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Creation and destruction of lower continental crust

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Zusammenfassung

Die Gesamtzusammenfassung der Kontinentalen Kruste resultiert aus dem Massenaustausch zwischen Kruste und Mantel. Krustenzuwachs erfolgt hauptsächlich beim Aufstieg in und durch die Kruste von aus dem Mantel abstammenden Basalt an konvergierenden Plattengrenzen und zum geringeren Teil Plattenintern. Der Krustenabbau wird erreicht per Subduktion der obersten Kruste, durch subkrustale Erosion an konvergierenden Plattengrenzen (Sedimente, Elemente kontinentaler Herkunft von hydrothermal veränderter ozeanischer Kruste). Dies wird hervorgerufen von der Schichtspaltung der untersten Kruste nach der Verdichtung durch die Gabbro-Eklogit-Phasentransformation, welche in der Krusten-Mantel-Dichte-Inversion resultiert. Da die Phasentransformation nur unter hohen Drücken stattfindet, werden tektonische Mächtigkeitszunahmen der Kruste (> 50 km) benötigt. Die unterste Kruste in Bereichen von konvergierenden Kontinent-Ozean und Kontinent-Kontinent Plattengrenzen unterliegt einer größeren Wahrscheinlichkeit vorübergehende Mächtigkeitszunahmen zu erfahren als platteninterne Kruste. Dementsprechend ist die Erhaltungswahrscheinlichkeit von mafischer unterer Kruste für platteninterne Bereiche größer als für Plattengrenzen. Schichtspaltung von mafischer unterer Kruste ist der Hauptprozeß basisch zusammengesetzte Gesteine aus der Kruste zu entfernen, hierbei wird die Kruste in Richtung »andesitische« Zusammensetzung verändert. Hinweise für Schichtspaltung der unteren Kruste stammen von »geochemisch bilanzierten« Profilen aus druckhaft deformierten Zonen. Weiterhin sprechen dafür hohe La/Yb-Werte, das Fehlen von Eu-Anomalien und hohe Sr-Gehalte, wie sie an der Basis tektonisch verdickter Kruste in Magmen, die aus der tiefen Kruste stammen, gefunden werden. Diese krustalen Magmen werden häufig von Mantelbasalten begleitet, die zu Krustenhebung und Dehnung in Verbindung stehen; beides im Zusammenhang stehend zu der gleichzeitig stattfindenden Schichtspaltung der unterlagernden Mantellithosphäre.

Abstract

Bulk continental crustal composition results from the net mass exchange between crust and mantle. Crustal addition is mainly by the rise of mantle-derived melts into and through the crust at convergent plate margins and (at a lower rate) within plate interiors. Crustal subtraction occurs by subduction of uppermost crust (sediment, continent-derived elements in hydrothermally altered oceanic crust), by subcrustal erosion at convergent margins and by delamination of lowermost crust following densifying gabbro-eclogite phase transformations that result in a crust-mantle density inversion. As the phase transformations only occur at high pressure, tectonic overthickening of the crust (to > 50 km) is required. The lowermost crust at continent-ocean and continent-continent convergent plate margins is more likely to experience these transient overthickening events (compressional orogenies) than is intraplate crust. Correspondingly, the preservation probability of mafic lower crust is greater for intraplate than for plate margin localities. Delamination of mafic lower crust is the main process for removing basic composition rocks from the crust, thereby creating »andesitic« crustal composition. Evidence for lower crustal delamination comes from »geochemically balanced« cross section of compressional belts, and from the high La/Yb ratios, lack of Eu anomalies, and high Sr contents in deep crustallyderived magmas from the base of tectonically over-thickened crust. These crustal magmas are often accompanied by mantle-derived basalts associated with crustal uplift and extension, both related to the coincident delamination of underlying mantle lithosphere.

Résumé

La composition d'ensemble de la croûte continentale résulte des échanges entre la croûte et le manteau. L'apport dans la croûte provient en ordre principal de la montée de basalte d'origine mantélique qui s'opère aux bordures des plaques convergentes et, dans une moindre mesure, à l'intérieur des plaques. Le départ hors de la croûte se produit par la subduction de la croûte supérieure (sédiments, éléments dérivés des continents dans la croûte océanique affectée d'altération hydrothermale), par érosion subcrustale le long des marges convergentes et par délamination à la base de la croûte, les transformations de phase gabbro-éclogitiques entraînant une augmentation de densité et une inversion de densité entre croûte et manteau. Comme ces transformations de phases ne se produisent qu'à haute pression, elles impliquent un épaississement tectonique de la croûte (jusqu'à plus de 50 Km). Le domaine probable de tels épaississement est la partie inférieure de la croûte en bordure des plaques convergentes continentocéan ou continent-continent (orogènes de compression), plutôt que la croûte intra-plaque. Inversement, la probabilité de conversion d'une croûte inférieure mafique est plus élevée au milieu des plaques que sur leurs bordures. La délamination de la croûte inférieure est le processus courant d'appauvrissement de la croûte en roches mafiques, avec création d'une composition crustale »andésitique«. Les arguments en faveur de cette delamination sub-crustale sont tirés de profils »géochimiquement équilibrés« dans les ceintures en compression, ainsi que des rapports La/Yb élevés, de l'absence d'anomalie de l'Eu et des hautes teneurs en Sr dans les magmas dérivés de la partie profonde des croûtes tectoniquement épaissies. Ces magmas crustaux sont souvent accompagnés de basaltes d'origine mantélique associés à un soulèvement et à une extension crustale, ces deux processus étant liés à la délamination concommittante de la lithosphère mantélique sousjacente.

Краткое содержание

Общий состав материк овой коры есть резуль тат обмена массами между Земной корой и мантией. Утолщение ко ры наблюдается гл. обр. при поднятии база льтов мантии в кору, которое идет по грани цам сближающихся пли т и значительно реже че рез породы самих плит. Утончение коры проис ходит при засасывани и верхней ее части, при э розии сходящихся гра ниц плит (отложения, элеме нты материкового происхождения, но гид ротермально изменен ной океанической коры). Эт о вызывается расщеплением нижней части коры после упло тнения в результате преобра зования габброэклог итовых фаз. Этот последний пр оцесс развивается только п ри особенно высоком удавлении, а это давле ние появляется при тектоническом утолщении мощности к оры (более 50км). В нижней части кор ы в регионе границ сходящихся материко вых (океанических и ма териковых) материковых плит про исходит, по всей вероятности, вре менное значительное утолщение мощности этих плитбо лыпее, чем таковое центриальных регион ов плит. Причем мафическая нижняя ча сть коры в центральны х регионах сохраняетс я лучше, чем на граница х плит. Расщепление сло ев мафической нижней части коры является о сновным процессом, удаляющим из нее поро ды базического соста ва, что приводит к измене нию этой части коры в сторону »андезитно го« состава. Указания на расщепление слоев нижней части коры наблюдают из геохими чески сбалансирован ных профилей зон, деформи рованных под воздействием давлен ия. Кроме того, высокое значение соотношения лантала /итербия, отсутствие аномалий европия и высокое сод ержание стронция, установлен ное в магме у базиса тектонически утолщенной Земной коры, которое, вероятн о пришло из глубинных слоев, говорят о справ едливости сказанног о. Эти магмы коры часто с опровождаются базал ьтовыми магмами, связанными с поднятиеми и расширениями. Оба на званных процесса в свою очередь развива ются одновременно с расщеплением глубин ных слоев подлежащей литосферы мантии.

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  1. S. Mahlburg-Kay

    Present address: INSTOC, Snee Hall, Cornell University, 14853, Ithaca, NY, USA

Authors and Affiliations

  1. Department of Geological Sciences and INSTOC, Cornell University, Snee Hall, 14853, Ithaca, NY, USA

    R. W. Kay

  2. Lab. de Geoch. et Cosmoch., IPG Paris, France

    R. W. Kay

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  1. R. W. Kay
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  2. S. Mahlburg-Kay
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Kay, R.W., Mahlburg-Kay, S. Creation and destruction of lower continental crust. Geol Rundsch 80, 259–278 (1991). https://doi.org/10.1007/BF01829365

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