88Sr/86Sr fractionation and calcite accumulation rate in the Sea of Galilee

Fruchter, Noa; Lazar, Boáz; Nishri, A.; Almogi‐Labin, Ahuva; Eisenhauer, Anton; Shlevin, Y. Be'eri; Stein, Mordechai

doi:10.1016/j.gca.2017.07.026

Cited by 17 publications

(21 citation statements)

References 59 publications

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“…Three species of extant freshwater cyprinids were analysed for their 87 Sr/ 86 Sr: Luciobarbus longiceps, Carasobarbus canis, and Capoeta damascina. The first two species have 87 Sr/ 86 Sr that vary between 0.70731 and 0.70757, agreeing well with water from different depths of Lake Kinneret which have an average 87 Sr/ 86 Sr of 0.70750 ± 0.00005 (2 SE) (Fruchter et al, 2017). Even lower values, between 0.70681 ± 0.00008 and 0.70729 ± 0.00006 (2 SE) were obtained for the C. damascina samples.…”

Section: Sr and O Isotope Data For Modern Fish Teeth And Bonessupporting

confidence: 69%

“…Much lower 87 Sr/ 86 Sr, between 0.70681 ± 0.00008 and 0.70757 ± 0.00005 (2 SE), were measured in the teeth of three species of modern Cyprinidae from Lake Kinneret, which receives its water from the Golan Heights drainage area that is mainly underlain by basaltic bedrocks (Hartman and Richards, 2014). The two freshwater cyprinids Luciobarbus longiceps and Carasobarbus canis have 87 Sr/ 86 Sr that vary between 0.70731 and 0.70757, agreeing well with Lake Kinneret water with an average 87 Sr/ 86 Sr of 0.70750 ± 0.00005 (2 SE) (Fruchter et al, 2017). Even lower values, between 0.70681 ± 0.00008 and 0.70729 ± 0.00006 (2 SE), were obtained for the C. damascina samples that are in good agreement with the Sr isotope composition of the main fresh water source of Lake Kinneret and the Jordan River, which has an average 87 Sr/ 86 Sr of 0.70678 ± 0.00006 (1 SD) (Fruchter et al, 2017).…”

Section: Discussionmentioning

confidence: 68%

“…For the Nile a 87 Sr/ 86 Sr range of 0.70680-0.70718 (Minia, central Egypt, Gerstenberger et al, 1997 and this study) and for the Nile delta and Lake Manzala a range of 0.70680-0.70880 (Reinhardt et al, 2001;Woodward et al, 2015) were used. For Lake Kinneret and the Jordan River, we used a 87 Sr/ 86 Sr range of 0.70684-0.70755 (Fruchter et al, 2017).…”

Section: Bioapatite δ 18 O Po4 Value Reconstruction For Fish From Levantine Water Bodiesmentioning

confidence: 99%

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Strontium and Oxygen Isotope Analyses Reveal Late Cretaceous Shark Teeth in Iron Age Strata in the Southern Levant

et al. 2020

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Skeletal remains in archaeological strata are often assumed to be of similar ages. Here we show that combined Sr and O isotope analyses can serve as a powerful tool for assessing fish provenance and even for identifying fossil fish teeth in archaeological contexts. For this purpose, we established a reference Sr and O isotope dataset of extant fish teeth from major water bodies in the Southern Levant. Fossil shark teeth were identified within Iron Age cultural layers dating to 8–9th century BCE in the City of David, Jerusalem, although the reason for their presence remains unclear. Their enameloid 87Sr/86Sr and δ18OPO4 values [0.7075 ± 0.0001 (1 SD, n = 7) and 19.6 ± 0.9‰ (1 SD, n = 6), respectively], are both much lower than values typical for modern marine sharks from the Mediterranean Sea [0.7092 and 22.5–24.6‰ (n = 2), respectively]. The sharks’ 87Sr/86Sr are also lower than those of rain- and groundwater as well as the main soil types in central Israel (≥0.7079). This indicates that these fossil sharks incorporated Sr (87Sr/86Sr ≈ 0.7075) from a marine habitat with values typical for Late Cretaceous seawater. This scenario is in line with the low shark enameloid δ18OPO4 values reflecting tooth formation in the warm tropical seawater of the Tethys Ocean. Age estimates using 87Sr/86Sr stratigraphy place these fossil shark teeth at around 80-million-years-old. This was further supported by their taxonomy and the high dentine apatite crystallinity, low organic carbon, high U and Nd contents, characteristics that are typical for fossil specimens, and different from those of archaeological Gilthead seabream (Sparus aurata) teeth from the same cultural layers and another Chalcolithic site (Gilat). Chalcolithic and Iron Age seabream enameloid has seawater-like 87Sr/86Sr of 0.7091 ± 0.0001 (1 SD, n = 6), as expected for modern marine fish. Fossil shark and archaeological Gilthead seabream teeth both preserve original, distinct enameloid 87Sr/86Sr and δ18OPO4 signatures reflecting their different aquatic habitats. Fifty percent of the analysed Gilthead seabream teeth derive from hypersaline seawater, indicating that these seabreams were exported from the hypersaline Bardawil Lagoon in Sinai (Egypt) to the Southern Levant since the Iron Age period and possibly even earlier.

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Section: Sr and O Isotope Data For Modern Fish Teeth And Bonessupporting

confidence: 69%

Section: Discussionmentioning

confidence: 68%

Section: Bioapatite δ 18 O Po4 Value Reconstruction For Fish From Levantine Water Bodiesmentioning

confidence: 99%

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Strontium and Oxygen Isotope Analyses Reveal Late Cretaceous Shark Teeth in Iron Age Strata in the Southern Levant

et al. 2020

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“…As already indicated by their seawater-like 87 Sr/ 86 Sr composition, the Sr budget of the calcareous Aegean sediments is dominated by a marine carbonate component (Klaver et al, 2015). Previous studies have found that modern carbonates are isotopically light relative to seawater at δ 88/86 Sr = 0.17-0.21 ‰ (e.g., Halicz et al, 2008;Krabbenhöft et al, 2010;Böhm et al, 2012;Vollstaedt et al, 2014;Fruchter et al, 2017;Müller et al, 2018), with which calcareous Aegean sediments overlap (Figure 4). Although the Sr isotope fractionation factor between seawater and inorganic calcite is dependent on temperature and precipitation rate (Böhm et al, 2012;AlKhatib and Eisenhauer, 2017) and δ 88/86 Sr of seawater has been variable throughout the Phanerozoic, 0-500 Ma carbonates mostly have lower δ 88/86 Sr than MORB (Vollstaedt et al, 2014).…”

Section: The δ 88/86 Sr Composition Of Subduction Zone Inputs 421 mentioning

confidence: 68%

Sr isotopes in arcs revisited: tracking slab dehydration using δ88/86Sr and 87Sr/86Sr systematics of arc lavas

Klaver

Lewis

Parkinson

et al. 2020

Geochimica et Cosmochimica Acta

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Dehydration of the subducting slab is a crucial process in the generation of hydrous convergent margin magmas, yet the exact processes of how and where the slab dehydrates and how these fluids are transported to the mantle wedge remain obscure. Strontium is a "fluid-mobile" element and as such well suited to investigate the source of slab-derived fluids. We employ mass-dependent Sr isotope systematics (δ 88/86 Sr; the deviation in 88 Sr/ 86 Sr of a sample relative to NIST SRM 987) of primitive arc lavas, in tandem with conventional radiogenic 87 Sr/ 86 Sr measurements, as a novel tracer of slab dehydration. To characterise the δ 88/86 Sr composition of subduction zone inputs, we present new δ 88/86 Sr data for subducting sediments, altered oceanic crust and MORB. Calcareous sediments are isotopically lighter and carbonate-free sediments are isotopically heavier than mid-ocean ridge basalts (MORB). Samples of the altered oceanic crust display elevated 87 Sr/ 86 Sr but only the most intensely altered sample has significantly higher δ 88/86 Sr than pristine MORB. Mafic arc lavas from the Aegean and Mariana arc invariably have a mass-dependent Sr isotope composition that is indistinguishable from MORB and lower 87 Sr/ 86 Sr than upper altered oceanic crust. This δ 88/86 Sr-87 Sr/ 86 Sr signature of the arc lavas, in combination with their high but variable Sr/Nd, can only be explained if it is provided by a fluid that acquired its Sr isotope signature in the deeper, less altered part of the subducted oceanic crust. We propose a model where the breakdown of serpentinite in the slab mantle releases a pulse of fluid at sub-arc depths. These fluids travel through and equilibrate with the overlying oceanic crust and induce wet partial melting of the upper altered crust and sediments. This hydrous melt is then delivered to the mantle source of arc magmas as a single metasomatic component. From mass balance it follows that the slab-derived fluid contributes >70 % of the Sr budget of both Mariana and Aegean arc lavas. Whereas this fluid-dominated character is unsurprising for the sediment-poor Mariana arc, the Aegean arc sees the subduction of 3-6 km of calcareous sediments that were found to exert very little control on the Sr budget of the arc magmas and are overwhelmed by the fluid contribution.

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“…Freytet & Verrecchia, ). Crystallization of primary calcite was apparently modulated by phytoplankton blooms, which caused a pH and alkalinity increase in the photic zone, similar to the formation of primary calcite in the modern freshwater Sea of Galilee (Katz & Nishri, 201 3 ; Nishri & Stiller, ; Fruchter et al ., ; Lev et al ., ). The algae bloom in the Sea of Galilee occurs due to elevated nutrient supply into the lake during times of intensified freshwater input.…”

Section: Discussionmentioning

confidence: 99%

Formation of lacustrine dolomite in the late Miocene marginal lakes of the East Mediterranean (Northern Israel)

et al. 2019

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The study focuses on the formation of lacustrine dolomite in late Miocene lakes, located at the East Mediterranean margins (Northern Israel). These lakes deposited the sediments of the Bira (Tortonian) and Gesher (Messinian) formations that comprise sequences of dolostone and limestone. Dolostones are bedded, consist of small-sized (<7 lm), Ca-rich (52 to 56 mol %) crystals with relatively low ordering degrees, and present evidence for replacement of CaCO 3 components. Limestones are comprised of a wackestone to mudstone matrix, freshwater macrofossils and intraclasts (mainly in the Bira Formation). Sodium concentrations and isotope compositions differ between limestones and dolostones: Na =~100 to 150 ppm;~1000 to 2000 ppm; d 18 O = À3Á8 to À1Á6&; À2Á0 to +4Á3&; d 13 C = À9Á0 to À3Á4&; À7Á8 to 0& (VPDB), respectively. These results indicate a climate-related sedimentation during the Tortonian and early Messinian. Wet conditions and positive freshwater inflow into the carbonate lake led to calcite precipitation due to intense phytoplankton blooms (limestone formation). Dry conditions and enhanced evaporation led to precipitation of evaporitic CaCO 3 in a terminal lake, which caused an increased Mg/Ca ratio in the residual waters and penecontemporaneous dolomitization (dolostone formation). The alternating lithofacies pattern reveals eleven short-term wet-dry climate-cycles during the Tortonian and early Messinian. A shift in the environmental conditions under which dolomite formed is indicated by a temporal decrease in d 18 O of dolostones and Na content of dolomite crystals. These variations point to decreasing evaporation degrees and/or an increased mixing with meteoric waters towards the late Messinian. A temporal decrease in d 13 C of dolostones and limestones and appearance of microbial structures in close association with dolomite suggest that microbial activity had an important role in allowing dolomite formation during the Messinian. Microbial mediation was apparently the main process that enabled local growth of dolomite under wet conditions during the latest Messinian.

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88Sr/86Sr fractionation and calcite accumulation rate in the Sea of Galilee

Cited by 17 publications

References 59 publications

Strontium and Oxygen Isotope Analyses Reveal Late Cretaceous Shark Teeth in Iron Age Strata in the Southern Levant

Strontium and Oxygen Isotope Analyses Reveal Late Cretaceous Shark Teeth in Iron Age Strata in the Southern Levant

Sr isotopes in arcs revisited: tracking slab dehydration using δ88/86Sr and 87Sr/86Sr systematics of arc lavas

Formation of lacustrine dolomite in the late Miocene marginal lakes of the East Mediterranean (Northern Israel)

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