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all geography including DSDP/ODP Sites and Legs
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Necker Island
Geomorphometric descriptions of archipelagic aprons off the southern flanks of French Frigate Shoals and Necker Island edifices, Northwest Hawaiian Ridge
Plots of (A) French Frigate Shoals (FFS) and Necker Island (NI) edifices es...
(A) Map view of multibeam echosounder bathymetry of Necker Island edifice (...
Sub-bottom profiler record south of the Necker Island edifice that shows th...
(A) Map view of multibeam echosounder bathymetry of Necker Island edifice (...
Contributions to the Petrography and Geochronology of Volcanic Rocks from the Leeward Hawaiian Islands
One of the objectives of the 1950 expedition to Bikini carried on by the Scripps Institution of Oceanography and the U. S. Navy Electronics Laboratory was to investigate previously located flat-topped seamounts ( guyots of Hess, 1946) in an area 600–1100 miles west of Hawaii. Five of these seamounts were surveyed by echo sounder, dredged, and cored, and were found to be peaks on a great submarine range—the Mid-Pacific Mountains—which extends from Necker Island in the Hawaiian Islands to near Wake Island. The flat-topped guyots are submerged to between 700 and 900 fathoms. The sides are concave upward with slopes about 20° near the tops. The profiles are symmetrical with breaks in slope at 720–1150 fathoms. Rounded sand grains, pebbles, cobbles, and boulders of olivine basalt were dredged from the tops and across the breaks in slope. Sandstone and reef coral were dredged together at one station. Dredge hauls across the breaks in slope on the tops of two guyots brought up an integrated Cretaceous (Aptian-Cenomanian) fauna of reef coral, rudistids, stromato-poroids, gastropods, pelecypods, and an echinoid; these have affinities with the faunas of the Tethyan Province around the Gulf Coast and adjacent regions. In a core taken in a basin near one guyot, the basaltic gravel layers contained Upper Cretaceous (Campanian-Maestrichtian) Foraminifera. Paleocene and Eocene Foraminifera occur on the flat tops of four guyots. The evidence indicates that in Cretaceous time the guyots were a chain of basaltic islands. These islands were wave-eroded to relatively flat banks on which a reef coral-rudistid fauna found lodgment and grew into reefs on and among the erosional debris. They never became fully developed atolls. The guyots were submerged during the Cretaceous to below the zone of reef-coral growth; finally they sank to present depth. The submergence is thought to have been due to regional subsidence of the sea bottom resulting for the most part from isostatic adjustments and subcrustal forces. A minor part of the submergence can probably be attributed to increase in ocean volume, sedimentation, and the compaction of soft sediments. In general the findings support Darwin’s Subsidence Theory for the formation of atolls; they furnish evidence for a deep Cretaceous Pacific Ocean; and they refute the hypothesis of transoceanic “sunken continents” used to explain faunal migrations, at the same time suggesting the possibility of “island stepping stones”.
Eustatic Bench of Islands of the North Pacific
Hawaiian hotspot volcanism mainly during geomagnetic normal intervals
Slope map of multibeam echosounder bathymetry of archipelagic aprons of Fre...
Map view of MBES bathymetry of large field of bedforms shed off the southea...
(A) Plot of debris avalanche areas vs. runout distance is overlain with cur...
(A) Multibeam echosounder (MBES) bathymetry of southern archipelagic aprons...
Overview map shows bathymetry of a section of the mid-Hawaiian Ridge and Mi...
(A) Perspective view of multibeam echosounder bathymetry looking NNE of sou...
A VISIT TO LOUIS-ALBERT NECKER ON THE ISLE OF SKYE, 1852.
North Pacific Bottom Potential Temperature
The bottom potential temperature distribution for the Pacific Ocean north of 11° S. is presented, based upon 495 data points derived from hydrographic stations, the Lamont thermograd, and an in-situ salinity-temperature-depth recorder. Although the entire range of potential temperature is only 1.2° C, an oceanwide pattern is apparent. The coldest bottom water (< 0.8° C potential temperature) occurs in the equatorial region between 160° and 180° W. This feature can be traced into the area north of Hawaii by paths both east and west of these islands with a warming of only 0.5° C. In order to separate the effect of the decrease of potential temperature with depth (which occurs in the upper 4000 to 5000 m) from the bottom variation due to influx of cold water, the anomaly of bottom potential temperature is plotted. This parameter is defined as the difference between the observed bottom potential temperature for a particular station and the average bottom potential temperature for the North Pacific at the depth of the observation. The water between 160° and 180° W. has the largest negative anomaly, 0.3° C colder than the average t p found at corresponding depths. The water north of Hawaii has a positive anomaly, indicating that in this region the deeper water is relatively warm compared to that in the equatorial region between 160° and 180° W., even after the depth effect is removed. The bottom water over and east of the crest of the mid-ocean ridge at 120° W. has large positive anomalies, suggesting the possibility that this water is warmed by geothermal heating. From the bottom potential temperature distribution and the anomalies of these values, together with recently obtained Lamont bottom current measurements, it is possible to trace the basic pattern of bottom circulation (which should also reflect the circulation for the water below 2000 to 2500 m). The sole influx of water is the Antarctic Bottom Water flowing northward along 175° W. from 20° S. to 16° N. This current is no doubt a continuation of the deep western boundary current along the Tonga Trench described recently for the South Pacific. From this point, the flow divides into two zonal branches. The eastern branch passes between the Johnston Island and Christmas Island Ridges and the western branch passes between the Marshall Islands and the Marcus-Necker Ridge. After trans-versing these respective passages, both flows turn northward, eventually converging in the North Pacific Basin between the Hawaiian and the Aleutian Islands, where deep upward transport is expected. It is estimated that the time necessary for the water to flow from 175° W., 10° S. to the center of the convergence area is 750 years.
A COMPARISON BETWEEN ‘PART OF SCOTLAND’ ON WILLIAM SMITH’S MAPS AND CONTEMPORARY MAPS OF SCOTLAND BY LOUIS-ALBERT NECKER AND JEAN-FRANÇOIS BERGER
Multiple melt source origin of the Line Islands (Pacific Ocean)
Aseismic ridges on underthrusting oceanic plates often trend into cusps or irregular indentations in the trace of the subduction zone. For example, the Hawaii-Emperor Ridge trends into the Kuril-Aleutian cusp, and the Marianas arc is bounded by the Marcus-Necker Ridge on the north and the Caroline Ridge on the south. The association between ridges and cusps is too common to be due to chance; it is proposed that the extra buoyancy of the plate with its aseismic ridge gives the plate greater resistance to sinking. This would inhibit back-arc extension and thereby produce a notch in the subduction zone. Island arcs may, therefore, acquire their curvature by additional constraints than the Earth’s curvature. The geology of about 15 such cusp areas is examined for evidence to test the hypothesis that cusps were caused by subducted aseismic ridges. This hypothesis applies only to cases where extensional basins lie behind the arcs. There also appear to be cases where the trace of the subduction zone has been modified not by inhibited back-arc spreading but by splintering of the overthrusting and possibly the underthrusting plate as well. Extremely high, massive aseismic ridges might induce arc polarity reversals and thereby assume the role of protocontinental nuclei. Seismicity and volcanism are examined where aseismic ridges are being subducted; there are several examples of reduced seismicity that cannot be explained by insufficient sampling time. By modifying the geometry of the subduction zone, the downgoing ridges necessarily affect seismicity. In addition, the plate containing the ridge may be thinner and hotter and more likely to deform by creep. There is no systematic increase or decrease in the number of andesite volcanoes where the ridges are subducted. However, lines of volcanoes and sometimes other kinds of geologic and seismic provinces may stop or start at the arc-ridge intersections. This is attributed to segmenting of the lithosphere into distinct tongues, each tongue acting more or less independently. Aseismic ridges would act as lines of weakness along which the downthrust slab becomes detached.