Strontium isotopic, chemical, and sedimentological evidence for the evolution of Lake Lisan and the Dead Sea

Stein, Mordechai; Starinsky, Abraham; Katz, Amitai; Goldstein, Steven L.; Machlus, M.L.; Schramm, Alexandra

doi:10.1016/s0016-7037(97)00191-9

Cited by 287 publications

(211 citation statements)

References 30 publications

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“…In addition to the chemical analysis, Sr isotopic ratios were also measured with a multi-collector inductively coupled plasma mass spectrometer (MC-ICP-MS, NEPTUNE Plus). Sr separation was done with Sr-Spec resin flowing, a method described by Stein et al (1997). Since marine 87 Sr / 86 Sr is constant with a value of 0.70917 (Hodell et al, 1990) while basalt and volcanic rocks have a lower ratio and Saharan dust has higher ratio (Capo et al, 1998, and references therein), this parameter can be used to determine the prevailing aerosol type in the sample due to scavenging.…”

Section: Cloud Water Samplesmentioning

confidence: 99%

The Horizontal Ice Nucleation Chamber (HINC): INP measurements at conditions relevant for mixed-phase clouds at the High Altitude Research Station Jungfraujoch

Lacher¹,

Lohmann²,

Boose

et al. 2017

Atmos. Chem. Phys.

112

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Abstract. In this work we describe the Horizontal Ice Nucleation Chamber (HINC) as a new instrument to measure ambient ice-nucleating particle (INP) concentrations for conditions relevant to mixed-phase clouds. Laboratory verification and validation experiments confirm the accuracy of the thermodynamic conditions of temperature (T ) and relative humidity (RH) in HINC with uncertainties in T of ± 0.4 K and in RH with respect to water (RH w ) of ±1.5 %, which translates into an uncertainty in RH with respect to ice (RH i ) of ±3.0 % at T > 235 K. For further validation of HINC as a field instrument, two measurement campaigns were conducted in winters 2015 and 2016 at the High Altitude Research Station Jungfraujoch (JFJ; Switzerland, 3580 m a.s.l.) to sample ambient INPs. During winters 2015 and 2016 the site encountered free-tropospheric conditions 92 and 79 % of the time, respectively. We measured INP concentrations at 242 K at water-subsaturated conditions (RH w = 94 %), relevant for the formation of ice clouds, and in the watersupersaturated regime (RH w = 104 %) to represent ice formation occurring under mixed-phase cloud conditions. In winters 2015 and 2016 the median INP concentrations at RH w = 94 % was below the minimum detectable concentration. At RH w = 104 %, INP concentrations were an order of magnitude higher, with median concentrations in winter 2015 of 2.8 per standard liter (std L −1 ; normalized to standard T of 273 K and pressure, p, of 1013 hPa) and 4.7 std L −1 in winter 2016. The measurements are in agreement with previous winter measurements obtained with the Portable Ice Nucleation Chamber (PINC) of 2.2 std L −1 at the same location. During winter 2015, two events caused the INP concentrations at RH w = 104 % to significantly increase above the campaign average. First, an increase to 72.1 std L −1 was measured during an event influenced by marine air, arriving at the JFJ from the North Sea and the Norwegian Sea. The contribution from anthropogenic or other sources can thereby not be ruled out. Second, INP concentrations up to 146.2 std L −1 were observed during a Saharan dust event. To our knowledge this is the first time that a clear enrichment in ambient INP concentration in remote regions of the atmosphere is observed during a time of marine air mass influence, suggesting the importance of marine particles on ice nucleation in the free troposphere.

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Section: Cloud Water Samplesmentioning

confidence: 99%

The Horizontal Ice Nucleation Chamber (HINC): INP measurements at conditions relevant for mixed-phase clouds at the High Altitude Research Station Jungfraujoch

Lacher¹,

Lohmann²,

Boose

et al. 2017

Atmos. Chem. Phys.

112

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“…Sr isotope ratios of continental water bodies, on the other hand, reflect the catchment geology and can differ substantially between drainage basins (e.g. Stein et al, 1997;Krom, 1999 Palmer & Edmond, 1989), but also a factor of ~30 higher concentration of dissolved Sr (Broecker & Peng, 1982;Palmer & Edmond, 1989 (Cox & Faure, 1974). These measurements were on bulk carbonates rather than shells, and the differences were not interpreted directly in terms of changes in water chemistry.…”

Section: Isotopic Proxies For Black Sea Hydrologic and Source Changesmentioning

confidence: 99%

The co-evolution of Black Sea level and composition through the last deglaciation and its paleoclimatic significance

Major

Goldstein

Ryan

et al. 2006

Quaternary Science Reviews

179

187

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The strontium and oxygen isotopic compositions of carbonate shells are a measure of the water delivered to the Black Sea lake since the last glacial maximum. Commencing at ~18 ka BP cal with the arrival of substantial meltwater from the Alpine and northern European ice sheets and overflow via the Caspian Sea from the disintegrating Siberian ice cover, the 87 Sr/ 86 Sr ratio rose rapidly from a glacial minima around 0.7087 to reach a set of peaks near 0.7091 in layers of conspicuous reddish-brown clay with a mineralogy of Eurasian provenance. The 87 Sr/ 86 Sr ratio oscillates between high in the red-brown layers to low in interbedded gray clays with glacial era mineralogy, indicative that the meltwater came in pulses. On the other hand, the rise of the 18 O ratio from glacial low values of -7 per mil was delayed until15.2 ka BP cal, after the last meltwater pulse. Sr composition shifted to that of the global ocean and remained there to the present. Since lake water is significantly depleted in strontium relative to seawater, any earlier leakage from the Mediterranean should have left a corresponding signal.

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“…The Dead Sea brines are characterized by a distinct enrichment in calcium and chloride (16,700 and 219,700 mg/l, respectively; Stein et al, 1997), while incoming freshwater runoff, which largely drains carbonate terrains, is enriched in bicarbonate (∼200 mg/l; Stein et al, 1997). The high calcium concentrations in the lake impose very low concentrations of bicarbonate and sulfate through the saturation of calcium carbonate and gypsum (CaSO 4 ·2H 2 O), respectively.…”

Section: Limnologymentioning

confidence: 99%

“…The Dead Sea lacustrine deposits include sequences of alternating aragonite and detrital laminae (aad facies, Figure 2), which represent annual deposition cycles of primary inorganic aragonite precipitated from the lake during summer evaporation and silt-size detritus washed into the lake during winters (Begin et al, 1974;Katz et al, 1977;Stein et al, 1997). The aad facies reflects a wet hydrological regime with high freshwater and thus bicarbonate input, and is associated with relatively higher lake levels.…”

Section: Sedimentologymentioning

confidence: 99%

Rates and Cycles of Microbial Sulfate Reduction in the Hyper-Saline Dead Sea over the Last 200 kyrs from Sedimentary δ34S and δ18O(SO4)

Torfstein

Turchyn

2017

Front. Earth Sci.

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We report the δ 34 S and δ 18 O (SO4) measured in gypsum, pyrite, and elemental sulfur through a 456-m thick sediment core from the center of the Dead Sea, representing the last ∼200 kyrs, as well as from the exposed glacial outcrops of the Masada M1 section located on the margins of the modern Dead Sea. The results are used to explore and quantify the evolution of sulfur microbial metabolism in the Dead Sea and to reconstruct the lake's water column configuration during the late Quaternary. Layers and laminae of primary gypsum, the main sulfur-bearing mineral in the sedimentary column, display the highest δ 34 S and δ 18 O (SO4) in the range of 13-28 and 13-30 , respectively. Within this group, gypsum layers deposited during interglacials display lower δ 34 S and δ 18 O (SO4) relative to those associated with glacial or deglacial stages. The reduced sulfur phases, including chromium reducible sulfur, and secondary gypsum crystals are characterized by extremely low δ 34 S in the range of −27 to +7 . The δ 18 O (SO4) of the secondary gypsum in the M1 outcrop ranges from 8 to 14 . The relationship between δ 34 S and δ 18 O (SO4) of primary gypsum suggests that the rate of microbial sulfate reduction was lower during glacial relative to interglacial times. This suggests that the freshening of the lake during glacial wet intervals, and the subsequent rise in sulfate concentrations, slowed the rate of microbial metabolism. Alternatively, this could imply that sulfate-driven anaerobic methane oxidation, the dominant sulfur microbial metabolism today, is a feature of the hypersalinity in the modern Dead Sea. Sedimentary sulfides are quantitatively oxidized during epigenetic exposure, retaining the lower δ 34 S signature; the δ 18 O (SO4) of this secondary gypsum is controlled by oxygen atoms derived equally from atmospheric oxygen and from water, which is likely a unique feature in this hyperarid environment.

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Strontium isotopic, chemical, and sedimentological evidence for the evolution of Lake Lisan and the Dead Sea

Cited by 287 publications

References 30 publications

The Horizontal Ice Nucleation Chamber (HINC): INP measurements at conditions relevant for mixed-phase clouds at the High Altitude Research Station Jungfraujoch

The Horizontal Ice Nucleation Chamber (HINC): INP measurements at conditions relevant for mixed-phase clouds at the High Altitude Research Station Jungfraujoch

The co-evolution of Black Sea level and composition through the last deglaciation and its paleoclimatic significance

Rates and Cycles of Microbial Sulfate Reduction in the Hyper-Saline Dead Sea over the Last 200 kyrs from Sedimentary δ34S and δ18O(SO4)

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