Phosphorus fractionation diagram as a quantitative indicator of crystallization differentiation of basaltic liquids

Anderson, A. T.; Greenland, L.P.

doi:10.1016/0016-7037(69)90129-x

Cited by 83 publications

(38 citation statements)

References 9 publications

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“…The whole rock composition was recalculated using mineral chemistry and modal analyses (Cvetković et al 2004 b). (La Tourette et al 1995), U, Zr and Hf (Villemant et al 1981), Nb and Y (Chazot et al 1996) and Ta (Green et al 1993); D mineral/melt for phlogopite (Phl) from Fujimaki et al (1984) except for Th and Nb (La Tourette et al 1995), U and Tb (Villemant et al 1981) and for Ta, Sr and Y (Foley et al 1996); D mineral/melt for ilmenite (Ilm) from Zack & Brumm (1998) except for P (Anderson & Greenland 1969) and for Zr and Hf (Fujimaki et al 1984); The values for D mineral/melt for calcite (cc) are considered too low for all elements except for Sr which is considered to be unity (e.g. Ionov & Harmer 2002); D mineral/melt for apatite (Ap) from Paster et al (1974) except for Th, U (average values from Luhr et al 1984;Bea et al 1994;Mahood & Stimac 1990), Sr, Dy and Lu (Watson & Green 1981), Zr, Hf and Er (Fujimaki 1986) and for P for which D mineral/melt was calculated on the basis of P 2 O 5 concentrations in apatite from ESLM xenoliths and in host basanites.…”

Section: Appendix Inversion Modelingmentioning

confidence: 99%

Mafic alkaline metasomatism in the lithosphere underneath East Serbia: evidence from the study of xenoliths and the host alkali basalts

Cvetković

Downes

Höck

et al. 2010

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Effects of mafic alkaline metasomatism have been interpreted by study of East Serbian (SE Europe) mantle xenoliths and petrogenesis of their host alkaline rocks. Fertile xenoliths (addition of >10 %vol. of metasomatic clinopyroxene) and tiny assemblages found in depleted xenoliths are distinguished. The fertile lithology contains Ti-Al-Cr-rich clinopyroxene, Fe-rich olivine, Fe-Al-rich orthopyroxene and Al-rich spinel. The composition of this lithology is modeled by addition of 5-20 wt% of a basanitic-like melt to a refractory mantle. The small-scale assemblages occur as pocket-like, symplectitic or irregular deformation-assisted accumulations of metasomatic phases, generally composed of Ti-Al-and incompatible elements-rich Cr-diopside, Cr-Fe-Ti-rich spinel, altered glass, olivine, apatite, ilmenite, carbonate and feldspar, as well as relicts of a high-TiO2 (~11 wt%) phlogopite. Textural relationships imply the following reaction: opx + Cr-rich sp ±phlogopite + Si-poor alkaline melt = Ti-Al-cpx + Ti-rich sp ± ol ± other minor phases. The inversion modeling, performed on least contaminated and most isotopically uniform host basanites, implies a source which is enriched in highly and moderately incompatible elements (~35-40xchondrite for U-Th-Nb-Ta, 2xchondrite for heavy rare earth elements) suggesting that the primary magma of the host basanites was not derived by melting of a homogeneous asthenospheric source. D0 values of the calculated basanitic source are similar to D0 values of anhydrous metasomatized mantle with small additions of metasomatic clinopyroxene and carbonate (~5 %) and with traces of ilmenite (~1 %) and apatite (~0.05 %). A schematic two-phase model involves percolation of CO2-and H2O-rich fluids, precipitation of metasomatic hydrous minerals and their subsequent breakdown due to the further uplift of hot asthenospheric mantle. This model uses a general idea of linking intraplate alkaline magmatism to lithospheric mantle sources enriched by sub-lithospheric melts at some time in the past. Mantle metasomatism is generally believed to be responsible for small-scale heterogeneities within the lithosphere (Dawson 1984; Harte 1984Harte , 1987Menzies et al. 1987). Evidence from the study of mantle xenoliths entrained in alkali basalts proved to be particularly important for understanding the origin of such heterogeneities. Studies have shown that the major metasomatic agents are: (i) carbonatitic melts (Baker et al. 1998;Yaxley et al. 1998;Gorring & Kay 2000; Wang & Gasparik 2001), (ii) silicate melts (Menzies et al. 1987;Vannucci et al. 1998;Zangana et al. 1999;Gregoire et al. 2000;Kepezhinskas et al. 1995Kepezhinskas et al. , 1996Schiano et al. 2002) and (iii) fluids (O'Reilly & Griffin 1988;Baker et al. 1998;Gorring & Kay 2000;Larsen et al. 2003), the latter two having a wide range of compositions. All these agents produce different metasomatic styles recognized by changes in primary mantle mineralogy and specific enrichments in trace element composition. It is widely accepted that mafic al...

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Section: Appendix Inversion Modelingmentioning

confidence: 99%

Mafic alkaline metasomatism in the lithosphere underneath East Serbia: evidence from the study of xenoliths and the host alkali basalts

Cvetković

Downes

Höck

et al. 2010

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“…The vectors show how the melt composition will change in response to crystallization of these phases, the lengths of the vectors corresponding to 50% crystallization (F = 0.5), except where indicated in the figure caption. The distribution coefficients (D) used to calculate the vectors are taken from the compilations of Pearce and Norry (1979), Ottonello et al (1984), Anderson and Greenland (1969), and Philpotts and Schnetzler (1970). Provided that neither distribution coefficients nor phase proportions vary markedly during basalt fractionation, linear fractionation trends should be obtained for each crystallizing assemblage.…”

Section: Trace-element Modelingmentioning

confidence: 99%

Geochemistry and Petrogenesis of Basalts from Deep Sea Drilling Project Leg 92, Eastern Pacific

Pearce¹,

Rodgers²,

Tindle³

et al. 1986

Initial Reports of the Deep Sea Drilling Project

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Basalts recovered on DSDP Leg 92 include all the major basalt types so far recovered from the ocean crust of the eastern Pacific. Basalts from Holes 597, 597A, 597B, 597C, and 599B are tholeiites exhibiting all the mineralogical and geochemical characteristics of N-type mid-ocean ridge basalts (MORB). Fragments of ferrobasalts and alkali basalts were also obtained, however, from Holes 60IB and 602B, respectively. Hole 597C, which penetrated 91 m into basement and is the deepest hole so far drilled in fast-spreading crust, yielded basalts that can be divided into three major lithologic units. The lowest unit, Unit III, contains modal olivine and comprises basalts which, at about 8 to 10% MgO, are as basic as any sampled from fast-spreading crust. The middle unit, Unit II, is the most evolved; its basalts are olivine free and contain between 6 and 7.5% MgO. The upper unit, Unit I, is intermediate in composition between Units II and III; it is characterized by both modal olivine and glomerocrysts made up of plagioclase and rare olivine. Unit I is probably a massive flow, whereas Units II and III may be massive flows or sills. The basalts appear to have undergone three stages of alteration ("deuteric," "relatively reducing," and "oxidizing"), the intensity of alteration decreasing markedly downcore. Hole 597B, at 26.4 m of basement penetration the only other "deep" hole, contains just one lithologic unit, which closely resembles Unit I of Hole 597C.Petrogenetic modeling reveals that the three lithologic units in Hole 597C are cogenetic and that they were derived from a depleted mantle source similar to the source of the tholeiites and ferrobasalts sampled in other holes; the alkali basalts are the only rocks derived from enriched mantle. Lavas of Unit III probably lay on the olivine-plagioclase cotectic, whereas the other lavas lay on an olivine-plagioclase-clinopyroxene peritectic. Some 60% of closed-system crystallization is needed to generate the most-evolved from the last-fractionated tholeiite, and a further 50% crystallization (80% overall) is needed to generate the ferrobasalts. Xenocrysts of calcic plagioclase and pseudomorphosed olivine in tholeiites from Hole 597B and Unit I of Hole 597C, and in the ferrobasalts from Hole 601B, provide evidence, however, that some magma mixing may have taken place.

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“…Table 6 lists the results of fractionation calculations (Anderson and Greenland, 1969) Figure 4. Note that the low-REE group (×) has higher Zr relative to P than the high-REE group (A).…”

Section: Rare-earth Atomic Nomentioning

confidence: 99%

Trace-Element Geochemistry of Tholeiitic Basalts from Site 433C, Suiko Seamount

Clague¹,

Frey²

1980

Initial Reports of the Deep Sea Drilling Project

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Phosphorus fractionation diagram as a quantitative indicator of crystallization differentiation of basaltic liquids

Cited by 83 publications

References 9 publications

Mafic alkaline metasomatism in the lithosphere underneath East Serbia: evidence from the study of xenoliths and the host alkali basalts

Mafic alkaline metasomatism in the lithosphere underneath East Serbia: evidence from the study of xenoliths and the host alkali basalts

Geochemistry and Petrogenesis of Basalts from Deep Sea Drilling Project Leg 92, Eastern Pacific

Trace-Element Geochemistry of Tholeiitic Basalts from Site 433C, Suiko Seamount

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