Geochemistry and age of the Ontong Java Plateau

Mahoney, John J.; Storey, Michael; Duncan, Robert A.; Spencer, Khalil J.; Pringle, Malcolm S.

doi:10.1029/gm077p0233

Cited by 184 publications

(166 citation statements)

References 56 publications

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“…)), with no evidence for a volumetrically significant younger phase at c. 90 Ma, as had been suggested by previous work (e.g. Mahoney et al 1993;Tejada et al 1996). At Site 1184, shipboard nannofossil data suggested that the volcaniclastic sequence was emplaced during the middle Eocene.…”

Section: Ocean Drilling Program Leg 192 Site 1184supporting

confidence: 55%

“…In addition, a comparison of the major-element data for unaltered glass and altered bulk tuff samples, as well as isotopic data for altered volcaniclastic rocks and basalts from the OJP (cf. Mahoney et al 1993;Tejada et al 1996Tejada et al , 2002Tejada et al , 2004Neal et aL 1997), provide some constraints on the chemical and isotopic changes that occur during sedimentation and alteration, and may assist future studies of similarly altered volcaniclastic rocks. This work is complemented by a study of lithic clasts from the volcaniclastic rocks at Site 1184 (Sharer et al 2004).…”

Section: Ocean Drilling Program Leg 192 Site 1184mentioning

confidence: 99%

“…Shafer et aL 2004), but falls within the range of previously analysed Kwaimbaita-type lavas (cf. Mahoney & Spencer 1991;Mahoney et al 1993;Tejada et aL 1996Tejada et aL , 2002Neal et al 1997). This sample belongs to Subunit IIA, which has a Kroenke-type elemental signature according to glass clasts and bulk tuff analyses.…”

Section: 15mentioning

confidence: 99%

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Phreatomagmatic eruptions on the Ontong Java Plateau: chemical and isotopic relationship to Ontong Java Plateau basalts

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Castillo

Neal

et al. 2004

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Abstract:The compositions of glass clasts in volcaniclastic rocks recovered from drilling at Site 1184 on the eastern salient of the Ontong Java Plateau (OJP) are investigated using microbeam analytical methods for major, minor and trace elements. These data are compared with whole-rock elemental and isotopic data for bulk tuff samples, and with data from basalts on the high plateau of the OJP. Three subunits of Hole 1184A contain blocky glass clasts, thought to represent the juvenile magmatic component of the phreatomagmatic eruptions that generated the volcaniclastic rocks. The glass clasts have unaltered centres, and are all basaltic low-K tholeiites, with flat chondrite-normalized rare earth element (REE) patterns. Their elemental compositions are very similar to the Kwaimbaita-type and Kroenke-type basalts sampled on the high plateau. Each subunit has a distinct glass composition and there is no intermixing of glass compositions between subunits, indicating that each subunit is the result of one eruptive phase, and that the volcaniclastic sequence has not experienced reworking. The relative heterogeneity preserved at Site 1184 contrasts with the uniformity of compositions recovered from individual sites on the high plateau, and suggests that the eastern salient of the OJP had a different type of magma plumbing system. Our data support the hypothesis that the voluminous subaerially erupted volcaniclastic rocks at Site 1184 belong to the same magmatic event as the construction of the main Ontong Java Plateau. Thus, the OJP would have been responsible for volatile fluxes into the atmosphere in addition to chemical fluxes into the oceans, and these factors may have influenced the contemporaneous oceanic anoxic event.

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Section: Ocean Drilling Program Leg 192 Site 1184supporting

confidence: 55%

Section: Ocean Drilling Program Leg 192 Site 1184mentioning

confidence: 99%

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Phreatomagmatic eruptions on the Ontong Java Plateau: chemical and isotopic relationship to Ontong Java Plateau basalts

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Castillo

Neal

et al. 2004

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“…40 Ar/ 39 Ar dating of the basalt from DSDP Site 317 indicated that the basalts were erupted around 123.7 ± 1.5 Ma (Mahoney et al 1993;Larson and Erba 1999). The vesicular character of the basalts also indicates that the eruptions took place in shallow water ).…”

Section: Discussion Of Isopach Mappingmentioning

confidence: 99%

Vertical tectonics of the High Plateau region, Manihiki Plateau, Western Pacific, from seismic stratigraphy

Stock

Clayton

et al. 2008

Mar Geophys Res

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The Manihiki Plateau is an elevated oceanic volcanic plateau that was formed mostly in Early Cretaceous time by hotspot activity. We analyze new seismic reflection data acquired on cruise KIWI 12 over the High Plateau region in the southeast of the plateau, to look for direct evidence of the location of the heat source and the timing of uplift, subsidence and faulting. These data are correlated with previous seismic reflection lines from cruise CATO 3, and with the results at DSDP Site 317 at the northern edge of the High Plateau. Seven key reflectors are identified from the seismic reflection profiles and the resulting isopach maps show local variations in thickness in the southeastern part of the High Plateau, suggesting a subsidence (cooling) event in this region during Late Cretaceous and up to Early Eocene time. We model this as a hotspot, active and centered on the High Plateau area during Early Cretaceous time in a near-ridge environment. The basement and Early Cretaceous volcaniclastic layers were formed by subaerial and shallow-water eruption due to the volcanic activity. After that, the plateau experienced erosion. The cessation of hotspot activity and subsequent heat loss by Late Cretaceous time caused the plateau to subside rapidly. The eastern and southern portions of the High Plateau were rifted away following the cessation of hot spot activity. As the southeastern portion of the High Plateau was originally higher and above the calcium carbonate compensation depth, it accumulated more sediments than the surrounding plateau regions. Apparently coeval with the rapid subsidence of the plateau are normal faults found at the SE edge of the plateau. Since Early Eocene time, the plateau subsided to its present depth without significant deformation.

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“…It was emplaced during three volcanic phases in the early Cretaceous: the initial formation phase (>125 Ma), followed by the expansion phase (∼125-116 Ma) and secondary volcanism (∼110-65 Ma; Pietsch & Uenzelmann-Neben 2015). During the expansion phase, previously referred to as main formation phase, massive eruptions of tholeiitic basalts occurred (Lanphere & Dalrymple 1976;Shipboard Scientific Party 1976;Mahoney et al 1993;Larson & Erba 1999;Hoernle et al 2010;Timm et al 2011), resulting in anomalously thick oceanic crust (Hussong et al 1979) that comprises a thickness up to 20 km on the High Plateau (Hochmuth et al, in preparation). Secondary volcanism (∼100-65 Ma) consisted of alkaline volcaniclastics (Ingle et al 2007;Hoernle et al 2010;Timm et al 2011), which broadened and flattened the topographic appearance of the High Plateau and preferentially occurred at the margins of the High Plateau (Pietsch & Uenzelmann-Neben 2015).…”

Section: The Manihiki Plateaumentioning

confidence: 99%