Data report: 87Sr/86Sr in pore fluids from IODP Expedition 355 Arabian Sea Monsoon1
Here we report the strontium isotope ratios (87Sr/86Sr) from pore fluids collected during International Ocean Discovery Program (IODP) Expedition 355. Ratios from Sites U1456 (N = 21) and U1457 (N = 20) are reported. Pore fluid 87Sr/86Sr is a useful tool to establish fluid-rock reactions, sources of Sr, and fluid mixing. The measured 87Sr/86Sr of the pore fluid has significant variations at both sites, and three distinct zones are identified. At Site U1456, 87Sr/86Sr starts at values similar to that of modern seawater (~0.7092) from near the seafloor down to ~100 meters below seafloor (mbsf). Over this interval, Sr concentration increases, whereas Ca decreases (Zone 1). Below 100 mbsf, 87Sr/86Sr values increase to a max of ~0.7100 at ~224 mbsf, and Sr concentrations decrease (Zone 2). Isotopic values then gradually decrease to ~0.7085, with an increase in Sr concentrations (Zone 3). Site U1457 displays the same general trends in pore fluid 87Sr/86Sr composition; however, there are distinct differences. First, Zone 1 occurs over a shorter interval (~0–54 mbsf) due to a lower sedimentation rate, and it also has lower Sr concentrations compared to Site U1456. Additionally, 87Sr/86Sr reaches a higher peak value in Zone 2 than at Site U1456. Finally, in Zone 3 the maximum Sr concentration reached is significantly lower than that at Site U1456.
International Ocean Discovery Program (IODP) Expedition 355, Arabian Sea Monsoon, was designed to achieve a better understanding of weathering and erosional patterns in the Himalayan region and of how these patterns respond to variations in the intensity of the Asian monsoon (see the Expedition 355 summary chapter [Pandey et al., 2016b]). To achieve this goal, two sites were drilled, Sites U1456 and U1457 (Figure F1), both located within Laxmi Basin in the eastern Arabian Sea. Drilling recovered sediments extending back to the middle Miocene at Site U1456. At Site U1457, lower Paleocene sediments were recovered directly overlying the basement rock. Laxmi Basin has a significant amount of sediment cover overlying the basement. Clastic sediments within the Arabian Sea are primarily sourced from the Indus River and its associated tributaries and have been since the onset of the India/Eurasia collision (Clift et al., 2001). These sites were drilled primarily to reveal how the Indus Fan evolved through time, to reconstruct the weathering and erosion history of the Western Himalaya, and to address questions pertaining to the nature of the basement in Laxmi Basin (see the Expedition 355 summary chapter [Pandey et al., 2016b]). The recovered sediment allows for examination of the evolution of the Indus Fan since the late Miocene.
Sediments and pore fluids from these cores will be used by scientists to achieve the scientific objectives of Expedition 355. However, these sediments and pore fluids, and any potential proxies archived within them, may be significantly affected by diagenetic reactions occurring within the sediment after deposition, which may affect the signal that is ultimately recorded. In order to make valid interpretations of any proxy record made using samples from the cores, we must first understand what processes have occurred within the sediment and how these processes may have altered them.
Waters buried with sediments are subject to major compositional changes during diagenesis of the sediments. These pore fluids contain a number of tracers that can be used to identify fluid sources and diagenetic reactions. The strontium isotope composition (87Sr/86Sr) of pore waters is a conservative tracer that does not undergo biological fractionation (Mook, 2001) and has been useful in establishing fluid-rock reactions, sources of Sr, and fluid mixing (e.g., Torres et al., 2004; Teichert et al., 2005; Solomon et al., 2009; Joseph et al., 2012, 2013; Moen et al., 2015).
There are several possible sources of Sr to pore fluids recovered with buried marine sediments, each with a distinct range of 87Sr/86Sr values. The first is coeval seawater, which has 87Sr/86Sr values that depend on the age of deposition. Modern seawater has a 87Sr/86Sr value of 0.7092 (McArthur et al., 2012). Another possible source is alteration of continental material. The bulk of the continents are enriched in radiogenic 87Sr, and thus continental felsic and basaltic rocks have relatively high isotopic values (87Sr/86Sr ranges from ~0.7010 to ~0.7180; Faure and Powell, 1972) that, if altered by diagenetic processes, may affect pore fluids. Another possible source is dissolution of biogenic calcite, which has Sr isotopic values ranging from ~0.7075 to 0.7092 coeval with seawater (100 to 0 Ma) (e.g., Gieskes 1981; Hess et al., 1986; Baker et al., 1982; Fantle and DePaolo, 2006; McArthur et al., 2012). Finally, fluid flow from the oceanic crust (~0.703; Veizer, 1989) beneath the sediment may also have an effect on the isotopic composition of the pore fluid near the sediment/crust interface if advection of fluids is significant, which is most common in sediment deposited above very young oceanic crust (Gieskes, 1981; Elderfield and Gieskes, 1982).
This study presents records of 87Sr/86Sr from pore fluids recovered from Sites U1456 and U1457 that were drilled as part of Expedition 355. It should be noted that the data reported here extend to a maximum depth of 864 meters below seafloor (mbsf) at Site U1456 and 848 mbsf at Site U1457. Each site has cored sections below the depths of the samples analyzed; however, pore water fluid sampling was discontinued at these depths. As such, there may be processes occurring within the deepest sediments (lithologic Unit V) not included here. The data reported will be useful for future studies using these sediments and pore fluids to examine fluid-rock reactions that have occurred so that researchers may have a better understanding of the diagenetic processes that have affected the sediments and pore fluids.
Interstitial waters were extracted on board from 5 to 15 cm long whole-round sections that were cut and capped immediately after core retrieval on deck (see the Expedition 355 methods chapter [Pandey et al., 2016a]). Whole-round samples were taken at a frequency of one sample per core (every ~9.5 m) or every other core when using the half-length advanced piston corer (HLAPC). Before squeezing, samples were removed from the core liner and the outer surface was carefully scraped with a spatula to minimize potential contamination by the coring process. The cleaned whole-round samples were placed into a titanium and steel squeezing device modified after the stainless steel squeezer of Manheim and Sayles (1974) and squeezed at ambient temperature with a hydraulic press at pressures of up to ~30,000 psi. The pore water squeezed out of the sediment was extruded into a prewashed (in 10% hydrochloric acid) 60 mL plastic syringe attached to the bottom of the squeezer assembly. The solution was subsequently filtered through a 0.45 µM polysulfone disposable filter (Whatman) into separate vials.
Calcium (Ca2+) and strontium (Sr2+) concentrations of interstitial waters were measured as part of the suite of shipboard geochemical measurements. Ca2+ concentrations were measured by ion chromatography, with an analytical percent error within 1.2% (see the Expedition 355 methods chapter [Pandey et al., 2016a]). Sr2+ concentrations were measured by inductively coupled plasma–atomic emission spectroscopy (ICP-AES) with an analytical percent error better than 1% (see the Expedition 355 methods chapter [Pandey et al., 2016a]).
The isotopic composition of Sr was measured on shore after the end of the expedition in pore fluid samples recovered from 2.95 to 863.69 mbsf at Site U1456 (N = 21) and from 7.87 to 847.97 mbsf at Site U1457 (N = 20). Sr concentrations of from shipboard analyses were used to measure out a specific volume of each pore fluid sample equivalent to 1 µg of Sr for isotopic analysis. Separation of Sr was carried out in the clean laboratory facility located at the University of Texas at Arlington, following the method outlined by Scher et al. (2014). Samples were heated to evaporation in a chemical fume hood. Dried residues were reconstituted in 100 µL of 8 M ultrapure HNO 3 and loaded directly onto Teflon microcolumns with 125 µL stem volumes loaded with Sr-spec resin (Eichrom Technologies, LLC, USA). After loading the sample onto the resin bed, 2 mL of 8 M ultrapure nitric acid was passed through the columns to elute major elements and trace metals. These elutions were discarded. Precleaned Teflon vials were then placed under the columns and 1 mL 0.005 M ultrapure nitric acid was passed through the columns to elute the Sr. Three method blanks were processed in the same manner as described and yielded an average of 17 pg of Sr or about 60,000× lower than the samples.
Isotopic analysis of the solution was carried out using the Neptune Plus multicollector inductively coupled plasma–mass spectrometer (MC-ICPMS) at the University of South Carolina (USA) following Scher et al. (2014). Instrumental mass fractionation during analyses was corrected by normalizing measured ratios to 86Sr/88Sr = 0.1194 using an exponential law. Replicate analysis of standard reference Material (SRM) 987 yielded 0.710315 ± 0.000010 (2σ, N = 17) for a first set of samples and 0.710306 ± 0.000012 (2σ, N = 13) for a second set. 87Sr/86Sr data were normalized to SRM 987, which has a reported 87Sr/86Sr value of 0.710248 (McArthur, 1994). Associated analytical error for each measurement can be found in Tables T1 and T2.
Table T1. Isotopic composition of Sr, Site U1456. Download table in .csv format.
Table T2. Isotopic composition of Sr, Site U1457. Download table in .csv format.
Overall, the Sr isotopic composition of the pore fluid from Site U1456 has significant variations throughout the analyzed cored sections, and there appears to be three distinct zones showing different 87Sr/86Sr patterns (Figure F2). In Zone 1, at the top of the site, the pore fluid has 87Sr/86Sr values similar to that of modern seawater (~0.7092) down to ~100 mbsf. Over this depth interval (0–100 mbsf), Sr concentration in the pore fluid increases, whereas Ca decreases. This interval corresponds to lithologic Unit I, which is characterized by nannofossil ooze and foraminifer-rich nannofossil ooze interbedded with clay, silt, and sand (see the Site U1456 chapter [Pandey et al., 2016c]). The carbonate sediments in the top 100 m of the site are all Pleistocene in age or younger. In general, calcareous nannofossils are moderately to well preserved throughout Site U1456, whereas planktonic foraminifer preservation varies from poor to good (see the Site U1456 chapter [Pandey et al., 2016c]).
In Zone 2, below 100 mbsf, 87Sr/86Sr values rapidly increase to a maximum value of ~0.7100 between 97 and 224 mbsf, whereas Sr concentrations decrease (Figure F2). There are several potential sources of material with high 87Sr/86Sr to the Arabian Sea, each with distinct typical Sr isotopic compositions. These are continental sources including the Deccan basalts (0.704–0.716; Peng et al., 1998), the higher Himalayan crystalline (0.710–0.908; Oliver et al., 2003; Bickle et al., 2005), the lesser Himalayan silicates (0.706–1.311; Singh et al., 1998; Bickle et al., 2001), the Vindhyan Supergroup (0.705–0.709; Ray et al., 2002; Kumar et al., 2002), and the Peninsular gneisses (0.702–0.725; Peucat et al., 1989). A change in lithology is also seen between Zones 1 and 2, where previously carbonate-rich sediments give way to sediments largely dominated by sand and clay.
In Zone 3, between ~224 and ~540 mbsf, 87Sr/86Sr values decrease gradually to ~0.7085. Below this, 87Sr/86Sr values remain relatively constant around 0.7085 over the remainder of the analyzed core samples to 864 mbsf (Figure F2). Also occurring over this interval is a gradual increase in both Sr and Ca concentrations, which reach maximum concentrations of 576 µM (863.69 mbsf) and 15 mM (802.64 mbsf), respectively. Recycled Paleogene carbonates are common throughout this section, where there is evidence of a mass transport deposit (see the Site U1456 chapter [Pandey et al., 2016c]). Marine carbonates from the Paleogene reflect the Sr isotopic signature of coeval seawater, which was less radiogenic than seawater from the late Miocene, which is the maximum age of the sediments examined (see the Site U1456 chapter [Pandey et al., 2016c]). Late Miocene seawater is characterized by 87Sr/86Sr values greater than 0.7088 (see McArthur et al., 2012, and references therein). The Sr isotopic composition of carbonates from the Paleogene ranged from ~0.70820 in the latest Paleogene (23.03 Ma) to a minimum of 0.70772 in the Ypresian (51 Ma) (see McArthur et al., 2012, and references therein).
Similar to Site U1456, Site U1457 displays the same general trends in pore fluid 87Sr/86Sr composition with depth (Figure F3). However, there are some distinct differences that we highlight. The topmost section (Zone 1) has pore fluid with 87Sr/86Sr values similar to that of modern seawater (~0.7092), down to ~54 mbsf, below which 87Sr/86Sr shifts to higher values. This trend is also seen at Site U1456, as both sites are dominated by biogenic calcite in the topmost sections, corresponding to lithologic Unit I. However, the sedimentation rate at Site U1457 was lower (~7 cm/ky) compared to Site U1456 (~12 cm/ky) over this interval (see the Site U1456 and Site U1457 chapters [Pandey et al., 2016c, 2016d]), causing the shift to higher values to begin at a shallower depth at Site U1457 (~54 mbsf) compared to Site U1456 (~100 mbsf) (Figure F4). Also, at Site U1457 the highest Sr concentration reached over this interval is ~206 µM, whereas Sr concentration reaches ~300 µM at Site U1456.
Below 54 mbsf (Zone 2), 87Sr/86Sr values rapidly increase to a maximum value of ~0.7103 at ~193 mbsf, whereas Sr concentration decreases (Figure F3). However, the maximum 87Sr/86Sr value at Site U1457 is significantly higher than that at Site U1456 (0.71032 compared to 0.71000) (Figure F4).
Between ~193 and ~615 mbsf (in Zone 3), 87Sr/86Sr values decrease gradually to ~0.7085. Below this, 87Sr/86Sr remains relatively constant around 0.7085 for the remainder of the analyzed core samples to 848 mbsf (Figure F3). There is also a gradual increase in both Sr and Ca concentrations, which reach maximum concentrations of 220 µM (814.82 mbsf) and 15 mM (738.29 mbsf), respectively. Reworked Cretaceous and Paleogene nannofossils are also common through this interval at Site U1457 (see the Site U1457 chapter [Pandey et al., 2016d]). However, the maximum Sr concentration reached at Site U1457 (220 µM) is significantly lower than the maximum Sr concentration reached at Site U1456 (576 µM) (Figure F4).
According to the data reported here, there are three distinct zones at both sites where different trends of 87Sr/86Sr values (and Sr concentrations) are displayed within the pore fluids. The first, uppermost Zone 1 (~0–100 mbsf at Site U1456 and ~0–54 mbsf at Site U1457), which falls within lithologic Unit I, is identified by pore fluid 87Sr/86Sr values similar to that of modern seawater, increasing Sr concentrations, and decreasing Ca concentrations. Zone 2 (~100–224 mbsf at Site U1456 and ~45–193 mbsf at Site U1457) is characterized by a rapid increase in 87Sr/86Sr values of the pore fluid and a decrease in Sr concentration, dominantly in lithologic Unit II. Finally, Zone 3 (~224–864 mbsf at Site U1456 and ~193–848 mbsf at Site U1457) has gradually decreasing 87Sr/86Sr values until a value of ~0.7085 is reached, where it remains relatively constant. This interval corresponds to lithologic Units III and IV (the latter was only measured at Site U1456).
This research used samples and data provided by the International Ocean Discovery Program (IODP). Funding for this research was provided by a U.S. Science Support Program Post-Expedition Activity Award to E.M. Griffith. We thank Cédric M. John and Denise K. Kulhanek for providing important comments, which helped to improve the present manuscript.
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1 Carter, S.C., Griffith, E.M., Scher, H.D., and the Expedition 355 Scientists, 2017. Data report: 87Sr/86Sr in pore fluids from IODP Expedition 355 Arabian Sea Monsoon. In Pandey, D.K., Clift, P.D., Kulhanek, D.K., and the Expedition 355 Scientists, Arabian Sea Monsoon. Proceedings of the International Ocean Discovery Program, 355: College Station, TX (International Ocean Discovery Program). https://doi.org/10.14379/iodp.proc.355.201.2017
2 School of Earth Sciences, The Ohio State University, USA. Correspondence author: firstname.lastname@example.org
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