Origin and interactions of fluids circulating over the Amik Basin (Hatay, Turkey) and relationships with the hydrologic, geologic and tectonic settings

Yüce, Galip; Italiano, Francesco; D’Alessandro, W.; Yalçın, Tolga; Yasin, Didem; Gulbay, A.H.; Ozyurt, N. Nur; Rojay, Bora; Karabaçak, Volkan; Bellomo, S.; Brusca, L.; Yang, Tsanyao Frank; Fu, Ching‐Chou; Lai, Chih‐Wei; Özacar, A. Arda; Walia, Vivek

doi:10.1016/j.chemgeo.2014.09.006

Cited by 49 publications

(17 citation statements)

References 89 publications

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“…Representative values of dD H2 (calculated assuming dD H2O = À50) are shown for reference. Alkaline springs/ophiolite data: Hakuba Happo, Japan (Suda et al, 2014); Dinaride ophiolite, Bosnia/Herzegovina (Etiope et al, 2017); Amik Basin, Turkey (Yuce et al, 2014); Semail ophiolite, Oman (Fritz et al, 1992;Miller et al, 2016;Neal and Stanger, 1983;Vacquand et al, 2018); Zambales ophiolite, Philippines (Abrajano et al, 1990;Sherwood Lollar et al, 2007;Vacquand et al, 2018). Zambales data are free gas emanations and dD H2O and maximum measured T of nearby spring water are assumed (Cardace et al, 2015).…”

Section: Introductionmentioning

confidence: 99%

Kinetics of D/H isotope fractionation between molecular hydrogen and water

Pester

Conrad

Knauss

et al. 2018

Geochimica et Cosmochimica Acta

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At equilibrium, the D/H isotope fractionation factor between H 2 and H 2 O (a H2O-H2(eq)) is a sensitive indicator of temperature, and has been used as a geothermometer for natural springs and gas discharges. However, dD H2 measured in spring waters may underestimate subsurface temperatures of origin due to partial isotopic re-equilibration during ascent and cooling. We present new experimental data on the kinetics of D-H exchange for H 2 dissolved in liquid water at temperatures below 100°C. Comparing these results with published exchange rates obtained from gas phase experiments (100-400°C), we derive a consistent activation energy of 52 kJ/mol, and the following rate expressions; ln k ¼ 9:186 À 6298=T and k 1 ¼ 9764:61 ½H 2 O e À6298=T where T is absolute temperature (K), k is the universal rate constant ([L/mol]/hr), and k 1 is a pseudo-first-order constant (hr À1) applicable to water-dominated terrestrial systems by constraining [H 2 O] as the density of H 2 O (in mol/L) at the P-T of interest. The density-dependent rate constant accounts for the kinetic disparity of D-H exchange with H 2 when dissolved in liquid H 2 O relative to a gas/steam phase, exemplifed by 1/k 1 at 100°C of $2 days in liquid, versus $7 yrs in saturated steam. This difference may explain the high variability of dD H2 observed in fumarolic gases. Fluids convecting in the crust frequently reach T > 225°C, where isotopic equilibrium is rapidly attained (<1 hr). We compare fractionation factors measured in natural fluids (a OBS) with values expected for equilibrium at the T of acquisition. Where these values differ, we use kinetic models to estimate cooling rates during upward advection that account for the observed disequilibrium. Models fit to fluids from Yellowstone Park and the Lost City (deep-sea) vent field, both recovered at $90°C, require respective transit times of $7 hrs and $11 days between higher temperature reaction zones and the surface. Using estimates of subsurface depths of origin, however, suggests similar mean fluid flow rates (10 s of meters/hr). Additional complications must be considered when interpreting the dD H2 of lower-temperature effluent. When applied to data from deep-sea hydrothermal systems, our kinetic models indicate microbial catalysis accelerates D-H exchange once fluids cool below $60°C. The H 2 measured in both continental alkaline springs and fracture fluids from Precambrian shield rock is likely produced at T < 100°C, through processes such as serpentinization. In these settings, dD H2 values appear closer to equilibrium with H 2 O than those from geothermal systems. Considering kinetic isotope effects may yield H 2 that is out of equilibrium when generated at lower temperatures, we calculate maximum (isothermal) times to apparent isotopic equilibrium of 1.3 yrs at 50°C, 9 yrs at 25°C, and 35 yrs at 10°C. A similar calculation applied to Antarctic brines (À13°C), where measured dD H2 is far from equilibrium, yields $350 yrs. This time is shorter than the fluids have been isolated (2.8 ka), suggesting...

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Section: Introductionmentioning

confidence: 99%

Kinetics of D/H isotope fractionation between molecular hydrogen and water

Pester

Conrad

Knauss

et al. 2018

Geochimica et Cosmochimica Acta

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“…This region is a window on a complete arc system with fore-arc, volcanic-arc and back-arc. Among various volatile elements in natural gases, helium-3 has been shown to be one of the most powerful tracers of fluid origin on Earth because of its mantle origin and since its isotopic variability depends on the geodynamic setting 21 – 25 , which is characterized by geophysical parameters such as terrestrial heat flow, Bouguer gravity anomaly, seismic velocity (P-wave perturbation), crustal deformation and magnetic anomaly. Therefore, the CH 4 / 3 He ratios of natural gases are expected to provide constraints on the origin of methane.…”

Section: Introductionmentioning

confidence: 99%

Origin of methane-rich natural gas at the West Pacific convergent plate boundary

Sano

Kinoshita

Kagoshima

et al. 2017

Sci Rep

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Methane emission from the geosphere is generally characterized by a radiocarbon-free signature and might preserve information on the deep carbon cycle on Earth. Here we report a clear relationship between the origin of methane-rich natural gases and the geodynamic setting of the West Pacific convergent plate boundary. Natural gases in the frontal arc basin (South Kanto gas fields, Northeast Japan) show a typical microbial signature with light carbon isotopes, high CH4/C2H6 and CH4/3He ratios. In the Akita-Niigata region – which corresponds to the slope stretching from the volcanic-arc to the back-arc –a thermogenic signature characterize the gases, with prevalence of heavy carbon isotopes, low CH4/C2H6 and CH4/3He ratios. Natural gases from mud volcanoes in South Taiwan at the collision zone show heavy carbon isotopes, middle CH4/C2H6 ratios and low CH4/3He ratios. On the other hand, those from the Tokara Islands situated on the volcanic front of Southwest Japan show the heaviest carbon isotopes, middle CH4/C2H6 ratios and the lowest CH4/3He ratios. The observed geochemical signatures of natural gases are clearly explained by a mixing of microbial, thermogenic and abiotic methane. An increasing contribution of abiotic methane towards more tectonically active regions of the plate boundary is suggested.

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“…The A 3 triple junction is currently centered near the Amik subbasin within the Karasu rift ( Fig. 2; Dewey et al, 1986;Over et al, 2004;Yuce et al, 2014), although other triple junction locations have been proposed owing to the tectonic complexity and distributed deformation within the region Research Paper (e.g., Karig and Kozlu, 1990;Tarı et al, 2014). The three plates are separated by two major transform fault systems: the left-lateral NE-SW-trending East Anatolian fault zone and the left-lateral N-S-trending Dead Sea fault zone (Fig.…”

Section: ■ Tectonic Settingmentioning

confidence: 99%

Age and mantle sources of Quaternary basalts associated with “leaky” transform faults of the migrating Anatolia-Arabia-Africa triple junction

et al. 2020

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The Anatolia (Eurasia), Arabia, and Africa tectonic plates intersect in southeast Turkey, near the Gulf of İskenderun, forming a tectonically active and unstable triple junction (the A3 triple junction). The plate boundaries are marked by broad zones of major, dominantly left-lateral transform faults including the East Anatolian fault zone (the Anatolia-Arabia boundary) and the Dead Sea fault zone (the Arabia-Africa boundary). Quaternary basalts occur locally within these “leaky” transform fault zones (similar to those observed within oceanic transform faults), providing evidence that mantle melting, basalt genesis, and eruption are linked to crustal deformation and faulting that extends into the upper mantle. We investigated samples of alkaline basalt (including basanite) from the Toprakkale and Karasu volcanic fields within a broad zone of transtension associated with these plate-boundary faults near the İskenderun and Amik Basins, respectively. Toprakkale basalts and basanites have 40Ar/39Ar plateau ages ranging from 810 ± 60 ka to 46 ± 13 ka, and Karasu volcanic field basalts have 40Ar/39Ar plateau ages ranging from 2.63 ± 0.17 Ma to 52 ± 16 ka. Two basanite samples within the Toprakkale volcanic field have isotopic characteristics of a depleted mantle source, with 87Sr/86Sr of 0.703070 and 0.703136, 143Nd/144Nd of 0.512931 and 0.512893, 176Hf/177Hf of 0.283019 and 0.282995, 206Pb/204Pb of 19.087 and 19.155, and 208Pb/204Pb of 38.861 and 38.915. The 176Hf/177Hf ratios of Toprakkale basalts (0.282966–0.283019) are more radiogenic than Karasu basalts (0.282837–0.282965), with some overlap in 143Nd/144Nd ratios (0.512781–0.512866 vs. 0.512648–0.512806). Toprakkale 206Pb/204Pb ratios (19.025 ± 0.001) exhibit less variation than that observed for Karasu basalts (18.800–19.324), and 208Pb/204Pb values for Toprakkale basalts (38.978–39.103) are slightly lower than values for Karasu basalts (39.100–39.219). Melting depths estimated for the basalts from both volcanic fields generally cluster between 60 and 70 km, whereas the basanites record melting depths of ∼90 km. Depth estimates for the basalts largely correspond to the base of a thin lithosphere (∼60 km) observed by seismic imaging. We interpret the combined radiogenic isotope data (Sr, Nd, Hf, Pb) from all alkaline basalts to reflect partial melting at the base of the lithospheric mantle. In contrast, seismic imaging indicates a much thicker (>100 km) lithosphere beneath southern Anatolia, a substantial part of which is likely subducted African lithosphere. This thicker lithosphere is adjacent to the surface locations of the basanites. Thus, the greater melting depths inferred for the basanites may include partial melt contributions either from the lithospheric mantle of the attached and subducting African (Cyprean) slab, or from partial melting of detached blocks that foundered due to convective removal of the Anatolian lithosphere and that subsequently melted at ∼90 km depth within the asthenosphere. The Quaternary basalts studied here are restricted to a broad zone of transtension formed in response to the development of the A3 triple junction, with an earliest erupted age of 2.63 Ma. This indicates that the triple junction was well established by this time. While the current position of the A3 triple junction is near the Amik Basin, faults and topographic expressions indicate that inception of the triple junction began as early as 5 Ma in a position farther to the northeast of the erupted basalts. Therefore, the position of the A3 triple junction appears to have migrated to the southwest since the beginning of the Pliocene as the Anatolia-Africa plate boundary has adjusted to extrusion (tectonic escape) of the Anatolia plate. Establishment of the triple junction over the past 5 m.y. was synchronous with rollback of the African slab beneath Anatolia and associated trench retreat, consistent with Pliocene uplift in Cyprus and with the current positions of plate boundaries. The A3 triple junction is considered to be unstable and likely to continue migrating to the southwest for the foreseeable geologic future.

show abstract

Origin and interactions of fluids circulating over the Amik Basin (Hatay, Turkey) and relationships with the hydrologic, geologic and tectonic settings

Cited by 49 publications

References 89 publications

Kinetics of D/H isotope fractionation between molecular hydrogen and water

Kinetics of D/H isotope fractionation between molecular hydrogen and water

Origin of methane-rich natural gas at the West Pacific convergent plate boundary

Age and mantle sources of Quaternary basalts associated with “leaky” transform faults of the migrating Anatolia-Arabia-Africa triple junction

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