Geochemical constraints on the petrogenesis of diamond facies pyroxenites from the Beni Bousera Peridotite Massif, North Morocco

D. G. Pearson, G. R. Davies, P. H. Nixon

Research output: Contribution to JournalArticleAcademicpeer-review

Abstract

The petrogenesis of pyroxenite layers within the Beni Bousera peridotite massif is investigated by means of elemental and Nd-Sr-Pb-O-S isotope analyses. The light rare earth element (LREE) depleted nature of many of the pyroxenites, their wide variation in composition, and lack of correlation between incompatible elements and fractionation indices preclude them from representing crystallized melts from a peridotitic source. The physical characteristics of the pyroxenites and their large (greater than a factor of 20) range in Ni rule out partial melting as the cause of their petrological and geochemical diversity. Major and compatible trace element geochemistry is consistent with formation of most of the pyroxenite suite via high-pressure crystal segregation in magma conduits intruding the peridotites. These magmas crystallized clinopyroxene, orthopyroxene, and garnet. The pressure of crystallization is constrained to be above ̃45 kbar from the presence of graphitized diamonds in pyroxenite layers. Lack of correlation between fractionation indices and highly incompatible elements and the wide variation in incompatible element abundances suggest that the suite did not form from genetically related magmas. The presence of positive and negative Eu anomalies (Eu/Eu* = 0{dot operator}54-2{dot operator}0) in pyroxenites which crystallized at pressures much greater than the plagioclase stability field (̃ 45 kbar) suggests that the parental magmas originated from precursors which formed in the crust. Oxygen isotope compositions of coexisting minerals in the pyroxenites indicate high-temperature equilibration but δ18O values vary from +4{dot operator}9 to + 9{dot operator}3‰, ruling out their derivation from the host peridotites or other normal mantle sources. The extreme O-isotope variation, together with δ34S values of up to + 13‰ in sulphides included within CPX strongly suggests that the melts from which the pyroxenites crystallized were derived from hydrothermally altered, subducted oceanic lithosphere. Extreme initial radiogenic isotope variation in the pyroxenites (εNd + 26 to -9,87Sr/86Sr 0{dot operator}7025-0{dot operator}7110, 206Pb/204Pb 18{dot operator}21-19{dot operator}90) support such an origin but also require a component with ancient, high U/Pb and Th/Pb in their source to explain the high Δ7/4 and Δ8/4 values of some pyroxenites. This component may be subducted hemi-pelagic sediment. Further evidence for a sediment component in the pyroxenites is provided by isotopically light carbon in the graphite pyroxenites (δ13C-16 to - 28‰). Parentdaughter isotopes in the pyroxenites are strongly decoupled, making estimation of formation ages speculative. The decoupling occurred recently (<200 Ma), probably as a result of partial melting associated with diapiric upwelling and emplacement of the massif into the crust from the diamond stability field. This late partial melting event further depleted the pyroxenites in incompatible elements. The variably altered nature of the subducted protolith and complex history of trace element fractionation of the pyroxenites has largely obscured geochemical mixing trends. However, Nd-Pb isotope systematics indicate that incorporation of the component with high U/Pb-Th/Pb occurred relatively recently (<200 Ma) for some pyroxenites. Other pyroxenites do not show evidence for incorporation of such a component and may be substantially older. Tectonic, geophysical, and isotopic constraints indicate formation of the pyroxenites in the mantle wedge above a subducting slab during the Cretaceous. Physical and chemical evidence for high-pressure fractionation seen in most of the pyroxenites precludes them from simply representing ancient subducted oceanic lithosphere, thinned by diffusion. However, the petrological and isotopic diversity of the massif support the concept of a 'marble cake' mantle capable of producing the observed geochemical diversity seen in oceanic magmas.

Original languageEnglish
Pages (from-to)125-172
Number of pages48
JournalJournal of Petrology
Volume34
Issue number1
DOIs
Publication statusPublished - 1 Feb 1993

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Morocco
petrogenesis
Diamond
peridotite
Isotopes
diamond
Fractionation
diamonds
isotope
pyroxenite
operators
fractionation
partial melting
Melting
isotopes
Trace Elements
oceanic lithosphere
Sediments
Oxygen Isotopes
Earth mantle

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@article{59cd13f4844a42a1b19ea95967a2fc47,
title = "Geochemical constraints on the petrogenesis of diamond facies pyroxenites from the Beni Bousera Peridotite Massif, North Morocco",
abstract = "The petrogenesis of pyroxenite layers within the Beni Bousera peridotite massif is investigated by means of elemental and Nd-Sr-Pb-O-S isotope analyses. The light rare earth element (LREE) depleted nature of many of the pyroxenites, their wide variation in composition, and lack of correlation between incompatible elements and fractionation indices preclude them from representing crystallized melts from a peridotitic source. The physical characteristics of the pyroxenites and their large (greater than a factor of 20) range in Ni rule out partial melting as the cause of their petrological and geochemical diversity. Major and compatible trace element geochemistry is consistent with formation of most of the pyroxenite suite via high-pressure crystal segregation in magma conduits intruding the peridotites. These magmas crystallized clinopyroxene, orthopyroxene, and garnet. The pressure of crystallization is constrained to be above ̃45 kbar from the presence of graphitized diamonds in pyroxenite layers. Lack of correlation between fractionation indices and highly incompatible elements and the wide variation in incompatible element abundances suggest that the suite did not form from genetically related magmas. The presence of positive and negative Eu anomalies (Eu/Eu* = 0{dot operator}54-2{dot operator}0) in pyroxenites which crystallized at pressures much greater than the plagioclase stability field (̃ 45 kbar) suggests that the parental magmas originated from precursors which formed in the crust. Oxygen isotope compositions of coexisting minerals in the pyroxenites indicate high-temperature equilibration but δ18O values vary from +4{dot operator}9 to + 9{dot operator}3‰, ruling out their derivation from the host peridotites or other normal mantle sources. The extreme O-isotope variation, together with δ34S values of up to + 13‰ in sulphides included within CPX strongly suggests that the melts from which the pyroxenites crystallized were derived from hydrothermally altered, subducted oceanic lithosphere. Extreme initial radiogenic isotope variation in the pyroxenites (εNd + 26 to -9,87Sr/86Sr 0{dot operator}7025-0{dot operator}7110, 206Pb/204Pb 18{dot operator}21-19{dot operator}90) support such an origin but also require a component with ancient, high U/Pb and Th/Pb in their source to explain the high Δ7/4 and Δ8/4 values of some pyroxenites. This component may be subducted hemi-pelagic sediment. Further evidence for a sediment component in the pyroxenites is provided by isotopically light carbon in the graphite pyroxenites (δ13C-16 to - 28‰). Parentdaughter isotopes in the pyroxenites are strongly decoupled, making estimation of formation ages speculative. The decoupling occurred recently (<200 Ma), probably as a result of partial melting associated with diapiric upwelling and emplacement of the massif into the crust from the diamond stability field. This late partial melting event further depleted the pyroxenites in incompatible elements. The variably altered nature of the subducted protolith and complex history of trace element fractionation of the pyroxenites has largely obscured geochemical mixing trends. However, Nd-Pb isotope systematics indicate that incorporation of the component with high U/Pb-Th/Pb occurred relatively recently (<200 Ma) for some pyroxenites. Other pyroxenites do not show evidence for incorporation of such a component and may be substantially older. Tectonic, geophysical, and isotopic constraints indicate formation of the pyroxenites in the mantle wedge above a subducting slab during the Cretaceous. Physical and chemical evidence for high-pressure fractionation seen in most of the pyroxenites precludes them from simply representing ancient subducted oceanic lithosphere, thinned by diffusion. However, the petrological and isotopic diversity of the massif support the concept of a 'marble cake' mantle capable of producing the observed geochemical diversity seen in oceanic magmas.",
author = "Pearson, {D. G.} and Davies, {G. R.} and Nixon, {P. H.}",
year = "1993",
month = "2",
day = "1",
doi = "10.1093/petrology/34.1.125",
language = "English",
volume = "34",
pages = "125--172",
journal = "Journal of Petrology",
issn = "0022-3530",
publisher = "Oxford University Press",
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}

Geochemical constraints on the petrogenesis of diamond facies pyroxenites from the Beni Bousera Peridotite Massif, North Morocco. / Pearson, D. G.; Davies, G. R.; Nixon, P. H.

In: Journal of Petrology, Vol. 34, No. 1, 01.02.1993, p. 125-172.

Research output: Contribution to JournalArticleAcademicpeer-review

TY - JOUR

T1 - Geochemical constraints on the petrogenesis of diamond facies pyroxenites from the Beni Bousera Peridotite Massif, North Morocco

AU - Pearson, D. G.

AU - Davies, G. R.

AU - Nixon, P. H.

PY - 1993/2/1

Y1 - 1993/2/1

N2 - The petrogenesis of pyroxenite layers within the Beni Bousera peridotite massif is investigated by means of elemental and Nd-Sr-Pb-O-S isotope analyses. The light rare earth element (LREE) depleted nature of many of the pyroxenites, their wide variation in composition, and lack of correlation between incompatible elements and fractionation indices preclude them from representing crystallized melts from a peridotitic source. The physical characteristics of the pyroxenites and their large (greater than a factor of 20) range in Ni rule out partial melting as the cause of their petrological and geochemical diversity. Major and compatible trace element geochemistry is consistent with formation of most of the pyroxenite suite via high-pressure crystal segregation in magma conduits intruding the peridotites. These magmas crystallized clinopyroxene, orthopyroxene, and garnet. The pressure of crystallization is constrained to be above ̃45 kbar from the presence of graphitized diamonds in pyroxenite layers. Lack of correlation between fractionation indices and highly incompatible elements and the wide variation in incompatible element abundances suggest that the suite did not form from genetically related magmas. The presence of positive and negative Eu anomalies (Eu/Eu* = 0{dot operator}54-2{dot operator}0) in pyroxenites which crystallized at pressures much greater than the plagioclase stability field (̃ 45 kbar) suggests that the parental magmas originated from precursors which formed in the crust. Oxygen isotope compositions of coexisting minerals in the pyroxenites indicate high-temperature equilibration but δ18O values vary from +4{dot operator}9 to + 9{dot operator}3‰, ruling out their derivation from the host peridotites or other normal mantle sources. The extreme O-isotope variation, together with δ34S values of up to + 13‰ in sulphides included within CPX strongly suggests that the melts from which the pyroxenites crystallized were derived from hydrothermally altered, subducted oceanic lithosphere. Extreme initial radiogenic isotope variation in the pyroxenites (εNd + 26 to -9,87Sr/86Sr 0{dot operator}7025-0{dot operator}7110, 206Pb/204Pb 18{dot operator}21-19{dot operator}90) support such an origin but also require a component with ancient, high U/Pb and Th/Pb in their source to explain the high Δ7/4 and Δ8/4 values of some pyroxenites. This component may be subducted hemi-pelagic sediment. Further evidence for a sediment component in the pyroxenites is provided by isotopically light carbon in the graphite pyroxenites (δ13C-16 to - 28‰). Parentdaughter isotopes in the pyroxenites are strongly decoupled, making estimation of formation ages speculative. The decoupling occurred recently (<200 Ma), probably as a result of partial melting associated with diapiric upwelling and emplacement of the massif into the crust from the diamond stability field. This late partial melting event further depleted the pyroxenites in incompatible elements. The variably altered nature of the subducted protolith and complex history of trace element fractionation of the pyroxenites has largely obscured geochemical mixing trends. However, Nd-Pb isotope systematics indicate that incorporation of the component with high U/Pb-Th/Pb occurred relatively recently (<200 Ma) for some pyroxenites. Other pyroxenites do not show evidence for incorporation of such a component and may be substantially older. Tectonic, geophysical, and isotopic constraints indicate formation of the pyroxenites in the mantle wedge above a subducting slab during the Cretaceous. Physical and chemical evidence for high-pressure fractionation seen in most of the pyroxenites precludes them from simply representing ancient subducted oceanic lithosphere, thinned by diffusion. However, the petrological and isotopic diversity of the massif support the concept of a 'marble cake' mantle capable of producing the observed geochemical diversity seen in oceanic magmas.

AB - The petrogenesis of pyroxenite layers within the Beni Bousera peridotite massif is investigated by means of elemental and Nd-Sr-Pb-O-S isotope analyses. The light rare earth element (LREE) depleted nature of many of the pyroxenites, their wide variation in composition, and lack of correlation between incompatible elements and fractionation indices preclude them from representing crystallized melts from a peridotitic source. The physical characteristics of the pyroxenites and their large (greater than a factor of 20) range in Ni rule out partial melting as the cause of their petrological and geochemical diversity. Major and compatible trace element geochemistry is consistent with formation of most of the pyroxenite suite via high-pressure crystal segregation in magma conduits intruding the peridotites. These magmas crystallized clinopyroxene, orthopyroxene, and garnet. The pressure of crystallization is constrained to be above ̃45 kbar from the presence of graphitized diamonds in pyroxenite layers. Lack of correlation between fractionation indices and highly incompatible elements and the wide variation in incompatible element abundances suggest that the suite did not form from genetically related magmas. The presence of positive and negative Eu anomalies (Eu/Eu* = 0{dot operator}54-2{dot operator}0) in pyroxenites which crystallized at pressures much greater than the plagioclase stability field (̃ 45 kbar) suggests that the parental magmas originated from precursors which formed in the crust. Oxygen isotope compositions of coexisting minerals in the pyroxenites indicate high-temperature equilibration but δ18O values vary from +4{dot operator}9 to + 9{dot operator}3‰, ruling out their derivation from the host peridotites or other normal mantle sources. The extreme O-isotope variation, together with δ34S values of up to + 13‰ in sulphides included within CPX strongly suggests that the melts from which the pyroxenites crystallized were derived from hydrothermally altered, subducted oceanic lithosphere. Extreme initial radiogenic isotope variation in the pyroxenites (εNd + 26 to -9,87Sr/86Sr 0{dot operator}7025-0{dot operator}7110, 206Pb/204Pb 18{dot operator}21-19{dot operator}90) support such an origin but also require a component with ancient, high U/Pb and Th/Pb in their source to explain the high Δ7/4 and Δ8/4 values of some pyroxenites. This component may be subducted hemi-pelagic sediment. Further evidence for a sediment component in the pyroxenites is provided by isotopically light carbon in the graphite pyroxenites (δ13C-16 to - 28‰). Parentdaughter isotopes in the pyroxenites are strongly decoupled, making estimation of formation ages speculative. The decoupling occurred recently (<200 Ma), probably as a result of partial melting associated with diapiric upwelling and emplacement of the massif into the crust from the diamond stability field. This late partial melting event further depleted the pyroxenites in incompatible elements. The variably altered nature of the subducted protolith and complex history of trace element fractionation of the pyroxenites has largely obscured geochemical mixing trends. However, Nd-Pb isotope systematics indicate that incorporation of the component with high U/Pb-Th/Pb occurred relatively recently (<200 Ma) for some pyroxenites. Other pyroxenites do not show evidence for incorporation of such a component and may be substantially older. Tectonic, geophysical, and isotopic constraints indicate formation of the pyroxenites in the mantle wedge above a subducting slab during the Cretaceous. Physical and chemical evidence for high-pressure fractionation seen in most of the pyroxenites precludes them from simply representing ancient subducted oceanic lithosphere, thinned by diffusion. However, the petrological and isotopic diversity of the massif support the concept of a 'marble cake' mantle capable of producing the observed geochemical diversity seen in oceanic magmas.

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