Analytical methods
Analytical Procedure for Whole Rock Geochemistry
Major and trace element contents of the granitic (38 samples) and metamorphic (4 samples) rocks were measured in Acme Analytical Laboratories Ltd. in Canada. A total of representative 4 sections from the metamorphic rocks were used for electron microprobe analysis on a Cameca SX 100 in the Centre for Earth Sciences in Vienna (Austria). The analytical conditions for the elements were 13 s (10 s for Peak and 3 s for Background) of counting interval, beam current 20 nA and acceleration voltage 15 kV. The results of the geochemical analyses are presented in the accompanying supplementary publication (Table 1 & 2). 
Analytical Procedure for LA-ICP-MC-MS zircon U-Pb dating technique
Four samples were collected from the Doğanşehir granitoid for dating of zircon by the  LA-ICP-MS and U-Pb methods. In addition, three samples from the Berit metaophiolite were dated utilising ID-TIMS Sm-Nd analysis. The LA-ICP-MS and Sm-Nd analytical work was carried outat the Laboratory of Geochronology, Centre for Earth Sciences, University of Vienna. The sample preparation procedure for zircon included crushing, sieving (0-250 mesh size fraction splitted), wet-sieving, heavy liquid (diiodmethan >3.2 gr/cm3), magnetic separation and hand picking under binocular microscope. The handpicked inclusion-free zircon fractions were mounted in epoxy, ground and polished prior to CL imaging and LA-ICP-MS analyses. CL imaging was performed with a JEOL JSM 6310 SEM with 15 kV acceleration voltages at the Institute of Earth Sciences, University of Graz. 
Cathodoluminescence (CL) images of the zircon crystals dated were obtained before LA-ICP-MC-MS dating to distinguish between different zircon domains as well as after LA-ICP-MC-MS measurements to confirm the exact location of the spots/line paths. CL images also provide useful information on the formation history of the zircons, help to identify the existence of more than one zircon domain (i.e. cores, rims) and enable areas of complex zonation to be avoided. In general, weak CL-emission (darker areas in the images) corresponds to relatively high amounts of minor and trace elements, where strong CL emission (lighter areas in the images) reflects relatively low amounts of minor and trace elements, including U (e.g. Sommerauer, 1974; Corfu et al. 2003). 
Zircon 206Pb/238U and 207Pb/206Pb ages were determined using a 193nm solid state Nd-YAG laser (NewWave UP193-SS) coupled to a multi-collector ICP-MS (Nu Instruments HR). Ablation in a He atmosphere was raster-wise according to the CL zonation pattern of the zircons. Line widths for rastering were 25 - 50 µm with a rastering speed of 5 µm/sec. Energy densities were 5 – 8 J/cm2 with a repetition rate of 10 Hz. The  He carrier gas was mixed with the Ar carrier gas flow prior to the plasma torch. Ablation duration was 60 to 120 sec with a 30 sec gas and Hg blank count rate measurement preceding ablation. Ablation count rates were corrected accordingly offline. Remaining counts on mass 204 were interpreted as representing 204Pb. Static mass spectrometer analysis was as follows: 238U in a Faraday detector, 207Pb, 206Pb, and 204 (Pb+Hg) were in ion counter detectors. 208Pb was not analysed. An integration time of 1 sec was used for all measurements. The ion counter – Faraday and inter-ion counter gain factors were determined before the analytical session using standard zircon Plesovice (Slama et al. 2008). During the analytical sessions, mass and elemental bias and mass spectrometer drift of both U/Pb and Pb/Pb ratios, respectively, were corrected using a multi-step approach: first-order mass bias is corrected using a dried 233U-205Tl-203Tl spike solution which was aspirated continuously in Ar and mixed to the He carrier gas coming from the laser before entering the plasma. This corrects for bias effects stemming from the mass spectrometer. The strongly time-dependent elemental fractionation coming from the ablation process itself is then corrected for using the "intercept method" of Sylvester & Ghaderi (1997). The calculated 206Pb/238U and 207Pb/206Pb intercept values are corrected for mass discrimination from analyses of standard Plesovice measured during the analytical session using a standard bracketing method. The correction utilizes regression of standard measurements by a quadratic function. The results of the geochemical analyses are presented in the accompanying supplementary publication (Table 4). 
Analytical Procedure for Sm-Nd dating technique
Before decomposition, handpicked mineral fractions were repeatedly rinsed, using acetone and deionised water in an ultrasonic bath. Refractory phases such as garnet were additionally washed for 30 min in warm (70 °C) 2.5 N HCl to eliminate surface contamination. Handpicked, pure mineral separates used for Sm-Nd and Rb-Sr analysis weighed between 20 and 200 mg. For whole rock analyses, c. 100 mg of ultrafine, well-homogenized sample powder was used.
Sample digestion for Sm-Nd isotope analysis was performed in Savillex® beakers using an ultrapure 5:1 mixture of HF and HClO4 at 110 °C on a hot plate. For whole rock powders, a minimum dissolution time of 3 weeks was applied to ensure complete leaching of the REEs from refractory material such as zircon. After evaporating the acids, repeated treatment of the residue using 5.8 N HCl resulted in clear solutions for all samples. Upon cooling, between 7 and 20 % of the sample solution were split off and spiked for Sm and Nd concentration determination by isotope dilution (ID) using a mixed REE tracer (147Sm-150Nd spike). The REE fraction was extracted using AG® 50W-X8 (200-400 mesh, Bio-Rad) resin and 4.0 N HCl. Nd and Sm were separated from the REE fraction using teflon-coated HdEHP, and 0.24 (0.18 N) and 0.8 (0.4) N HCl, respectively, as elution media. Nd IC samples for minerals were, in some cases, separated twice. Maximum total procedural blanks for both Sm and Nd were < 50 pg. 
Sm & Nd, were run as metals from a Re double filament, using a Finnigan® MAT262 (for ID) and a ThermoFinnigan® Triton TI TIMS (for IC), while Rb fractions were loaded on Ta single filaments using H3PO4, and run on a Finnigan® MAT262 mass spectrometer. A 143Nd/144Nd ratio of 0.511843±0.000001 (n = 17) was determined for the La Jolla (Nd) during the period of investigation. Within-run mass fractionation for Nd isotope compositions (IC) was corrected for relative to 146Nd/144Nd = 0.7219. Uncertainties on the Nd isotope ratios are quoted as 2sm. For the 147Sm/144Nd ratio, a mean error of ±1 % was applied; this includes blank contribution, uncertainties on spike composition, and machine drift; regression calculation is based on these uncertainties and the isochron calculations follow Ludwig (2003). Age calculations (Sm-Nd) are based on a decay constant of 6.54 x 10-12 a-1 for 147Sm (Lugmair & Marti, 1978); age errors are given at the 2s level. For Nd, a continuous depletion of the upper mantle is assumed throughout geological time using the following Depleted Mantle (DM) model parameters: 147Sm/144Nd = 0.222, 143Nd/144Nd = 0.513114 (Michard et al., 1985).

References
Corfu, F., Hanchar, J. M., Hoskin, P. W. O., & Kinny, P. 2003. Atlas of zircon textures. Reviews in Mineralogy and Geochemistry, 53, 469–500.
Ludwig, K.R., 2003. User’s manual for Isoplot 3.00. In: Berkeley Geochronology Center Special Publication, Berkeley, 74 pp.
Lugmair, G. W. & Marti, K. 1978. Lunar initial 143Nd/144Nd: differential evolution of the lunar crust and mantle. Earth and Planetary Science Letters, 39, 3349–3357.
Michard, P., Gurriet, P., Soudant, N. & Albarède, F. 1985. Nd isotopes in French Phanerozoic shales: external vs. internal aspects of crustal evolution. Geochimica et Cosmochimica Acta, 49, 601–610.
Slama, J., Kosler, J., Condon, D. J., Crowley, J. L., Gerdes, A., Hanchar, J. M., Horstwood, M. S. A., Morris, G. A., Nasdala, L., Norberg, N., Schaltegger, U., Schoene, B., Tubrett, M. N. & Whitehouse, M. J. 2008. Plešovice zircon – a new natural reference material for U-Pb and Hf isotopic microanalysis. Chemical Geology, 249(1-2), 1-35.
Sommerauer, J. 1974. Trace elements distribution patterns and mineralogical stability of zircons—an application for combined electron microprobe techniques.  Electron Microscopy Society of South Africa, Proceedings, 4, 71–72.
Sylvester, P. J. & Ghaderi, M., 1997. Trace element analysis of scheelite by excimer laser ablation-inductively coupled plasma-mass spectrometry (ELA-ICP-MS) using a synthetic silicate glass standard. Chemical Geology, 141, 49–65.