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Mantle Sources of Recent Anatolian Intraplate Magmatism: A Regional Plume or Local Tectonic Origin?

Abstract We present an extensive study of rehomogenized olivine‐hosted melt inclusions, olivine phenocrysts, and chromian spinel inclusions to explore the link between geodynamic conditions and the origin and composition of Pliocene–Quaternary intraplate magmatism in Anatolia at Kula, Ceyhan‐Osmaniye, and Karacadağ. Exceptional compositional variability of these products reveals early and incomplete mixing of distinct parental melts in each volcanic center, reflecting asthenospheric and lithospheric mantle sources. The studied primitive magmas consist of (1) two variably enriched ocean island basalt (OIB)‐type melts in Kula; (2) both OIB‐type and plume mid‐ocean ridge basalt (P‐MORB)‐like melts beneath Toprakkale and Üçtepeler (Ceyhan‐Osmaniye); and (3) two variably enriched OIB‐type melts beneath Karacadağ. Estimated conditions of primary melt generation are 23–9 kbar, 75–30 km, and 1415–1215 °C for Kula; 28–19 kbar, 90–65 km, and 1430–1350 °C for Toprakkale; 23–18 kbar, 75–60 km, and 1400–1355 °C for Üçtepeler; and 35–27 kbar, 115–90 km, and 1530–1455 °C for Karacadağ, the deepest levels of which correspond to the depth of the lithosphere‐asthenosphere boundary in all regions. Although magma ascent was likely facilitated by local deformation structures, recent Anatolian intraplate magmatism seems to be triggered by large‐scale mantle flow that also affects the wider Arabian and North African regions. We infer that these volcanics form part of a much wider Arabian‐North African intraplate volcanic province, which was able to invade the Anatolian upper plate through slab gaps.


Introduction
The supporting information contains (1) a description of the models, procedures and calculations used in the melt inclusion data analysis; (2) figures that illustrate features of the data complementary to those presented in the main text; and (3) whole-rock, olivine, spinel, melt inclusion and estimated primary melt composition data.

Text S1. High-temperature microthermometry of melt inclusions
As all melt inclusions (MI) in olivine phenocrysts were partially or fully crystallized, hightemperature microthermometric heating/quenching experiments were performed to rehomogenize them prior to analysis. Heating-quenching experiments were performed at the Vrije Universiteit Amsterdam following procedures outlined in Nikogosian et al. (2002). In most cases, complete homogenization was achieved. We used the recorded homogenization temperatures (Thomogenization) as an experimental estimation of the temperatures at which the MI were trapped during host olivine crystallization. Based on 250 runs ( Figure S1), the Thomogenization values range between 1090 and 1270 °C for inclusions within Kula olivines (Fo83-87.5), 1110 and 1285 °C for inclusions within Ceyhan-Osmaniye olivines , and between 1140 and 1240 °C for inclusions within Karacadağ olivines (Fo=75-84.5). Figure S1. Host olivine Fo content (mol %) versus melt inclusion homogenization temperature (°C).

Text S2. Melt inclusion compositions: corrections and calculations
Some of the homogenized MI from Ceyhan-Osmaniye and Karacadağ display lower FeO content than that of the host lavas, and show a negative correlation with the Fo content of their host olivines ( Figure S2). This is typical for the re-equilibration of Fe between MI and their host olivine phenocrysts during slow cooling prior to eruption (cf., Danyushevsky et al., 2000Danyushevsky et al., , 2002a)-a process termed "Fe-loss". To correct for this post-entrapment modification of MI compositions, the method of Danyushevsky et al. (2000) was followed, assuming a uniform initial FeO content corresponding to the FeO content of the respective host rocks (Table S1). The olivine-melt equilibrium model of Ford et al. (1983) was used in the procedure, utilizing Fe 2+ /Fe 3+ ratios in the melt as estimated in coexisting olivine-hosted Cr-spinel inclusions, using the spinel-melt equilibria of Maurel & Maurel (1982) (Fe 2+ /Fe 3+ = 5.5 for samples KAR-1,2,3,4 and OSM-1,2,3,4; and 6.0 for 2A,3,4,5,6,7,. The employed correction procedure mostly affects MgO and FeO content-the effects on other major element oxides were insignificant ( Figure S3) so that overall geochemical trends and variability within the MI remain unchanged. Furthermore, the model of Danyushevsky et al. (2000) was used to calculate the temperature of olivine-MI equilibrium, i.e. the temperature of entrapment ( Figure S4). Figure S2. Host olivine Fo (mol %) versus the FeO* content (wt%) in the uncorrected, homogenized melt inclusions from (a) Kula, (b) Ceyhan-Osmaniye and (c) Karacadağ. Grey field shows the range of FeO* content in the host rocks from each volcanic district, with arrows illustrating the trends for Fe-loss in Ceyhan-Osmaniye and Karacadağ MI. Figure S3. Comparison between homogenized (measured) versus corrected melt inclusion compositions (wt%), illustrating minor differences between them. Shown for comparison are dashed lines at 1:1 (black) and dashed lines (grey) at ± 0.5 wt% for SiO2, MgO, Al2O3 and CaO; ± 0.2 wt% for Na2O, K2O and TiO2; and ± 0.05 wt% for P2O5. The calculated temperatures of equilibrium between the corrected melt inclusion compositions and their olivine hosts range from 1090 to 1275 °C for Kula, 1110 to 1280 °C for Ceyhan-Osmaniye and 1130 to 1255 °C for Karacadağ. As shown in Figure S5, these values are remarkably close to those experimentally determined by homogenization (± 20 °C; see Table S4), demonstrative of a reassuring self-consistency of our methods.

Text S3. Primary melt compositions: criteria and calculations
The studied MI from Kula (Fo87-83), Ceyhan-Osmaniye (Fo87-77) and Karacadağ (Fo85-75) are hosted by olivines which contain somewhat lower forsterite content than those typically in equilibrium with mantle peridotite (Fo > 88; e.g., Arai, 1994). As shown in Figure S6a-S6c, the calculated equilibrium temperatures (following the model of Ford et al. (1983) and Danyushevsky et al. (2001)) of olivine and clinopyroxene allow scrutinization of melt compositions in which olivine was the only crystallizing phase. Excluded, therefore, in the discussion on parental melts (section 5.1) and mantle sources (section 5.2) and the calculation of primary melt compositions (section 5.3 and detailed below), are all melts in which olivine equilibrium temperatures approach those of clinopyroxene within a range of 20 °C ( Figure S6d; compositions denoted by asterisks in Table  S4), thereby ensuring the exclusive (and reversible) effect of liquidus olivine fractional crystallization on the primary melt compositions. Additionally, because olivine does not include nor fractionate trace elements during crystallization, the diversity in trace element ratios of these melt inclusions has remained unchanged and represents that of the primary melts from which they have originated.  (1983). These calculations were performed using Petrolog3 software (Danyushevsky & Plechov, 2011), at dry conditions and using as input parameters the melt oxidation state (Fe 2+/ Fe 3+ as estimated from the ratios in coexisting Cr-spinel inclusions in olivine and the spinel-melt equilibrium of Maurel & Maurel, 1982). The target Fo content used in this calculation was estimated from extrapolation of the relations between olivine Fo content and associated spinel Cr# in the different compositional groups onto the OSMA (illustrated by star symbols in Figure  3d), yielding a minimum value of Fo in equilibrium with the mantle, i.e., Fo88.5 for Kula Group-1, Fo89 for Kula Group-2, Fo87 for Toprakkale, Fo88 for Üçtepeler and Fo90 for Karacadağ.
Systematic variability and groupings observed in trapped melt compositions, such as shown in Figure 7, are similarly present in the calculated primary melts, testifying to the negligible effect of olivine crystallization on the compositional diversity of major elements recorded in the melts.

Text S4. Calculation of oxygen fugacity
Oxygen fugacity (fO2) values ( Figure S7) were obtained following the method of Danyushevsky & Sobolev (1996), which employs the model by Borisov & Shapkin (1989) and utilizes the composition, equilibrium temperature and Fe 2+ /Fe 3+ ratios of the melt inclusions. The latter were estimated from calculated Fe 2+ /Fe 3+ ratios of olivine-hosted spinel inclusions and the experimentally determined spinel-melt equilibria of Maurel & Maurel (1982). Calculations were carried out using Petrolog3 software (Danyushevsky & Plechov, 2011).      Table S1. Major and trace element compositions of the studied whole-rock samples. FeO*: all iron expressed as FeO. Table S2. Compositions of olivine phenocrysts in studied samples. FeO*: all iron expressed as FeO. <d.l. = below detection limit. Table S3. Compositions of spinel inclusions and their olivine hosts. FeO*: all iron expressed as FeO; a: calculated on the basis of stoichiometry. <d.l. = below detection limit. Table S4. Major and trace element compositions of the studied melt inclusions, major element compositions of their olivine hosts and estimated primary melts, experimental homogenization temperature, estimated olivine-MI equilibrium temperature, oxygen fugacity, as well as primary melt generation temperature, pressure and depth. Melt inclusion major element compositions are shown both as measured (uncorrected) and Fe-loss-corrected values (see supporting information Text S1). FeO*: all iron expressed as FeO. n.d. = not determined. <d.l. = below detection limit. * = melts excluded from primary melt calculation due to possible cotectic olivine-clinopyroxene crystallization (see supporting information Text S3).