Zusammenfassung
Sedimentäre »Formations«, die im westlichen Nord-Atlantik durchJansa et al. (1979) aufgestellt wurden, sowie deren Äquivalente im östlichen Nord-Atlantik wurden röntgenographisch auf ihre Mineralzusammensetzung hin untersucht; es werden die Ergebnisse semiquantitativer Diffraktometer-Analysen von über 1000 Proben verschiedener Fahrtab-schnitte des Deep Sea Drilling Projects vorgestellt. Die Ergebnisse der einzelnen Bohrungen werden in Form von Diagrammen von etwa 35 verschiedenen Mineralphasen dargestellt.
Aus dem westlichen Nord-Atlantik wurden die Bohrlokationen 105, 106, 386, 387, 391, 417 und 418, aus dem östlichen Nord-Atlantik die Bohrlokationen 367, 369, 370, 415 und 416 untersucht. Für die meisten »Formations« ließen sich charakteristische Mineralspektren ermitteln, so daß diese dadurch auch zusätzlich gekennzeichnet werden können. Die Änderungen an den »Formations«-Grenzen sind in den meisten Fällen scharf, in einigen Fällen bestehen aber auch gleitende Übergänge. Lokale Variationen im Mineralspektrum einer »Formation« lassen sich meist mit der Entfernung vom Liefergebiet erklären.
Das Gesamtprofil der Sedimente im westlichen Nord-Atlantik reicht vom Oxfordium bis ins Quartär. Es besteht aus: tonigen Kalksteinen (Cat Gap Formation) Kalksteinen (Blake-Bahama Formation); Tonsteinen und Shales (Hatteras Formation); zeolithischen Tonsteinen (Plantagenet Formation); Nanno-Mergeln (Crescent Peaks Member); Kieselschlammen, Tonen und Hornsteinen (Bermuda Rise Formation) und hemipelagischen Schlammen (Blake Ridge Formation); mit lokal umgelagerten Flachwasserkarbonaten (Great Abaco Member).
Ein entsprechendes Profil im östlichen Nord-Atlantik ist nur an der Bohrlokation 367 entwickelt, wo auch entsprechende Mineralspektren gefunden wurden. Bei den Bohrlokationen 369, 370, 415 und 416 werden die Sedimentfolgen durch bedeutende Zufuhr von terrigenem Detritus bestimmt: Turbidite alternieren mit pelagischen Sedimenten. Das wird auch in den Mineralspektren deutlich, aber es ist nicht möglich, dem westlichen Nordatlantik entsprechende »Formationen« daraus abzuleiten.
Seismische Reflektoren, die sich über weite Areale im westlichen Nordatlantik verfolgen lassen, wurden an den lithologischen Sequenzen der Bohrungen geeicht (Tucholke 1979). Sie sind in den meisten Fällen auf lithologische Wechsel und Änderungen im Mineralspektrum zurückzuführen und markieren so auch oft »Formations«-Grenzen. Daneben können Impedanz-Unterschiede aber auch durch Korngrößenänderungen, Diagenese oder Erosionsdiskordanzen bedingt sein, wie das bereitsTucholke (1979) gezeigt hat.
Abstract
Sedimentary formations established in the western North Atlantic basin byJansa et al. (1979) and their coeval counterparts from the eastern North Atlantic were studied for their mineral composition using X-ray powder diffractometry. More than thousand samples from different legs of the Deep Sea Drilling Project were analysed semiquantitatively. The results are presented as diagrams of about thirty five different mineral phases versus depth/stratigraphy in the single boreholes. Sites 105, 106, 386, 387, 391, 417, and 418 were studied from the western North Atlantic, and Sites 367, 369, 370, 415, and 416 from the eastern North Atlantic off W-Africa. Specific mineral spectra were found from most of the formations which can thus be additionally characterized. The change of mineral composition along the formation boundaries is in most cases sharp but along some of the boundaries it is transitional. Local variations of mineral spectra within the same formation can mainly be referred to distance from source areas.
The sedimentary section studied from the western North Atlantic basin ranges in age from Oxfordian to Quaternary. It consists of: argillaceous limestones (Cat Gap Formation); limestones (Blake-Bahama Formation); claystones and shales (Hatteras Formation); zeolitic claystones (Plantagenet Formation); nanno-marls (Crescent Peaks Member); siliceous oozes, clays, and cherts (Bermuda Rise Formation), and hemipelagic muds (Blake Ridge Formation) with locally redeposited shallow-water carbonates (Great Abaco Member).
A corresponding section in the eastern North Atlantic is only developed at Site 367 where similar mineral assemblages could be found. At Sites 369, 370, 415, and 416 the sediment sequence is dominated by turbiditic influx of terrigenous components alternating with pelagic sediments; this can clearly be depicted from the mineral suites but it is not possible to establish sedimentary formations which can be paralleled to those within the western North Atlantic.
Seismically mappable reflectors which were calibrated at the sediment sequence of the drillsites, are in most cases related to lithological changes and mineral composition. These acoustic horizons are very often coincident with formation boundaries. Besides different mineral composition, changes in grain size and diagenesis but also erosional unconformities are responsible for the impedance contrasts leading to the reflectors as already pointed out byTucholke (1979).
Résumé
Les «formations» sédimentaires décrites parJansa et al. (1979) dans la partie ouest de l'Atlantique Nord ainsi que leurs correspondants dans la partie est de l'Atlantique Nord ont été étudiées par analyse diffractométrique afin de déterminer leur composition minéralogique. Plus de 1000 échantillons de divers «legs» du Deep Sea Drilling Project ont fait l'objet d'une analyse semiquantitative. Les résultats sont présentés sous forme de diagrammes concernant environ 35 minéraux pour chaque sondage. Ont été étudiés: dans le nord-ouest de l'Atlantique, les sites 105, 106, 386, 387, 391, 417 et 418, et dans le nord-est de l'Atlantique les sites 367, 369, 370, 415 et 416.
La plupart des «formations» peuvent être caractérisées par des spectres typiques de minéraux. Ces spectres changent d'ordinaire de manière brusque d'une formation à l'autre mais il existe aussi des changements progressifs. Des variations locales des spectres de minéraux au sein d'une même «formation» peuvent être expliquées par l'éloignement plus ou moins grand des sources terrigènes. Les sections sédimentaires étudiées s'étendent stratigraphiquement de l'Oxfordien jusqu'au Quaternaire. Il s'agit, de bas en haut:
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de calcaires argileux (Cat Gap Formation);
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de calcaires (Blake-Bahama Formation);
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d'argilites et de shales (Hatteras Formation);
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d'argilites zéolitiques (Plantagenet Formation);
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de marnes à nannofossiles (Crescent Peaks Member);
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de boues siliceuses, d'argiles et de silex (Bermuda Rise Formation);
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ainsi que de boues hémipélagiques (Blake Ridge Formation) contenant par endroits des carbonates remaniés provenant d'un milieu peu profond (Great Abaco Member).
Dans l'est de l'Atlantique Nord, seul le site 367 présente un profil correspondant, avec mêmes assemblages minéraux. Les profils des sites 369, 370, 415 et 416 sont dominés par des turbidites terrigènes alternant avec des sédiments pélagiques, ce qui ressort clairement des associations minérales. Il n'est pas possible dans ces profils de définir des formations corrélables à celles du nord-ouest de l'Atlantique. Des réflecteurs sismiques, que l'on peut suivre sur de grandes étendues sont, dans la plupart des cas, en relation avec des changements de lithologie et, par conséquent, des changements de composition minéralogique. Souvent, ces réflecteurs sismiques coïncident avec les frontières entre les «formations». Ainsi, les changements d'impédance peuvent être causés par les changements de granulométrie, de diagenèse ou par des surfaces d'érosion comme l'avait déjà notéTucholke (1979).
Краткое содержание
Провели рентгеногор афические исследова ния осадочных «формаций», которы ус тановили Jansa и др. в 1979 году в западной част и северной Атлантики, и их эквивалентов в восто чной части ее на минералогический состав. Приводятся ре зультаты полуколиче ственного анализа более, чем 1000 пр об, взятых из различны х участков, обрабатыва емых в рамках проэкта DSDP. На диаграммах предс тавлены примерно 35 раз личных минералогических фа з из отдельных буровы х скважин.
В западной части севе рной Атлантики иссле довали буровые скважины 105, 106, 386, 387, 391, 417 и 418, а в восточной - 367, 369, 370, 414, и 416. Для б ольшинства «формаций» удалось у становить характерн ые скопления минералов (спектр минералов), что явилось дополнительной инфо рмацией. Границы «фор маций» в большинстве случае в резко разделяются; плавные переходы отм ечаются только в отде льных случаях. Локальные ко лебания в этих скопле ниях минералов в случае одной формац ии можно объяснить отдаленностью ее от о бласти сноса. Общий профиль седиме нтов в западной части северной Атлантики охватывае т период от оксфордск ого века до четвертичног о периода включитель но. Он состоит из: глинистых известняк ов (формация Cat Gap); известняков (формаци я Blake-Bahama); нерасслоенного глин истого сланца и сланц ев (формация Hatteras); цеолитовых нерассло енных глинистых слан цев (формация Plantagenet); нанно-мергелей (форма цияСrescent Peaks); кремнистого ила, глин и роговика (формация Bermuda Rise); полупелагических ил ов (формация Blake Ridge); с локально переотлож енными карбонатами м елководья. (Great Abaco Member): Соответствующий про филь в восточной част и северной Атлантики находится только в буровой сква жине 367, где установлен и соо тветствующий спектр минералов. Осадочные свиты буро вых скважин 369, 370, 415 и 416 отличаются значит ельным приносом терр игенного детрита. Турбидиты че редуются с пелагичес кими седиментами. Это особ енно ясно выражено в спектре минералов, но установить «формаци и», соответствующие таковым западной час ти северной Атлантики, не удалось.
Сейсмическую отража тельную способнасть седиментов западной части север ной Атлантики связал и с литологическими хар актеристиками буров ых скважин (Tucholke, 1979). Она отображает в бо лыпенстве случаев изменения литологич еского состава и, след овательно, изменения спектра ми нералов, а также отмеч ает границы «формаций». К роме того, как указыва ет Tucholke, (1979), различия импендан ца, т.е. полного (кажущегося) сопротив ления, могут быть вызв аны изменениями грануло метрического состав а, процессами диагенеза, или появле ниями несогласий во в ремя эрозии.
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Rothe, P. Mineral composition of sedimentary formations in the North Atlantic Ocean. Geol Rundsch 78, 903–942 (1989). https://doi.org/10.1007/BF01829329
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DOI: https://doi.org/10.1007/BF01829329