Integrated multi-site U–Th chronology of the last glacial Lake Lisan

Torfstein, Adi; Goldstein, Steven L.; Kagan, Elisa J.; Stein, Mordechai

doi:10.1016/j.gca.2012.11.003

Cited by 79 publications

(89 citation statements)

References 43 publications

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“…The exploration of the paleoseismic history of the late Quaternary Dead Sea basin (DSB) was accompanied by significant advances in establishing the stratigraphic‐chronological framework of the Lisan Formation based on several exposed sections at the DSB (Torfstein, Goldstein, Kagan, et al, ) and the recent recovery of deep sedimentary cores at the abyssal (300 m water depth) and shallow floors of the modern Dead Sea (the Dead Sea International Continental Scientific Drilling Programs (ICDP) drilling project; Stein et al, ; Neugebauer et al, , Torfstein et al, ). The detailed stratigraphy and improved chronology of the Lisan Formation at the marginal terraces and deep floor of the lake allow us to establish a comprehensive integrated history of earthquake‐induced sedimentary structures (seismites) at the entire DSB during the time interval of 70–14 ka.…”

Section: Introductionmentioning

confidence: 99%

Integrated Paleoseismic Chronology of the Last Glacial Lake Lisan: From Lake Margin Seismites to Deep‐Lake Mass Transport Deposits

2018

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Seismically disturbed sedimentary sequences (seismites) in the last glacial (70–14 ka) Lisan Formation are exposed in the marginal terraces of the Dead Sea and recovered from sedimentary core drilled by the International Continental Scientific Drilling Programs at the depocenter of the lake at water depth of 300 m. The core reveals various types of centimeter‐ to meter‐scale disturbed lake sediments: turbidites, homogenites, slumps, and other deformations, interspersed with undisturbed lamination. The transported sediments comprise a main source of the thickness tripling of the Lisan Formation at the depocenter of the lake compared to the margins. Excluding (mass transport deposits MTDs) from chronology yields a normal, event‐free age‐depth model for core. Moreover, time intervals of units missing at the exposed sections of the lake margin are synchronous with intervals of mass transport deposits (MTDs) at the deepest lake floors. In the deep core, the recurrence interval range of MTD with thickness > 1 cm is ~ 100–300 years, while that of the thick MTD (>50 cm) is ~ 2,500 years, twice the recurrence interval of the seismites at the lake's margins. The ~1,000 year recurrence at the lake's margins lies within the ranges that have been calculated for ~M6.5–7 earthquakes. The significantly higher figure shown by depocenter core suggests activity on various faults and the response of the lake sediments in the entire Dead Sea basin. Overall, an unprecedented chronology of seismic activity was achieved for the late Pleistocene Lisan Formation providing a framework of earthquake activity in the vicinity of the Dead Sea basin during the period of the last high lake stand.

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Section: Introductionmentioning

confidence: 99%

Integrated Paleoseismic Chronology of the Last Glacial Lake Lisan: From Lake Margin Seismites to Deep‐Lake Mass Transport Deposits

2018

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“…The main deglacial pulse of gypsum deposition, the "Upper Gypsum Unit" (UGU, 17.1-15.5 ka; Torfstein et al, 2013a), is observed at the Masada M1 outcrop (Figure 2) where it displays a thickness of 1.07 m and δ 34 S in the range of 24. This correlation in isotopic composition between the DSDDP core and the marginal outcrop can also be observed in additional gypsum beds that have been previously correlated (Torfstein et al, 2015 The "Lower Gypsum Unit, " marking the MIS4-3 transition (61-58.5 ka) is present in almost all marginal sites along the Dead Sea, yet its correlation to the DSDDP core is more challenging because the corresponding interval is characterized by the frequent occurrence of thinner gypsum laminae.…”

Section: Resultsmentioning

confidence: 99%

“…The timing of Termination -II and -I is marked by red arrow left of the columnar section. Ages of marker layers in (b) are from Torfstein et al (2013a). Note that the Masada M1 section of the Lisan Formation, corresponds to depths of ∼177-90 mblf in the DSDDP core.…”

Section: Sulfur and Sulfate Bound Oxygenmentioning

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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“…Lisan detritus was sampled from the Masada M1 section that was recently dated by the U-Th method (Torfstein et al, 2013a(Torfstein et al, , 2013b. Detritus was taken by scraping with a scalpel in a laminar flow hood the same sediment blocks that were previously used for age measurement.…”

Section: Sampling and Analytical Methodsmentioning

confidence: 99%

“…In order to evaluate the cause of 10 Be secular variations in the Lisan Formation, the ages of the samples were calculated according to the age-depth model of the studied M1 section (Torfstein et al, 2013a(Torfstein et al, , 2013b and drawn together with the Lake level curve of Lake Lisan (Torfstein et al, 2013a(Torfstein et al, , 2013b. Fig.…”

Section: Temporal Variations Of 10 Be In the Lisan Formationmentioning

confidence: 99%

Beryllium isotopes as tracers of Lake Lisan (last Glacial Dead Sea) hydrology and the Laschamp geomagnetic excursion

Belmaker¹,

Stein²,

Beer³

et al. 2014

Earth and Planetary Science Letters

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Integrated multi-site U–Th chronology of the last glacial Lake Lisan

Cited by 79 publications

References 43 publications

Integrated Paleoseismic Chronology of the Last Glacial Lake Lisan: From Lake Margin Seismites to Deep‐Lake Mass Transport Deposits

Integrated Paleoseismic Chronology of the Last Glacial Lake Lisan: From Lake Margin Seismites to Deep‐Lake Mass Transport Deposits

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

Beryllium isotopes as tracers of Lake Lisan (last Glacial Dead Sea) hydrology and the Laschamp geomagnetic excursion

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