Easter Island Age

Though Professor Murrill was not a member of the mission, he was asked to examine and analyse the anthropological aspects of the skeleton found by the mission during Easter Island missions. These finds shed a clear light on the origins of the Easter Islanders.

It is unlikely that a Negroid migratory (possibly from Melanesia) has anticipated a Polish to Easter Island and, based on his assessment of the type grouping system, he proposes that the Polish and Native Indians might come from the same genetic stock in East Asia.

The Easter Volcano Range

On this website we summarize the cases for the Plume and Plate assumptions. In the Plume theory, the intra-plate vulcanism is attributed to a warm diaphragm that climbs from the core-shell limit and is fixated in relation to other plums. In the plate theory, the molten mass is fed to the lithospherical expansion, which allows a leak to the already present molten mass which is widely spread in the flat shell.

The Easter and Sala y Gomez Islands are located on the Nazca Plateau in the East Pacific in an area of high terrain known as Sala y Gomez Ridge (Figure 1). The topographical high is continued at its east end as the Nazca ridge. It is about 4,100 km long and mostly of vulcanic origins.

Only the small peaks of the high peaks make up the island itself and show only a small part of the mountain crest (Clarke & Dymond, 1977). The Easter Island is 360 km eastern of the Eastern Pacific Rise (EPR) and the island Sala y Gomez 390 km further south. Oster-Mikroplatte is located slightly westward of Easter Island and forms at 5. 2 Ma (approx. 3 hours of magnetics; Fig. 1).

Oster-Sala y Gomez-Kamm itself is about 2,900 km long and about 150 km afar. Nazca-back is about 1.200 km long and about 300 km broad. In general, the whole area is aging eastwards. The Pitcairn Gambier Range, another mountain range, stretches westwards from the Eastern Pacific Rise (EPR).

There also shows the casual island, which included Pitcairn Island, which was volcanic at ~ 3.0-0. 3 Ma; Gilliou et al., 1997). Fig. 1: The K-Ar age shows that the eastern Pacific archipelago grows older from 8 Ma to ~26 Ma. The different sites suggested for an Easter flag are marked with an asterisk: Easter:

The Easter Island (Morgan, 1971), Sala y Gomez Island (Ray et al., 2012), 360 km from Sala y Gomez (O'Connor et al., 1995), western Easter Island (Haase et al., 1996) and between Easter and Sala y Gomez Isles (Montelli et al., 2006). At ~ 19 cm/a, the propagation frequency of the Easter microwave is the highest on earth (Müller et al., 2008).

In the vernacular, the burrs Sala y Gomez and Nazca were commonly ascribed to the Nazca movement over a coat flag (Morgan, 1971). For such a flag, several topical locations have been proposed, among them one under Easter Island (Morgan, 1971), one under the island of Sala y Gomez (Ray et al., 2012), a 360 km of Sala y Gomez (O'Connor et al., 1995), one western of Easter Island (Haase et al., 1996) and one between Easter and Sala y Gomez (Montelli et al., 2006) (Figure 1).

Suberaerial volcanic activity on the crest was observed in the periods 0.13 - 2.4 Ma on Easter Island (O'Connor et al., 1995) and 1.3 - 1.9 Ma on the island of Sala y Gomez (Bonatti et al., 1977; Clark & Dymond, 1977). Sala y Gomez rividge and its westerly equivalent, the Pitcairn Gambier necklace, both cut the edge of the eggplant at the south end of the Easter microplate (Hey et al., 1995).

As the east ditch began to spread north, the micro plate began to develop at ~ 5. 2 Ma (Chron 3). It took up to ~ 2.5 Ma, during which the West Rift adapted by segmentation along new transformation errors. While the trans-pressive north border moved with the northerly migratory Ostgrabenspitze, the transtential south border stayed almost solid.

Ma to the north of the east ditch and the southwest ditch began to open along the Pacific-East trans-stensional transformation area. Pressurization took place along the north border when the Nazca panel was pushed over the microscope table. In Hagen et al. (1990) it was argued that this microtiter plates were induced by an outer flag, although this is not part of the general flag theory and microtiter plates are present only at other flag sites that have been nominated.

On the Nazca sheet itself there are other complexity, among them relic microtitre plates and dead spread centers (Ray et al., 2012). Further proposals for the origins of volcanic activity that formed the Easter-Sala y Gomez series are a "hot line" (Bonatti & Harrison, 1976; Bonatti et al., 1977), a leaking fault area ( "Herron, 1972; Clark & Dymond, 1977), an early dispersal centre (Mammerickx, 1981) and a litospheric dispersal area ( "Mammerickx & Sandwell, 1986).

Bathymnetic maps of a part of the vulcanic area, approximately 1,350 km long, showing the south part of the Easter micro-plate and the Easter and Saly and Gomez Isles, show that vulcanism is common, that the buildings are not distributed linearly and that some of the volcano crests are not under-parallel.

More than 3,000 different volcano centers (Liu & Naar, 1997a) and common igneous currents appear over large parts of the seabed, which are different from any other volcano range studied on the seabed (Liu & Naar, 1997b). Actual lithospherical resilient width along the entire length of the necklace, calculated by modelling the gravitational information, is ~1-4 km (Kruse et al., 1997).

RA et al (2012) reported 40Ar/39Ar decremental warming age measurements for basalt excavated from the crest eastward of Salas y Gomez Island, which includes the Nazca crest. With a few exemptions, they reported that the age increases from 1.4 to 30 Ma to the west (Figure 2). Fig. 2: 40Ar/39Ar Age from the mountain ranges eastward of Easter Island vs. along the Salas y Gomez range.

Fig. 3: Assumed age of the lower crust at the moment of the outbreak of volcano on Mount vs. removal of the sample point from the island of Sala y Gomez (by Ray et al., 2012). The Sala y Gomez Ridge is surrounded by flat vulcanic bands and two distinctive crests with flat peaks that rise to a depth of only 1500m.

On the west end of the mountain crest, the sea bed has an mean of 2,800 metres (Stoffers et al., 1994). This high topographical area is approximately parallelepiped to the directions of relativ movement between the Pacific and Nazca plate. There is a scattering of isles and sea mountains. Maya & Diament (1991) reported a large abnormal topographical characteristic around Easter Island (Figure 4).

Geographical coarseness mapping (Figure 5) shows that the Oster-Sala y Gomez back is a continual ribbon with a high topographical elevation of characteristics such as the seamount (Maia & Diament, 1991). Illustration 4: Bathymetry of the Easter Island area. The distance between the contours is 500 m. A = Australian archipelago; C = South Cook Islands; M = Marquesas archipelago; S = Society Islands; T = Tuamotu archipelago and plateau; A = Pitcairn-Gloucester orientation; SG = Easter-Sala y Gomez chains; N = Nazca ridges; M = 25°S ridges.

SG: Easter - Sala y Gomez necklace (Maia & Diament, 1991). The Easter Island is the result of three large vulcanic centers, namely Poike, Rano Kau and Terravaka. Fig. 6: Percentage of rocks from Easter Island, calculated from 200 specimens. In Ray et al. (2012), a shortage of time-progressive geochemistry gradients along the mountain crest eastward of Salas y Gomez was reported.

However, Glisovic & Forte (2014) reported that the provinces have a geometric imbalance with Pb, Sr and Nd isotopic analyses showing greater accumulation in the NE half of the Easter Island salas and Gomez crest than in the SW half. It has been construed within the framework of the flag theory in order to mirror the structures within the flag line.

For the Galapagos Islands, Harpp et al (2014) proposed a bilateral asymmetrical heterogeneous structure, which Glisovic & Forte (2014) ascribed to the geometric shape of the lower mantle's lower shell geochemistry reservoir ("Figure 7"). Within the framework of the Plate Theory this would be seen as a later variation of the flat top cladding structure.

Fig. 7: Illustration of a flag pattern to illustrate the Easter Salas y Gomez volcano ridge's bilaterally symmetric composition. Vulcanism that constructed the burr is ascribed to an origins in the deeper cloak with advancing exhaustion and blending with molten masses that originate from the exhausted top cloak during the interactions between plum and burr.

Both the geochemistry of the Easter and Galapagos system are more exhausted than other Pacific volcanoes. Both in the plume and in the plate hypothesis, a thin lithospheric layer allowing a flatter ascent would lead to a greater amount of melt, which in turn could lead to a larger proportion of the exhausted MORB spring in the lava composition.

Based on the assumption used, the EPR is directly above the east lobes of Pacific LLVSP. This was thought to drive the flux across the CMB coating to the substrate and replace the cooler and less compact jacket. Pitcairn Island. The heterogeneous nature of the sheath under the EPR was evaluated as part of this trial and a large area increase in buoyancy from the CMB to the Easter plate interface was proposed.

It has been construed as a thermic flag whose form differs with the deep, but which the last 65 Ma is based on (Glisovic & Forte, 2014). Montaggner (2002) used SEISOMOLOGY to identify low speed EW-oriented low speed and low speed channel anisotropies below Easter Island at dephts of < 370 km and to investigate relationships with past and present panel movements.

All the volcano crest, which extends from the south end of the Easter micro plate to the west end of the Nazca crest (Figure 1), has broken through and around an old fault area ((Figure 10). This rupture area is marked by misalignments in magnetical abnormalities and can be traced from the east end of the Easter Range to the Chilean rift.

Though very young basalt can be found on Easter Island, the volcano range and its equivalent, the Pitcairn-Gambier range western of the EPR, extends significantly to the EPR. Vulcanism was presumed to result from the transtention and "leakage" of the molten mass from the cladding through this permanent discontinuity at Menard & Atwater (1968; Herron, 1972; Clark & Dymond, 1977).

MRIs show that the rupture area on the right side was 18 - 7 Ma (Figure 1), but on the lefthand side since 5 Ma, the estimated point in the Easter microplate's formation. The largest part of Sala y Gomez Ridge originated in this "dark" age. Further instances of approximately time-progressive vulcanic burrs that have developed at fault areas are the Lakshadweep-Chagos Ridge (postulated that it is connected to a flag that is currently under Reunion Island) and the Ninety East Ridge (postulated that it is connected to a flag that is currently under Kerguelen Island), both in the Indian Ocean (see The Deccan beyond the plume hypothesis, Figure 5).

In the Easter area, a recent plate theory suggests that volcanic activity is associated with the structural imbalance that must characterize the south end of the Easter rotary micro-plate (Schilling et al., 1985). Reconstructs of the microtitre plate's tectonical past show that its south border was always influenced in extent (Rusby & Searle, 1995).

The strain must be several hundred kilometres around the microtiter plate. Relatively recent volcanic activity on Easter Island (~ 0.13 Ma; Baker et al. 1974) and the older volcanic activity on Sala y Gomez (~ 1.9 - 1.3 Ma) suggest the expansion area, which allows intra-plate volcanic activity up to 360 km away from the EPR, but is at a reduction at a range of 750 km.

Fig. 10: Easter - Sala y Gomez volcano range: Bathymmetry and geomagne. Sala y Gomez Island. For the explanation of the Easter - Sala y Gomez volcano range, both plum and plate-based assumptions were proposed. Problems with the Plane assumption are: the lack of a vertical rise and a tidal base at the old (eastern) end of the volcano sequence, which could be an incoming plum crest; seismic studies have not yet detected a plum-like texture that extends from the top to the core-shell limit; high swelling temperature for the volcanoes is not yet proven.

Every Easter - Sala y Gomez volcano range pattern must illustrate the most important observations from the area. That can only be declared as a chance in the flag mock-up; the mirror-image volcano crests emanating from the EPR to the western and eastern sides. There is no idea how this could be constituted by a flag several hundred kilometres eastward of the EPR; largely similar topographic characteristics around the southerly end of the Juan Fernandez micro plate, 950 km further southward on the EPR.

Forecasts and proofs for the Plate and Plume hypothesis. Easter Island Petrorology and Georochemistry. Bonatti, E., C. G. A. Harrison, D. E. Fisher, J. Honnorez, J. G. Schilling, J. J. Stipp and M. Zentilli (1977), Easter volcano necklace (South-East Pacific): Cloak hotline, J. Geophys.

Bonatti, E. and C. G. A. Harrison (1976), Sharp Line in the Earth's Earth's Earth's Mantle, Natur, 263, 402-404. The geochronology and petrochemicals of the Easter and Sala y Gomez Islands: implication for the formation of the Sala y Gomez Ridge. Unsspiked K-Ar dated young Loihi and Pitcairn vulcanic rock hotspot seams, J. Volc.

Reconstruction of the Cenozoic cloak: The Cenozoic evolution: Consequences for the dynamic of the coat flag under the Pacific and India plaques. Mutual interchange between the Easter flag and the spread shaft of the Easter plate, Nature 382, 344-346. Hagen, R.A., N.A. Baker, D.R. Naar und R.N. Hey (1990), A SeaMarc II study subsurface vulcanism près de l'île de Pâques, mars.

Kruse, S. E., J. Z. Liu, D. F. Naar, and R. A. Duncan (1997), Easter Sea Range Lithospheric Range Actual Resilient Width, J. Geophys. Top cladding low channel anisotropies below the Pacific Plate. Convective plume in lower coat, natural, 230, 42-43. Naar, D.F., and R.N. Hey, Easter Mike Plate Tektonic Evolutions, J. Geophys.

Easter volcanic time-space map, Earth planet. Ray, J. S., J. J. Mahoney, R. A. Duncan, J. Ray, P. Wessel and D. F. Naar (2012), Timology and Georochemistry of lava from the Nazca Ridge and the Easter Seamount Chain: a ~30 Myr Hot Spot Records, J. Pet. 53, 1417-1448. Rusby, R. I. and R. C. Searle (1995), A Story of the Easter Microdisk, 5. 25 Ma to date, J. Geophys.

H. Sigurdsson, A. N. Davis and R. N. Hey (1985), Easter microplatemaking, Motherhood, 317, 325-331. Geoology of young U-boat volcanos western Easter Island, Southeast Pacific, Mar.