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Nihoa Island
Contributions to the Petrography and Geochronology of Volcanic Rocks from the Leeward Hawaiian Islands
Eustatic Bench of Islands of the North Pacific
Seismic refraction surveys along the Hawaiian Ridge, Kauai to Midway Island
Hawaiian submarine manganese-iron oxide crusts—A dating tool?
Abstract Oceanic plates are geologically young, forming at mid-ocean ridges and becoming deeper and older with distance away from these spreading centres, to be subducted into ocean trenches. Most of the islands that occur on these oceanic plates are basaltic, formed at hot spots, and carried into deeper water as the plate migrates. In tropical reef-forming seas, volcanic islands are usually protected by coral reefs, and undergo transition from fringing reefs, to barrier reefs, to atolls, as envisaged by Darwin. Linear island chains comprise volcanic islands at successive stages in the progression from volcano through coral reefs to seamounts and guyots. Erosion occurs rapidly in the early stages once eruption has ceased, and older islands are conspicuously dissected by fluvial action, as observed by Dana. Many are subject to submarine slumping. In the absence of coral reefs, marine abrasion truncates islands, producing near-vertical cliffs, and islands may be entirely bevelled; Balls Pyramid in the southern Pacific appears to be at the penultimate stage of this planation with a broad shelf around it. Coral reefs protect the shoreline, which is usually deeply embayed, with progressive subsidence until volcanic residuals are all that remain on ‘almost-atolls’. Reef limestones indicate earlier phases of reef formation, and there are limestone cliffs around many tropical islands composed of Last Interglacial limestone often veneering older reef terraces. In some cases, the morphology of these limestone coasts contains prominent notches or surf benches reflecting different degrees of exposure to wave energy, or subtle flexure and vertical displacement. Islands provide discrete examples of rocky coasts, with contrasts between adjacent islands, or islands of different ages, providing many insights into the evolutionary stages and the morphodynamics of bold coasts.
Seismometric investigation of the Hawaiian lava column
A plate model for Jurassic to Recent intraplate volcanism in the Pacific Ocean basin
Reconstruction of the tectonic evolution of the Pacific basin indicates a direct relationship between intraplate volcanism and plate reorganizations, which suggests that volcanism was controlled by fracturing and extension of the lithosphere. Middle Jurassic to Early Cretaceous intraplate volcanism included oceanic plateau formation at triple junctions (Shatsky Rise, the western Mid-Pacific Mountains) and a diffuse pattern of ocean island volcanism (Marcus Wake, Magellan seamounts) reflecting an absence of any well-defined stress field within the Pacific plate. The stress field changed in the Early Cretaceous when accretion of the Insular terrane to the North American Cordillera and the Median Tectonic arc to New Zealand stalled migration of the Pacific-Farallon and Pacific-Phoenix ocean ridges, leading to the generation of the Ontong Java, Manahiki, Hikurangi, and Hess Rise oceanic plateaus. Plate reorganizations in the Late Cretaceous resulted from the breakup of the Phoenix and Izanagi plates through collision of the Pacific-Phoenix ocean ridge with the southwest margin of the basin and development of island arc–marginal basin systems in the northwestern part of the basin. The Pacific plate nonetheless remained largely bounded by spreading centers, and intraplate volcanism followed preexisting lines of weakness in the plate fabric (Line Islands) or resulted from fractures generated by ocean ridge subduction beneath island arc systems (Emperor chain). The Pacific plate began to subduct under Asia in the Early Eocene as inferred from the record of accreted material along the Japanese margin. Further changes to the stress field at this time resulted from abandonment of the Kula-Pacific and the North New Guinea (Phoenix)–Pacific ridges and from development of the Kamchatkan and Izu-Bonin-Mariana arcs, leading to the generation of the Hawaiian chain as a propagating fracture. The final major change in the stress field occurred in the Late Oligocene as a result of breakup of the Farallon into the Cocos and Nazca plates, which caused a hiatus in Hawaiian volcanism; initiated the Sala y Gomez, Foundation, and Samoan chains; and terminated the Louisville chain. The correlations with tectonic events are compatible with shallow-source models for the origin of intraplate volcanism and suggest that the three principal categories of volcanism, intraplate, arc, and ocean ridge, all arise from plate tectonic processes, unlike in plume models, where intraplate volcanism is superimposed on plate tectonics.