos and

Reischmann (1999), Gessner et al. (2001, 2004), Koralay et al.

(2004), Dora et al. (2002, 2005), Candan et al. (2011a); e data from

Loos (1995); for Saharan Metacraton and Arabian-Nubian Shield data

sources: see Ustaomer et al. (2012). B basement, C cover series, NPNeoproterozoic

b

Fig. 12 Late Proterozoic/Cambrian paleogeographic map of the

Gondwana super continent (modified after Wilson et al. 1997 and

Kroner and Stern 2005). The Mozambique Belt and Late Proterozoic–

Cambrian isotopic ages of magmatic rocks are shown on the map.

Location of magmatic rocks (500–570 Ma) are after 1 Moghazi

(2002); 2 Gessner et al. (2004); 3: Farahat et al. (2007); 4 Stoeser and

Camp (1985); 5 Abdelsalam et al. (2002); 6 Teklay et al. (1998); 7Yibas et al. (2002); 8 Stern (1994); 9 Wilson et al. (1997); 10

Goodenough et al. (2010); 11 Liu et al. (2006) and 12 Raharimahefa

and Kusky (2010).AS Arabian Shield, DA Damara, DM Dom

Feliciano, DR Denman Darling, M Madagascar, MA Mauretanides,

MM Menderes Massif, PB Pryd Bay, PR Pampean Ranges, PSPaterson, QM Queen Maud Land, SD Saldania, SG South Granulite

Terrane, TAM Transantarctic Mountains, TS Trans-Sahara belt, ZBZambezi


123

developed on an Andean-type active margin and are

ascribed to the Cadomian Orogeny. In the Sandıklı area,

mylonitized granites and meta-quartz porphyries were

dated at 543 ± 7 Ma (Kroner and Sengor 1990) and

541 ± 9 Ma (Gursu et al. 2004). In the Afyon Zone, meta-

quartz porphyries yielded similar ages (541 ± 4 Ma;

Gursu et al. 2005). These I-type arc magmatic rocks, which

are assumed to be related to southward subduction of

oceanic crust beneath the northern margin of Gondwana,

are ascribed to the Cadomian Orogeny (Bozkaya et al.

2006; Gursu et al. 2005; Gursu and Goncuoglu 2006).

Additionally, the Mutki granites and associated vein rocks

in the Bitlis Massif have U/Pb zircon ages of 546 ± 6 and

531 ± 4 Ma (Ustaomer et al. 2009). Ustaomer et al. (2009)

suggest that this Ediacaran–early Cambrian magmatic

activity belongs to Cadomian arc-magmatism bordering the

northern margin of Gondwana.

On a regional scale, common ca. 550-Ma granitoid

intrusions have been documented along the Mozambique

Belt and have been related to the closure of Mozambique

Ocean (Fig. 12; Stoeser and Camp 1985; Stern 1994;

Wilson et al. 1997; Teklay et al. 1998; Abdelsalam et al.

2002; Moghazi 2002; Yibas et al. 2002; Gessner et al.

2004; Liu et al. 2006; Farahat et al. 2007; Goodenough

et al. 2010; Raharimahefa and Kusky 2010). The geo-

chronological data presented in this and previous studies

clearly reveal the existence of widespread acidic magmatic

activity in the latest Neoproterozoic basement of the MM

(Hetzel and Reischmann 1996; Loos and Reischmann

1999; Koralay et al. 2011) that spanned the period

520–590 Ma, having an average age of about 550 Ma. A

detailed geochemical–petrological study considering the

geological relations, ages and metamorphic character of the

orthogneisses has not been carried out yet. However, based

on limited geochemical data (Bozkurt et al. 1993, 1995,

2006; Dannat 1997; Koralay et al. 2004), it is suggested

that the orthogneisses were derived from medium-K calc-

alkaline, peraluminous, S-type, syn- to post-orogenic

granites, which themselves were most probably generated

by partial melting of lower continental crust during conti-

nent–continent collision. The late Neoproterozoic meta-

morphic history of the Precambrian basement of the MM,

Fig. 13 Locations of Pan-African and Cadomian magmatic activities

in Turkey. Cadomian locations from Kroner and Sengor (1990),

Gursu and Goncuoglu (2006), Gursu et al. (2005), Okay et al. (2008),

Ustaomer et al. (2005) and Ustaomer et al. (2009). Pan-African

locations from Hetzel and Reischmann (1996), Loos and Reischmann

(1999), Gessner et al. (2001, 2004), Chen et al. (2002), Dora et al.

(2002), Koralay et al. (2004) Dora et al. (2005). AES Ankara-Erzincan

Suture, AZ Afyon Zone, B Balkanides, BFZ Bornova Flysch Zone,

BM Bolu Massif, BPM Bitlis-Poturge Massif, IPS Intra-Pontid Suture,

IAZ Izmir-Ankara Suture, IZ Istanbul Zone, KM Kırsehir Massif, LNLycian Nappes, MM Menderes Massif, PS Pamphylian Suture, RSMRhodope-Strandja Massif, S Sandıklı, SZ Sakarya Zone, TB Thrace

Basin, TZ Tavsanlı Zone


123

in contrast, has been studied in detailed (Candan et al.

2001, 2011b; Oberhansli et al. 1997, 2010). Petrological

and geochronological data clearly reveal a polymetamor-

phic evolution of the Precambrian basement under granu-

lite (583 ± 6 Ma; Koralay et al. 2006), eclogite (530 ± 22

Ma; Oberhansli et al. 2010) and upper amphibolite facies

(551 ± 1 Ma; Hetzel et al. 1998) conditions (Fig. 14). The

medium-temperature eclogites are assigned to extreme

crustal thickening induced by continental collision during

the collision of East and West Gondwana (Candan et al.

2011a, b). In contrast to the Cadomian event, the late

Neoproterozoic–early Cambrian closure of the Mozam-

bique Ocean and the related Pan-African Orogeny is

characterized by regional-scale granulite (610–520 Ma;

average 550 Ma; Key et al. 1989; Ayalew and Gichile

1990; Holzl et al. 1994; Paquette et al. 1994; Shiraishi et al.

1994) and, more rarely, eclogite facies (530–500 Ma; Ring

et al. 2002) metamorphism. Based on the paleogeographic

position and good correlation of the major metamorphic

events, the polymetamorphic history of the MM basement

has been attributed to final amalgamation of Gondwana

along the Mozambique Ocean, that is East African Orog-

eny, since a long time (Sengor et al. 1984, Satır and

Friedrichsen 1986; Dora et al. 2002, 2005; Candan et al.

2001, 2011b; Hetzel and Reischmann, 1996; Dannat 1997;

Hetzel et al. 1998; Loos and Reischmann 1999; Gessner

et al. 2001; Okay 2001; Gessner et al. 2004; Koralay et al.

2004). As it can be seen in Fig. 14, these polyphase

metamorphic events (585–530 Ma), which are assigned to

the Pan-African Orogeny, coincide with the intrusion per-

iod of the orthogneisses (590–520 Ma).

Finally, using the close relation between polyphase

metamorphic events and multistage granite intrusions as

discussed above, we can attribute the formation of latest

Neoproterozoic–early Cambrian granitoid intrusions (bio-

tite and tourmaline orthogneisses) in the MM to processes

such as the closure of the Mozambique Ocean and conti-

nental collision of East and West Gondwana. Therefore,

the MM can be placed on the northernmost end of the

Mozambique Belt (Fig. 12).

Conclusions

Field observations, detailed mapping and new geochrono-

logical data on the orthogneisses and their country rocks of

the MM allow the following conclusions:

• The intrusion ages of the leucocratic tourmaline

orthogneisses and biotite orthogneisses are latest Neo-

proterozoic to earliest Cambrian (550–540 Ma). These

granitoids in the MM are the products of a widespread

Pan-African acidic magmatic activity occurring between

590 and 520 Ma.

• Based on the good temporal with the polymetamorphic

history of Precambrian basement of the MM, these

granitoid intrusions can be attributed to the closure of

the Mozambique Ocean and the continental collision of

East and West Gondwana during the latest Neoprote-

rozoic to earliest Cambrian.

• The primary magmatic contacts between orthogneisses

and country rocks are still preserved. The primary

deposition age of these country rocks, which are exposed

continuously along the southern gneiss boundary in the

southern submassif, is latest Neoproterozoic, 600–550

Ma. The Saharan Metacraton and Arabian-Nubian Shield

in the Mozambique Belt are suggested to be the possible

sources of these metasedimentary rocks.

• Detrital zircon ages of *550 Ma in the muscovite-

quartz schists indicate that the Pan-African basement

forms the source rocks for the cover series of the MM.

Fig. 14 Latest Neoproterozoic–early Cambrian magmatic phases and

metamorphic events of the Pan-African basement. 1–2 Dora et al.

(2002), Koralay et al. (2005), Candan et al. (2011b); 3–4: Koralay

et al. (2006), Koralay et al. (unpublished data); 5–7: Hetzel and

Reischmann (1996), Loos and Reischmann (1999), Gessner et al.

(2001, 2004), Koralay et al. (2004), Hasozbek et al. (2010); Candan

et al. (2011a); 8 Hetzel et al. (1998); 9 Candan et al. (2011b),

Oberhansli et al. (2010)


123

Acknowledgments This study was financially supported by The

Scientific and Research Council of Turkey (TUBITAK; grant no.

YDABCAG – 101 Y 132) as well as the Volkswagen-stiftung/Ger-

many. The support of these granting agencies is warmly acknowl-

edged. We wish to thank Wolfgang Siebel, Qiuli Li and Zhenhui Hou

for assistance with the Pb–Pb evaporation and LA-ICP-MS datings.

We thank Gultekin Topuz and an anonymous reviewer for construc-

tive comments and suggestions. Thanks are also due to Aral Okay and

Martin Timmermann for their invaluable criticism on the text.

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