Holocene and late glacial palaeoceanography and palaeolimnology of the Black Sea: Changing sediment provenance and basin hydrography over the past 20,000years

Piper, David Z.; Calvert, S. E.

doi:10.1016/j.gca.2011.07.016

Cited by 34 publications

(21 citation statements)

References 116 publications

(184 reference statements)

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“…The REE in surface sediments of the Black Sea [65] support the results of the mineralogy studies. Surface sediments recovered in box cores from the western basin margin have a flat REE curve that is representative of the largely felsic rocks of eastern Europe, whereas surface sediments from the southern basin margin have a light REE depletion that reflects a moderate mafic-rock contribution from the ultramafic rocks of the Pontic Mountains in northern Anatolia.…”

Section: Lithogenous Sediment Fractionsupporting

confidence: 78%

“…Aluminum serves as a proxy for the lithogenous fraction [63,64]. Examples of trace elements also hosted predominantly by this fraction include the alkali metals, heavy-mineral hosted trace elements, plus Nb, Ga, Sc, Ta as evidenced by their linear correlations with Al that extrapolate essentially to the origin [65]. Their relationship with Al adds support to the use of Al alone as a proxy for this sediment fraction.…”

Section: Marine Sediment Factionmentioning

confidence: 90%

“…Modeling and leaching analyses of Quaternary pelagic sediments from the central Pacific Ocean reveal that the siliciclastic fraction of these sediments similarly has a flat WSA-normalized curve [14]. The relationship between the REE composition of sediments and their terrigenous sources is further recorded by the sediments that are accumulating under the strongly negative redox condition of the Black Sea [65]. Two major terrigenous sources of significantly different composition were identified initially by the clay mineralogy of the surface sediments [74].…”

Section: Lithogenous Sediment Fractionmentioning

confidence: 99%

“…Within sediment cores recovered from the abyssal region of the basin, the curves change abruptly every few 10 s of centimeters (Figure 8), or ca 2000 to 3000 yrs [65], from the one type of curve to the other. The shift of the curves reflects a shift in the dominance of the northern and western source versus the southern and eastern source that was likely driven by regional changes of climate since the LGM [77].…”

Section: Lithogenous Sediment Fractionmentioning

confidence: 99%

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Normalized Rare Earth Elements in Water, Sediments, and Wine: Identifying Sources and Environmental Redox Conditions

Piper¹,

Bau²

2013

AJAC

155

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The concentrations of the rare earth elements (REE) in surface waters and sediments, when normalized on an elementby-element basis to one of several rock standards and plotted versus atomic number, yield curves that reveal their partitioning between different sediment fractions and the sources of those fractions, for example, between terrestrial-derived lithogenous debris and seawater-derived biogenous detritus and hydrogenous metal oxides. The REE of ancient sediments support their partitioning into these same fractions and further contribute to the identification of the redox geochemistry of the sea water in which the sediments accumulated. The normalized curves of the REE that have been examined in several South American wine varietals can be interpreted to reflect the lithology of the bedrock on which the vines may have been grown, suggesting limited fractionation during soil development.

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Section: Lithogenous Sediment Fractionsupporting

confidence: 78%

Section: Marine Sediment Factionmentioning

confidence: 90%

Section: Lithogenous Sediment Fractionmentioning

confidence: 99%

Section: Lithogenous Sediment Fractionmentioning

confidence: 99%

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Normalized Rare Earth Elements in Water, Sediments, and Wine: Identifying Sources and Environmental Redox Conditions

Piper¹,

Bau²

2013

AJAC

155

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“…Although Re concentrations of less than 5.0 ppb may occur in some Archean ORM deposited beneath a fully anoxic atmosphere and oceans, only a minority of Archean samples had sufficiently low Re concentrations to be excluded from the compilation. We also note that Re concentrations in Unit I and II sediments of the restricted Black Sea are significantly above this threshold ($20-76 ppb; Ravizza et al, 1991;Crusius et al, 1996;Piper and Calvert, 2011); the filter therefore does not exclude Black Sea-type restricted basins from the compilation. As Re burial is independent of sulfide (H 2 S) availability, no filter for euxinia is required as in the case for Mo.…”

Section: Methodsmentioning

confidence: 98%

A model for the oceanic mass balance of rhenium and implications for the extent of Proterozoic ocean anoxia

Sheen

Kendall

Reinhard

et al. 2018

Geochimica et Cosmochimica Acta

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Emerging geochemical evidence suggests that the atmosphere-ocean system underwent a significant decrease in O 2 content following the Great Oxidation Event (GOE), leading to a mid-Proterozoic ocean (ca. 2.0-0.8 Ga) with oxygenated surface waters and predominantly anoxic deep waters. The extent of mid-Proterozoic seafloor anoxia has been recently estimated using mass-balance models based on molybdenum (Mo), uranium (U), and chromium (Cr) enrichments in organic-rich mudrocks (ORM). Here, we use a temporal compilation of concentrations for the redox-sensitive trace metal rhenium (Re) in ORM to provide an independent constraint on the global extent of mid-Proterozoic ocean anoxia and as a tool for more generally exploring how the marine geochemical cycle of Re has changed through time. The compilation reveals that mid-Proterozoic ORM are dominated by low Re concentrations that overall are only mildly higher than those of Archean ORM and significantly lower than many ORM deposited during the ca. 2.22-2.06 Ga Lomagundi Event and during the Phanerozoic Eon. These temporal trends are consistent with a decrease in the oceanic Re inventory in response to an expansion of anoxia after an interval of increased oxygenation during the Lomagundi Event. Mass-balance modeling of the marine Re geochemical cycle indicates that the mid-Proterozoic ORM with low Re enrichments are consistent with extensive seafloor anoxia. Beyond this agreement, these new data bring added value because Re, like the other metals, responds generally to lowoxygen conditions but has its own distinct sensitivity to the varying environmental controls. Thus, we can broaden our capacity to infer nuanced spatiotemporal patterns in ancient redox landscapes. For example, despite the still small number of data, some mid-Proterozoic ORM units have higher Re enrichments that may reflect a larger oceanic Re inventory during transient episodes of ocean oxygenation. An improved understanding of the modern oceanic Re cycle and a higher temporal resolution for the Re compilation will enable further tests of these hypotheses regarding changes in the surficial Re geochemical cycle in response to variations in atmosphere-ocean oxygenation. Nevertheless, the existing Re compilation and model results are in agreement with previous Cr, Mo, and U evidence for pervasively anoxic and ferruginous conditions in mid-Proterozoic oceans.

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Geochemistry of the Black Sea during the last 15 kyr: A protracted evolution of its hydrography and ecology

Piper

2016

Paleoceanography

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The Black Sea is a 2200 m deep anoxic, marine sea connected to the Mediterranean Sea via the Dardanelles Strait, Marmara Sea, and the 3 km wide, 35 m deep Bosphorus Strait. The biogeochemistry of sediment from the Anatolia slope has recorded changes to the hydrography leading up to and following the input of Mediterranean water at ~9.4 ka (103 years B.P.), when global sea level rose to the level of the Bosphorus sill and high‐salinity water from the Mediterranean began to spill into the then brackish lake. The water initially mixed little with the lake water but cascaded to the bottom where it remained essentially isolated for ~1.6 kyr, the time required to fill the basin from the bottom up at its present input rate. The accumulation of Mo in the seafloor sediments, a proxy of bottom‐water anoxia, increased sharply at ~8.6 ka, when bacterial respiration in the bottom water advanced to SO42− reduction by the oxidation of organic detritus that settled out of the photic zone. Its accumulation remained elevated to ~5.6 ka, when it decreased 60%, only to again increase slightly at ~2.0 ka. The accumulation of Corg, a proxy of primary productivity, increased threefold to fourfold at ~7.8 ka, when upward mixing of the high‐salinity bottom water replaced the then thin veneer of the brackish photic zone in less than 50 years. From that time onward, the accumulation of Corg, Mo, and additional trace metals has reflected the hydrography of the basin and Bosphorus Strait, controlled largely by climate.

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Holocene and late glacial palaeoceanography and palaeolimnology of the Black Sea: Changing sediment provenance and basin hydrography over the past 20,000years

Cited by 34 publications

References 116 publications

Normalized Rare Earth Elements in Water, Sediments, and Wine: Identifying Sources and Environmental Redox Conditions

Normalized Rare Earth Elements in Water, Sediments, and Wine: Identifying Sources and Environmental Redox Conditions

A model for the oceanic mass balance of rhenium and implications for the extent of Proterozoic ocean anoxia

Geochemistry of the Black Sea during the last 15 kyr: A protracted evolution of its hydrography and ecology

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