An iron-rich deposit from the Northeast Pacific

Piper, David Z.; Veeh, H. H.; Bertrand, W.G.; Chase, R. L.

doi:10.1016/0012-821x(75)90183-1

Cited by 41 publications

(15 citation statements)

References 38 publications

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“…The REE patterns of hydrothermal Mn oxide deposits may or may not have a negative Ce anomaly depending on the temperature of the fluid, proximity to the hydrothermal source, and amount of hydrogenetic input (Puteanus et al, 1991;Toth, 1980;Hein, et al, 1992a;Piper et al, 1975;Stoffers et al, 1985). Highertemperature, more heat-source proximal deposits would be expected to have larger negative Ce anomalies (Fleet, 1983).…”

Section: La Ce Pr Nd Sm Eu Gd Tb Dy Ho Er Tmmentioning

confidence: 94%

Hydrothermal mineralization along submarine rift zones, Hawaii

Hein¹,

Gibbs

Clague

et al. 1996

Marine Georesources & Geotechnology

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This is the first article to describe mineralization of midplate submarine rift zones and hydrothermal manganese oxide mineralization of midplate volcanic edifices. Hydrothermal Mn oxides were recovered from submarine extensions of two Hawaiian rift zones, along Haleakala and Puna Ridges. These Mn oxides form two types of deposits, metallic stratiform layers in volcaniclastic rocks and cement for clastic rocks; both deposit types are composed of todorokite and bimessite. Thin Fe-Mn crusts that coat some rocks formed by a combination of hydrogenetic and hydrothermal processes and are composed of δ-MnO 2 . The stratiform layers have high Mn contents (mean 40%) and a large fractionation between Mn and Fe (Fe/Mn = 0.04). Unlike most other hydrothermal Mn oxide deposits, those from Hawaiian rift zones are enriched in the trace metals Zn, Co, Ba, Mo, Sr, V, and especially Ni (mean 0.16%). Metals are derived from three sources: mafic and ultramafic rocks leached by circulating hydrothermal fluids, clastic material (in Mn-cemented sandstone), and seawater that mixed with the hydrothermal fluids. Mineralization on Haleakala Ridge occurred sometime during the past 200 to 400 ka, when the summit was at a water depth of more than 1,000 m. Hydrothermal circulation was probably driven by heat produced by intrusion of dikces, magma reservoirs, and flow of magma through axial and lateral conduits. The supply of seawater to ridge interiors must be extensive because of their high porosity and

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Section: La Ce Pr Nd Sm Eu Gd Tb Dy Ho Er Tmmentioning

confidence: 94%

Hydrothermal mineralization along submarine rift zones, Hawaii

Hein¹,

Gibbs

Clague

et al. 1996

Marine Georesources & Geotechnology

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“…The higher contents of Si, Sr and Ba in G994 may be related to higher contents of terrigenous material derived from the New Zealand landmass as this sample was taken from a station closer to New Zealand than G1003 (see MEYLAN et al 1975;BACKER et al 1976 CROCKET et al 1973;PIPER and GRAEF 1974). The rare earth element concentrations are, however, higher than those in a number of abyssal marine and other sediments (HASKIN and GEHL 1962;WILDEMAN and HASKIN 1965;HAS KIN et al 1966;SHIMOKAWA et al 1972;VOLKOV and FOMINA 1973;FLEET and KEMPE 1974;PIPER 1974b;PIPER and GRAEF 1974;PIPER et al 1975;FLEET 1977;HEIN et al In press;MELGUEN et al In press) as well as in marine basalts (MASUDA and NAGASAWA 1975;FLEET et al .1976;THOMPSON et al 1978), although the La concentrations are lower than those reported in previous spectrographic analyses of some marine clays (YOUNG 1954;GOLDBERG and ARRHENIUS 1958;EL WAKEEL and RILEY 1961) (see however, DYMOND et al 1973DYMOND et al , 1977). The high rare earth contents of the G994 and G 1003 sediments therefore probably reflect the well oxidised nature of these sediments (to be published elsewhere).…”

Section: B Sedimentsmentioning

confidence: 92%

The distribution of rare earth, precious metal and other trace elements in Recent and fossil deep-sea manganese nodules.

Glasby

Keays

Rankin³

1978

Geochem. J.

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Four deep-sea manganese nodules and one fossil nodule from Timor have been analysed for 45 elements (major elements, rare earths and precious metals) by X-ray fluorescence, spark source mass spectrometry and neutron activation analysis. Co-existing sediments from two nodule sites in the South western Pacific Basin have also been analysed. Differences in nodule composition are apparent, particularly for the Timor nodule. The trace metal compositions of this nodule, however, reveals it to be a typical deep-sea nodule, although some element redistribution has clearly taken place since exposure of the nodule on land. The distribution of a number of elements including Tl, Ir, Pd, Au and the rare earth elements between deep-sea nodules and their associated sediments appears to be dependent on a number of factors including the major element composition of the nodule (e.g. dilution by the silicate phase of the nodule), the differing stability of various element complexes in seawater, and the influence of differences in redox states on complex stability. Au and Si, on the other hand, are positively correlated in nodules and sediments possibly because they have a common source, either submarine detritus or basalt-seawater interaction. The rare earth contents of the sediments from the N.E. sector of the Southwestern Pacific Basin are high compared with previous determinations of rare earths in marine sediments and show no evidence of Ce depletion relative to La on a shale-normalised basis. These high contents reflect the well oxidised conditions and low sedimentation rates of this environment.

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“…(1 = smectites with low rare-earth element concentrations from Galapagos hydrothermal mounds (average of three samples); 2 = Fe-rich hydrothermally derived product from northeast Pacific [Piper et al, 1975]; 3 = vein smectites from Hole 504B basalts, Costa Rica Rift (Sharaskin et al, in press); 4 = Mn-enriched sediments, Malinelo deposit, Italy [Bonatti, Zerbi, et al, 1976]; 5 = Fe-Mn oxide sediment from Galapagos mounds; 6 = lower Mn crusts of Galapagos mounds; 7 = Fe-rich smectites of Galapagos mounds; 8 = oxidized hydrothermal pyrite concretions from Romanch deep (Bonatti, Honnorez-Guerstein, et al, 1976); 9 = upper manganese crusts of Galapagos mounds; 10 = metalliferous sediments from the East Pacific Rise [Piper and Graef, 1974]; 11 = metalliferous sediments of Troodos massif, Cyprus [Robertson and Fleet, 1976].) …”

Section: Minor Elementsmentioning

confidence: 99%