Elsevier

Gondwana Research

Volume 23, Issue 2, March 2013, Pages 682-700
Gondwana Research

Evolution and provenance of Neoproterozoic basement and Lower Paleozoic siliciclastic cover of the Menderes Massif (western Taurides): Coupled U–Pb–Hf zircon isotope geochemistry

https://doi.org/10.1016/j.gr.2012.05.006Get rights and content

Abstract

In the Menderes Massif (western Taurides) a Neoproterozoic basement comprising metasediments and intrusive granites is imbricated between Paleozoic platform sediments. U–Pb–Hf zircon analyses of Menderes rock units were performed by us using LA-ICP-MS. The U–Pb detrital zircon signal of the Neoproterozoic metasediments is largely consistent with a NE African (Gondwana) provenance. The oldest unit, a paragneiss, contains significant amounts (~ 30%) of Archean-aged zircons and εHf (t) values of about a half of its Neoproterozoic zircons are negative suggesting contribution from Pan-African terranes dominated by reworking of an old crust. In the overlying, mineralogically-immature Core schist (which is still Neoproterozoic), the majority of the detrital zircons are Neoproterozoic, portraying positive εHf (t) values indicating derivation from a proximal juvenile source, resembling the Arabian–Nubian Shield.

The period of sedimentation of the analyzed metasediments, is constrained between 570 and 550 Ma (Late Ediacaran). The Core schist sediments, ~ 9 km thick, accumulated in less than 20 My implying a tectonic-controlled sedimentary basin evolved adjacent to the eroded juvenile terrane. Granites, now orthogneisses, intruded the basin fill at 550 Ma, they exhibit ± 0 εHf (t = 550 Ma) and TDM ages of 1.4 Ga consistent with anatexis of various admixtures of juvenile Neoproterozoic and Late Archean detrital components. Granites in the northern Arabian–Nubian Shield are no younger than 580 Ma and their εHf (t) are usually more positive. This implies that the Menderes does not represent a straightforward continuation of the Arabian–Nubian Shield.

The lower part of the pre-Carboniferous silisiclastic cover of the Menderes basement, comprises a yellowish quartzite whose U–Pb–Hf detrital zircon signal resembles that of far-traveled Ordovician sandstones in Jordan (including 0.9–1.1 Ga detrital zircons), supporting pre-Triassic paleorestorations placing the Tauride with Afro-Arabia. The detrital signal of the overlying carbonate-bearing quartzitic sequence indicates contribution from a different source: the majority of its detrital zircons yielded 550 Ma and ± 0 εHf (t = 550 Ma) values identical to that of the underlying granitic gneiss implying exposure of Menderes-like granites in the provenance.

260–250 Ma lead-loss and partial resetting of the U–Pb system of certain zircons in both basement and cover units was detected. It is interpreted as a consequence of a Permian–Early Triassic thermal event preceding known Triassic granitoid intrusions.

Graphical abstract

Highlights

► Menderes Neoproterozoic Core schist unit was deposited subsequently to 570 Ma. ► Core schist was sourced from a proximal, juvenile Neoproterozoic crust. ► A paragneiss was sourced from erosion of distal, mostly non-juvenile Pan-African segments. ► 550 Ma anatectic granitoids intruded the basin fill; they do not exist in the Arabian–Nubian Shield. ► Zircons at base of Paleozoic quartzites resemble African sandstone; top resembles local basement.

Introduction

It is commonly accepted that prior to opening of the eastern Mediterranean in the Triassic, the Tauride Block was originally a part of northern Gondwana and was attached to NE Africa (Gutnic et al., 1979, Şengör and Yilmaz, 1981, Garfunkel and Derin, 1984, Robertson et al., 1991, Göncüoglu and Kozlu, 2000, Monod et al., 2003, Garfunkel, 2004, Ghienne et al., 2010). The basement of the Tauride, exposed mainly in the Menderes and Bitlis massifs, and in the Karacahisar and Sandıklı regions (Kröner and Şengör, 1990, Gürsu et al., 2004), was taken to represent the northern continuation of the Neoproterozoic Pan‐African basement of Afro-Arabia (Şengör et al., 1984, Gessner et al., 2004, Ustaömer et al., 2009) that was imprinted by “Cadomian” orogeny (e.g. Neubauer, 2002, Stampfli et al., 2002, Nance et al., 2008). The latter has been delineated as an Andean-type orogenic belt fringing the north Gondwana margin at the closure of the Precambrian (Neubauer, 2002, Nance et al., 2008 and references therein; Ustaömer et al., 2009, Ustaömer et al., 2012).

Although there is a general consensus that during the Paleozoic and until the opening of the eastern Mediterranean the Tauride had resided on the NE African margin of Gondwana, the exact geological properties of its basement and whether it represents a fragment of the Arabian–Nubian Shield (e.g. Ustaömer et al., 2009) or of another Pan-African edifice (e.g. Oberhänsli et al., 2010) are not fully resolved. This is due in part to the fact that subsequently to northward drift from the current SE Mediterranean the Tauride terrane and its Neoproterozoic basement were involved in Alpine orogeny (Robertson et al., 1991, Hetzel and Reischmann, 1996, Bozkurt and Oberhansli, 2001, Okay, 2008) and in post-Alpine extensional tectonics (e.g. Bozkurt and Park, 1994, Bozkurt, 2007, van Hinsbergen et al., 2010). The precise original position of the Tauride block during the Neoproterozoic and prior to the onset of Lower Paleozoic platform sedimentation is thus poorly constrained, and the set of processes shaping and leading to the consolidation of the Taurus basement is not completely clear.

The Neoproterozoic and Paleozoic rock sections of the Menderes Massif in western Anatolia are the targets of the present study. Herein we define the geologic properties of the Menderes Massif basement and its Lower Paleozoic platform sediments by using coupled U–Pb–Hf zircon isotope geochemistry with the aim of clarifying aspects of the Late Neoproterozoic to Early Paleozoic geological evolution of this region. Specifically, the present study focuses on clarifying the age of deposition and the provenance of Neoproterozoic metasediments, on reassessing the age but mainly on defining the respective roles of juvenile magmatic additions versus crustal reworking in the generation of the Late Neoproterozoic Menderes granitoids. The U–Pb–Hf of detrital zircons from the Lower Paleozoic cover helps assessing the provenance of these quartz-rich sandstones and their link to Gondwana.

The Menderes Massif in western Anatolia (Bozkurt and Oberhansli, 2001, Okay, 2008; Fig. 1) is a Tertiary extensional metamorphic core complex (e.g. Bozkurt and Park, 1994, Ring and Collins, 2005) that overprinted an Alpine nappe stack (Ring et al., 1999, Ring et al., 2001, Gessner et al., 2004), probably involving large‐scale recumbent folding (Okay, 2001). Tertiary extensional grabens striking approximately E–W, divide the Menderes into a northern, central and southern submassifs (Figs. 1 and 2).

Neoproterozoic to Late Paleozoic rocks, as well as some Triassic granitoids (Koralay et al., 2001), make up the protolith of the “Menderes nappes”. In the southern submassif (SSM), high- to medium grade Neoproterozoic metasediments, which are intruded by ca. 550 Ma orthogneisses (Çine nappe of Ring et al., 2001), are overlain by low-grade metasediments (Selimiye nappe of Ring et al., 2001) representing the Paleozoic Gondwanan platform (Şengör et al., 1984, Okay, 2001, Gessner et al., 2004, Candan et al., 2011). In the central submassif (CSM) this sequence occurs as isolated klippes (Figs. 1 and 2) thrusted upon the underlying imbricated tectonic sheet (Bozdağ of Ring et al., 2001); the latter shows close similarity with the basement section of the SSM, but exhibits an inverted metamorphic field gradient (Ring et al., 2001) and an inverted stratigraphic order (Hetzel et al., 1998, Dora et al., 2001). The lowermost tectono-stratigraphic unit of the CSM (Bayındır nappe of Ring et al., 2001) is presumably para-autochthonous (Gessner et al., 2004) inferred as correlative to the Paleozoic cover of the SSM (Selimiye) because of its lithology and low-grade metamorphism (Şengör et al., 1984 and references therein; Okay, 2001). Menderes nappes are overthrusted by Mg-carpholite bearing (Rimmele et al., 2003) Mesozoic nappe (Milas marble; Whitney et al., 2008, Gessner et al., 2001) and by the HP-LT Dillek nappe, which exhibits blueschist mineralogy (Ring et al., 1999, Okay, 2001). The Selcuk and Lycian nappes (e.g. Okay, 2008) cape the Alpine nappe edifice of the western Taurides (Fig. 1).

The Neoproterozoic basement section of the Menderes Massif comprises metasedimentary and metamorphosed igneous rocks, bearing evidence for a granulite, eclogite and amphibolite-facies metamorphism (Oberhänsli et al., 1997, Oberhänsli et al., 2010, Candan et al., 2001, Dora et al., 2001). On the basis of the ca. 550 Ma intrusion ages of the orthogneisses (e.g. Gessner et al., 2004), the sedimentation age of the metasedimentary host rocks was estimated as Late Proterozoic (Dora et al., 2001).

The paragneisses (Dora et al., 2001; including “pelitic gneiss” of Hetzel et al., 1998) are fine-grained, massive or slightly foliated. The protolith has been estimated as a litharenite of cratonic provenance (Dora et al., 2001); a 610 Ma age was obtained for the youngest detrital zircon in this unit using Pb/Pb evaporation (Koralay et al., 2003).

The schist sequence was previously described as “Core-series schists” (Dora et al., 2001), “medium- to high-grade schists” (Bozkurt and Oberhansli, 2001 and references therein), “Pan African garnet–mica schist/biotite–albite schist” (Candan et al., 2011), “Boz Dağ schist” (Hetzel et al., 1998), “high-grade schists” (Oberhänsli et al., 2010) and “migmatized Pan-African schists (Core schists)” (Şengün et al., 2006). In the present study we use the term “Core schist”.

The Core schist is usually gray-colored and coarse-grained. Its amphibolite-facies mineralogy includes an almandine-rich garnet; in the deeper part of the sequence kyanite and staurolite are often found (Regnier et al., 2007). U–Pb geochronology of detrital zircons from the Core schists cluster at ca. 640–670 Ma; Grenvillian-aged (ca. 1.0 Ga) and Archean detrital zircons as old as 3239 Ma were also detected (Candan et al., 2011).

In the right-way-up section of the southern submassif, the Paragneiss unit is conformably overlain by the Core schist: the contact is exposed, for example, near Dalama village (Figs. 1 and 2); implying that the paragneiss is stratigraphically older than the Core schist (Şengün et al., 2006). In the overturned sequence of the CSM, the contact is exposed north of Birgi village (Figs. 1 and 2) and the transition zone between both units shows frequent intercalations and transitional facies (Dora et al., 2001).

The metasedimentary host rocks are intruded by strongly deformed granitic orthogneisses (augen gneisses; Bozkurt and Park, 1997, Gessner et al., 2001), which are often associated with metabasic rocks (Hetzel et al., 1998, Candan et al., 2001).

Most zircons from the orthogneisses yield intrusion ages of ca. 550 Ma (Gessner et al., 2004, Hasözbek et al., 2010; see also a summary in Oberhänsli et al., 2010); the orthogneisses from Derbent area in the CSM (Fig. 1) yielded somewhat older Pb–Pb ages of 560–570 Ma (Koralay et al., 2004); some plutons display younger ages of ca. 520 Ma (Loos and Reischmann, 1999). Inherited zircons core ages in all orthogneisses span back to 2555 Ma (Reischmann et al., 1991, Hetzel et al., 1998, Gessner et al., 2004). The granitoids are calc-alkaline, peraluminous, S-type granites and granodiorites, involving some older crustal material in their melt (Bozkurt and Oberhansli, 2001 and references therein; Koralay et al., 2004, Gessner et al., 2004).

Metabasites appear mostly as amphibolitic lenses, enclaves and sheet-like bodies in the granitoids (Oberhänsli et al., 1997, Oberhänsli et al., 2010, Candan et al., 2001) and sometimes as small metagabbro/amphibolitic/eclogitic bodies (e.g. eclogitic body in Kiraz area, CSM — Candan et al., 2001). They are locally crossed by granitic orthogneisses or included as enclaves (Hetzel et al., 1998, Candan et al., 2001). We interpret these field relations as indicating that the metabasic intrusions were synplutonic and generally coeval with the granitoid intrusions. Our interpretation is supported by the fact that U–Pb zircon (TIMS) ages obtained from metagabbros (Oberhänsli et al., 2010) overlap within error the age of intrusion of the granitoids as defined by us and by previous studies. Farther below we suggest that basic magmatism played a major role in the latest Neoproterozoic–Cambrian geodynamic evolution of the Menderes basement.

The Paleozoic cover sequence of the Menderes Massif (Göktepe Formation: Okay, 2001 and references therein) is highly distinctive and well traced in the southern submassif (Fig. 1). The age of the whole formation is considered to be Carboniferous–Permian based on the presence of fauna at the upper part of the black marbles (Dürr, 1975, Şengör et al., 1984, Okay, 2001, Candan et al., 2011). Dora et al. (2001) defined a “yellowish-colored muscovite–quartz schist layer” as a separate unit in the lower part of the cover, probably of Ordovician–Devonian age. In the Central submassif, the lowermost (para-autochthonous; e.g. Gessner et al., 2004) rock section (Bayındır nappe of Ring et al., 2001) lithologically resembles the Göktepe Formation and therefore they are considered correlative (Şengör et al., 1984).

We define two principal quartzitic units in the lower (pre-Permian) siliciclastic part of the cover: Carbonate-bearing quartzites form the top of this sequence gradually intercalated with the overlying black marble. The youngest detrital zircon from the carbonate-bearing quartzitic sequence displays an age of ca. 520 Ma (Loos and Reischmann, 1999), providing a lower bound for the timing of deposition of this part of the sequence. The age of sedimentation of this unit was estimated as Late Devonian–Early Carboniferous, based on poorly preserved briozoa fauna (Konak et al., 1987, Bozkurt and Oberhansli, 2001 and references therein).

The yellowish layer (lowermost yellowish-colored carbonate-poor part of the metaquartzarenite; Candan et al., 2011), associated with channel fill metaconglomerate (Gökçay metaconglomerate; Candan et al., 2011 and references therein), is locally preserved at the base of the cover section in Gökçay area of the SSM (Fig. 1, Fig. 2, and 3). The metaconglomerate defines the erosional contact with the basement (Candan et al., 2011). It contains granitic pebbles whose mineralogy and U–Pb zircon ages are identical to the Neoproterozoic granites below the cover (tourmaline leucocratic granitoids of 549.6 ± 3.7 Ma; Candan et al., 2011).

A summary of the key observations concerning the metamorphic evolution of the Menderes Massif has been provided by Oberhänsli et al. (2010). The Neoproterozoic basement of the Menderes Massif bears several metamorphic mineral assemblages attesting for a complex metamorphic history. Granulite-, eclogite- and amphibolite-facies metamorphic stages were distinguished (Candan et al., 2001 and references therein; Oberhänsli et al., 2010).

Granulite-facies mineral assemblages and coronitic textures are better preserved in the lower part of the basement section — within the paragneisses (Dora et al., 2001) and metagabbros (Candan et al., 2001, Oberhänsli et al., 2010). Metamorphic conditions for these granulite-facies charnockites, orthopyroxene gneisses and orthopyroxene paragneisses indicate temperature of 730–750 °C and pressure of the 6 Kb (Dora et al., 2001 and references therein). Koralay et al. (2006, abs.) reported SHRIMP U–Pb ages of 580 Ma from the interior of unzoned zircons and interpreted these ages as the timing of granulite-facies metamorphism in the paragneiss. Eclogite-facies assemblages in well-preserved (garnet–omphacite) eclogites and eclogitic metagabbros, correspond to P–T conditions of ca. 650 °C and 15 Kb, and overprinted the granulite-facies assemblages; it was recently dated by U–Pb zircon to 530 Ma (Oberhänsli et al., 2010). An amphibolite-facies overprint at 625 °C and 7 Kb (Candan et al., 2001); or minimum P–T conditions of > 500 °C and 7 Kb at the roof of the basement section (Regnier et al., 2003) partially obliterated the eclogitic mineral assemblage in the basement rocks (Candan et al., 2001). This is in line with Rb–Sr whole-rock ages of about 500 Ma (i.e. post-eclogite) obtained from the Menderes basement section by Satir and Friedrichsen (1986), Pb–Pb garnet ages by Ring et al. (2004) and the U–Th–Pb monazite ages from the garnet schist (Catlos and Cemen, 2005).

The fact that all the three aforementioned metamorphic stages are recognized in the metagabbros suggests that the metamorphism affected the Menderes basement subsequently or during the Late Neoproterozoic magmatic activity (570–540 Ma). It is thought that none of these metamorphic phases affected the Phanerozoic cover sediments above the Menderes basement and therefore that they predated sedimentation of the Paleozoic cover (Candan et al., 2001).

The Paleozoic cover section exhibits mostly greenschist facies mineralogy. An Alpine shear zone (Selimiye shear zone: Regnier et al., 2003) separates between basement and cover sections in the SSM concealing the nature of the original basement–cover contact in many places. The basement rocks beneath the shear zone exhibit minimum P–T conditions of 7 Kb and 500 °C, while the P–T conditions in the Paleozoic rocks within the shear zone reached maximum P–T conditions of 4 Kb and 525 °C (Regnier et al., 2003) and were accompanied by a different sense of shear, suggesting a different tectonic direction for the metamorphosed Paleozoic units (e.g. Hetzel and Reischmann, 1996, Regnier et al., 2007). Previous geochronologic studies suggested an Alpine age (Şengör et al., 1984, Hetzel and Reischmann, 1996, Lips et al., 2001) or Early Triassic age (pre-230 Ma; Akkök, 1983) for the greenschist metamorphism.

Section snippets

Sampling: field observations and sample descriptions

Neoproterozoic and Paleozoic rock units of the Menderes Massif were sampled. The sampling locations and sample numbers are marked on the geological map and their relative positions are marked on a tectono-stratigraphic cross section and on a stratigraphic columnar section (Fig. 1, Fig. 2, and 3); their GPS coordinates are provided (Table 1). All analyzed samples were collected stratigraphically below the Permian–Carboniferous marbles, in localities that were well-described in previous studies.

Methods: U–Pb–Hf zircon isotope geochemistry

Zircon U–Pb geochronology coupled with Lu–Hf isotope geochemistry was applied in the present study. The U–Pb geochronology on oscillatory zoned grains provides zircon crystallization ages, while the Lu–Hf isotopic composition obtained from the same grain, provides indication on the average crustal residence time of the parental magma. i.e., the timing of initial separation of the crustal source from the depleted mantle.

Zircons were extracted by standard separation techniques and were mounted in

Results

The results of U–Pb zircon geochronology are given in Table A (Appendix A, Supplementary data). CL imaging of representative zircon types is shown in Fig. 4. The U–Pb results for magmatic samples are plotted on a series of concordia diagrams, weighted average (WA) and probability/density plots in Fig. 5. U–Pb results obtained for detrital samples are presented on probability/density plots in Fig. 7, Fig. 9. 91–109% concordant data points only are plotted; U–Pb ages (238U/206Pb) are used for

Paragneiss

The fine-grained Paragneiss unit is stratigraphically the oldest rock in the Menderes Massif; the detritus it contains has been previously assigned a cratonic provenance (Dora et al., 2001, Şengün et al., 2006). Most zircons from the gray paragneiss are well-rounded supporting long-distance transport. The detrital zircon U–Pb–Hf signal obtained from this rock unit is consistent with derivation from a north African Precambrian crust. About 60% of the detrital zircons yield Neoproterozoic ages

Conclusions

  • The U–Pb–Hf detrital zircon content of the Menderes Neoproterozoic metasediments fit a Gondwana provenance, consistent with derivation from Neoproterozoic Pan-African orogens, most likely from various segments along the east African Orogen and the Sahara Metacraton. The U–Pb–Hf detrital zircon data suggest that at the time the Core schist protholith was deposited, the Menderes terrane must have resided in the vicinity of a juvenile Neoproterozoic crust, resembling but not identical to the

Acknowledgments

This research was supported by the G.I.F., the German–Israeli Foundation for Scientific Research and Development (grant number 977‐168, 8/2007). We thank Erdin Bozkurt for his supportive cooperation all along this project and for a joint field trip; Talip Gungor, Uwe Ring and Klaus Gessner for leading a memorable Samos-Menderes GSA field forum which provided important insights for this study. Zvi Garfunkel is thanked for clarifying many aspects of eastern Mediterranean geology. Discussions with

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