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Deep-sea carbonates: Reading the carbon-isotope signal

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Zusammenfassung

Das Kohlenstoff-Isotopensignal in den Tiefseesedimenten spiegelt ein Zusammenspiel wider, das (1) von den globalen Austauschraten des ozeanischen Kohlenstoffreservoirs mit der Biosphäre, den Böden und den Sedimenten gesteuert wird, (2) in dem ein globaler und regionaler Wechsel in der Produktivität des Oberflächenwassers und (3) interne Veränderungen in der Wassermassen-Struktur und -Zirkulation (Becken-zu-Becken-Fraktionierung, Sauerstoffminimumentwicklung) zum Ausdruck kommen, und (4) in dem eine spezifische Fraktionierung hervorgerufen durch die Milieuänderung im Lebensraum der Organismen und/oder ontogenetische Fraktionierung (»Vitaleffekte«) erscheint. Zusätzliche Komplikationen entstehen aus unterschiedlichen Erhaltungsmöglichkeiten. Es ist unmöglich, alle diese verschiedenen Faktoren vollständig zu isolieren. Als Faustregel kann man annehmen, daß langpenodische Signale, die parallel mit Plankton- und Benthosentwicklungen verlaufen, externe globale Fraktionierungstrends widerspiegeln, während kurzzeitige Signale eher an interne Muster gebunden sind (Fraktionierung innerhalb der Wassermassen). Die verschiedenen Möglichkeiten der Interpretation werden an speziellen Fällen diskutiert: am Übergang Pleistozän zu Holozän, an der Veränderung des Kohlenstoffverhältnisses im Messinium und an dem Monerey-Maximum im Miozän.

Abstract

The carbon isotope signal in deep-sea sediments reflects a mix of (1) global changes in the rates of exchange of the ocean's carbon reservoir with biosphere, soil, and sediments, (2) global and regional changes in surface water productivity, (3) internal shifts in water-mass structure and circulation (basin-basin fractionation, oxygen minimum development), and (4) organism-specific fractionation effects due to changes in micro-habitat and/or ontogenic fractionation (»vital effects«). Additional complications arise from differential preservation. It is impossible to entirely isolate these various factors. As a rule of thumb, long period signals that are parallel for planktonic and benthic data reflect external (global) fractionation patterns, whilst short-period signals are more likely tied to internal patterns (water-mass fractionation). The various approaches to interpretation are illustrated with three case studies: the Glacial-Holocene transition, the Messinian Carbon Shift, and the Miocene Monterey Excursion.

Résumé

Le signal isotopique du carbone enregistré dans les sédiments océaniques résulte d'un ensemble de mécanismes qui reflètent: 1) les variations globales dans l'intensité des échanges entre le réservoir du carbone de l'océan et la biosphère, les sols et les sédiments, 2) les variations globales et régionales de productivité des eaux de surface, 3) les changements dans la structure et la circulation des masses d'eaux (fractionnement de bassin à bassin, développement d'un niveau à minimum d'oxygène), et 4) les effets de fractionnement propres aux organismes, dûs à des changements de micro-habitat et/ou à un fractionnement au cours de l'ontogénie (»effet vital«). La préservation différentielle ajoute certaines difficultés d'interprétation. Il n'est pas possible d'isoler entièrement chacun de ces différents facteurs. D'une manière générale les signaux à longue période dont les variations sont parallèles pour les données planctoniques et benthiques correspondent à un fractionnement dû à des facteurs externes (globaux), alors que les signaux à courte période sont plus vraisemblablement liés à des facteurs internes (fractionnement des masses d'eaux). Trois cas étudiés permettent d'illustrer ces différents types d'interprétation: la transition Glaciaire/Holocène, le »décrochement Messinien« et l'»enrichissement de Monterey« au Miocène.

Краткое содержание

Соотношения изотопо в углерода в глубоков одных океанических отложе ниях отображают взаимодействие, кото рое: 1) регулируется гло бальным обменом океаническо го резервуара углеро да с биосферой, дном водо емов и их седиментами; 2) выражается глобальн ой и региональной сме ной продуктивности пове рхностных вод, а также 3) изменениями в структуре и циркуля ции водных масс (фракционирование в з ависимости от бассей на к бассейну, минимальное образов ание кислорода) и 4) проявляется специфи ческим фракциониров анием, вызванным изменения ми окружающей среды в жизненном пространстве органи змов и/или онтогенети ческим фракционированием э тих изотопов — “жизне нный эффект”. Трудности пр едоставляет различн ая степень сохранности исходного состава из отопов. Разделить все эти фак торы полностью не уда ется; как правило, можно гов орить о том, что соотно шение изотопов в глобально м масштабе, протекающ ее параллельно с развит ием планктона и бенто са, отображают внешние г лобальные тенденции фракционирования, в т о время, как локальные связаны скорее всего с местны м фракционированием в водных массах. Дискут ируется возможность различной интерпретации отдел ьных частных случаев: например, на рубеже плейстоцен а и голоцена; а также изменение соотношен ия стабильных изотоп ов в мессинском веке и эфф ект Монтери в миоцено вых отложениях.

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  1. W. H. Berger

    Present address: Scripps Institution of Oceanography, University of California, San Diego

  2. E. Vincent

    Present address: Département de Géologie Dynamique, Université Pierre et Marie Curie, Paris

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    E. Vincent

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Berger, W.H., Vincent, E. Deep-sea carbonates: Reading the carbon-isotope signal. Geol Rundsch 75, 249–269 (1986). https://doi.org/10.1007/BF01770192

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