Easter Island Timeline

Do you think the scientists will ever know how the humans lifted up those giant minds?

As religion evolved: Explanation of the dead, speaking idols and..... - Brian McVeigh

Wherefore have many worshippers - Moses, Old Testament prophesies, Zoroaster - claimed to have listened to God's expression? It is not surprising that antique civilisations have certain characteristics, such as the "living dead" (treatment of the deceased as if they were still alive); "talking idols" (care and nourishment of portraits); monuments of corpsearch and " deities " (pyramids, ciggurats, temples).

Initially suggested by neuropsychologist Julian Jaynes, this hypothesis posits that an early mindset existed: a "human" (the lefthand side of the brain) listened to the voice of "gods" or "ancestors" (the right hemisphere). It was this psychologic internalization of the sacred experiences that formed the foundation for the great faiths and philosophical ideas of the whole wide globe in India, China, Greece and the Near East in the midst of the first millenium BC.

Survival of Easter Island - Jan J. Boersema

Using scholarly research and historic resources, such as the maritime magazines of the Netherlands businessman who was the first in Europe to come to the island in 1722, Boersema shows that the deforestation did not endanger the island's diet and led to hunger and war. Based on historic and scholarly findings, Boersema shows how Easter Island societies reacted to changes in culture and ecology as they developed and survived.

Timeline and geochemistry of lavas from the Nazca Ridge and Easter Seamount chain: a ? Myr Hotspot Record | Journal of Petrology

Osterseekette and the Nazca Ridge are two of the most striking vulcanic characteristics on the Nazca Ridge. Due to the absence of geographical and geochronical information, many issues regarding their type and origins remain unanswered for large parts of both networks. The 40Ar-39Ar decremental heat ing-age regulations for dredging rock from volcanos eastwards of Salas y Gomez Island show that the aging is increasing from 1-4 to 30 Ma in the eastern part with very few exemptions, which confirms that the two tracks are part of the same hot spot trails and indicate a hot spot site near Salas y Gomez instead of below Easter Island about 400 km further ww.

The majority of the volcanos appear to have broken out on the seabed, which was 5-13 myr old, and there is no discernible systemic alteration of the seabed alteration at the point of sea mount form. At about 23 Ma the Nazca ridge stopped forming and that of the Easteramount chain began, which corresponds to a shift in the movement of the Nazca album.

Nd-Sr-Pb isotope composition is in the region of the previously recorded levels for the Easter Seamount volcanos in the western part of Easter Island; moreover, most of our clusters of datasets are in a relatively small part of this range[e.g. Nd-Sr(t) between +6-0 and +4-0]. In the absence of a mesochemical boundary along the Salas y Gomez eastern boundary, there is evidence that the ratios of these end links have not changed systematically over the years.

It is bounded by two microdisks (Easter and Juan Fernandez) and comprises two relic microdisks (Mendoza and Bauer) and three large Seamount necklaces (Easter SEAMOTS, Nazca Ridge and Carnegie Ridge) (e.g. Mayes et al., 1990; Naar & Hey, 1991; Liu, 1996). The Easter Salas Hot Spot is one of the few Pacific hot spots that Courtillot et al. (2003) indicates a deeper, lower coat source, which is referred to as "primary" host.

Volcanic activity at the Easter Salas Hot Spot has created two seamounts on the Nazca Plate: the Easter Mount Chain (ESC) and the Nazca Ridge (NR), which together make up a km km long hot spot path (Fig. 1). It is ?km?km long, km km19 broad, and tends approximately west-east of the East-Rift spread line of the Easter microplate towards the south end of the NR.

Peru-Peru-Chile Peru-Peru-Chile Graben (e.g. Woods & Okal, 1994) is located northeast of the east end of the escal to long and km km away. Satelite-supported Bathymetrie (Smith & Sandwell, 1997) of the SE Pacific Basin showing the Nazca Ridge, Easter Seamount Chain and other characteristics of the Nazca Platem.

The sites of the dredging sites from which specimens were taken from this report are identified. Except for those labelled DM (for R.V. Dmitry Mendeleev Cross 14) and GS (for GS7202), all specimens were gathered during the drift-expledition. A dotted line near SEAMOLUNT 115 coarsely indicates the border between NR and ESC, and the insert shows an increased elevation of the area of the elbows that connects the two.

Satelite-supported Bathymetrie (Smith & Sandwell, 1997) of the SE Pacific Basin showing the Nazca Ridge, Easter Seamount Chain and other characteristics of the Nazca Platem. The sites of the dredging sites from which specimens were taken from this report are identified. Except for those labelled DM (for R.V. Dmitry Mendeleev Cross 14) and GS (for GS7202), all specimens were gathered during the drift-expledition.

A dotted line near SEAMOLUNT 115 coarsely indicates the border between NR and the insert shows an increased elevation of the area of the elbows that connects the two. In spite of its importance as an important hot spot path, most of the ESC-NR system was not investigated in geochemical or dating terms, as only a few volcanos in the long part of Salas y Gomez were investigated.

This paper deals with these issues with new 40Ar-39Ar ages, main and micronutrients and Sr-Nd-Pb isotope datasets for lava excavated eastwards of Salas y Gomez (from 80-3°W-105-2°W; Fig. 1) during a 2001 ocean voyage and during three earlier ocean voyages (see rehearsal and analysis details).

Morgans ('72) proposed that a coat flag under Easter Island would create a hot spot and that the topographical characteristics of the island's linearity eastward and westward would be due to the movement of the Nazca and Pacific panels above the flag. 1995, mainly on the basis of their 40Ar-39Ar ages for several specimens from the European Space Station and one from the south-western end of the NR, indicated that the centre of the hot spot is below or slightly easterly of Salas y Gomez, which is 400 km eastward of the major Easter Island.

This hypothesis can be validated with our new geochronology datasets. Lava from Salas y Gomez and adjoining sea mounts achieve higher Pb and Sr and lower Nd isotope proportions than lava from ESC volcanos further westwards, as well as Easter Island, or from the cracks of the Easter microplate (Kingsley et al., 2002, 2007, and reference therein).

These observations were evaluated to back up the assumption that the centre of the hot spot is near Salas y Gomez and that the more western part of the Sun volcano is a consequence of the flag wall deflecting towards the east trench propagation line (Hanan & Schilling, 1989; Fontignie & Schilling, 1991; Kingsley & Schilling, 1998; Kingsley et al., 2002, 2007; Simons et al., 2002).

Haase & Devey (1996) and Haase et al (1996, 1997) reasoned that the centre of the hot spot is on or even slightly western of Easter Island. It was based on (1) the analysis that the composite Easter Island ages, and not Salas y Gomez, showed an ostensible Easter Island ages, (2) the greater Easter Island area, and (3) the higher Easter Island ages,

All the volcanos between the eastern ditch of the Easter microplate and Easter Island than between Easter Island and Salas y Gomez, and (4) the observations that some Easter Island lava Nd and Sr have isotope relationships in the value region of Salas y Gomez.

Available aging dates for lava from Easter Island (0-13-2-4 Ma; O'Connor et al., 1995) and Salas y Gomez (1-3-1-9 Ma; Bonatti et al., 1977; Clark & Dymond, 1977) are the same. Reconstruction of platy and platy movements (Okal & Cazenave, 1985; Naar et al., 1993; Kruse et al., 1997; Naar & Wessel, 2000; Harada et al., 2003) indicate that the hot spot centre is below Salas y Gomez, while seasonal surveys with limited frequencies of Montelli et al.

The Easter Island and Salas y Gomez (2006) favoured a coat flag with a diameter of 400 km, which is located at a location (27°S, 108°W) between Easter Island and Salas y Gomez, but nearer to Easter Island. Unfortunately, the necessary meteorological information to solve this problem is missing. In contrast to Morgan's (1972) flag theory, in which hot spots are fixated in relation to each other, current datasets and modelling give indications of inter-hot spot movements (e.g. Koppers et al., 2004; Wessel & Kroenke, 2009).

Modelling by Steinberger & O'Connell (1998) and Steinberger (2002) forecasts that Easter salas and Hawaiian hot spots are approaching the nearest of all the hot spots on the globe (about 2?cma-1). Since the propagation between the Pacific and Nazca plateaus were also the highest (- cma-1 ?cma northern of the Easter microplate; Müller et al., 2008), the times of well-dated volcanos in these volcano tracks have the ability to solve the movement between the hottests.

Here, too, the stratigraphic geochronology was too poor for the ESC-NR system. We' re using the new ages presented here to raise the problem of fixing hotspots in an upcoming post. So far biogeochemical datasets for ecoscavas are mainly limited to volcanos in the western part of Salas y Gomez and for the NR there are none (Bonatti et al., 1977; Clark & Dymond, 1977; Fretzdorff et al.

Seeberg, the most eastern of Kingsley, Schilling and associates, is at 102-2°W, while Haase and his associates focus on lava at 109-3°W (Easter Island) south. Additionally to Easter Island and Salas y Gomez Island datasets, Cheng et al. (1999) report on Sr and Nd isotopic relationships for nine seed mount specimens and Pb isotopic relationships for four of them from a longer 84-6°W section of the ecosystem.

A number of the above mentioned trials have seen systemic lengthwise fluctuations in the chemistry and structure of the isotope along the Salas y Gomez and Ostgraben link. Suggested end members are incompatible-element-worn jackets corresponding to those along the south East Pacific Rise (EPR) and the north part of the East Rift, and relatively incompatible with elements of flag jackets (e.g. Kingsley & Schilling, 1998; Cheng et al., 1999; Haase, 2002; Kingsley et al., 2007).

Specimens 206Pb/204Pb between 20-0 and 21-5, 87Sr/86Sr between 0-7030 and 0-7035 and ?Nd at +2. The specimens examined here were excavated from mounts between 19-45°S, 80-27°W and 26-35°S, 105-23°W. The majority were gathered in 2001 during stage 6 of the drift-expledition of R.V. Roger Revelle (Naar et al., 2002) (Table 1); the dates for these specimens are marked with the DRFT code in the tables 2-4.

The GS7202 sample is from the University of Miami sample library and was excavated by J. Dymond and J. Clark of Oregon State University. The other four specimens, which we used only for dateing, were taken from the DM14-1028 excavator of the R.V. Dmitry Mendeleev Kreuzfahrt 14 (provided by Debra Stakes, ship scientist).

We have, however, taken specimens from 12 NR-amounts ( "DRFT 79-112" excavator trains; Fig. 1 and Table 1) and from 13 mounts on the ESC just south of Salas y Gomez ( "DRFT 115-139" excavator trains; Fig. 1 and Table 1). The majority of the eruptive rock is either very fine-grained volcanic or plagioclasic-phyric cushion lava, many of them vector.

In addition to plagioclases, some specimens also contain olive oil and clinopyroxes. Nearly all magmatic specimens were crusted with fertiliromanganese. Nearly all magmatic specimens were crusted with fertiliromanganese. The DRFT specimens were gathered during the Drift 06 survey in 2001. Dmitry Mendeleev from R.V. and GS7202 from the University of Miami dredging group.

With DRFT 79-1, an accuracy of 30-0 Ma for the seamount is calculated using the age-distance relation in Fig. 3. Italic printed overall fusion altitudes are the best estimate for solid and matrix specimens with a 39Ar and 36Ar-rebound. The seabed's bottom - old Seeberg.

The DRFT specimens were gathered during the Drift 06 survey in 2001. Dmitry Mendeleev from R.V. and GS7202 from the University of Miami dredging group. With DRFT 79-1, an accuracy of 30-0 Ma for the seamount is calculated using the age-distance relation in Fig. 3.

Italic printed overall fusion altitudes are the best estimate for solid and matrix specimens with a 39Ar and 36Ar-rebound. The seabed's bottom - old Seeberg. 40 new 40Ar-39Ar in-cremental warming analysis were carried out on 28 seed mounts along the ESC-NR, resulting in crystallisation times between 1-? and 30-8 Ma.

Tables 1 and 2 show the sites and a compilation of the 40Ar-39Ar age group. Complete readings can be retrieved and retrieved from the EarthRef. org Digital Archive (ERDA) by simple search for specimen numbers or the name of sequential chain. You can download the datafiles in Microsoft Excel file formats.

40Ar-39Ar stage heater ostensible aging spectrum for plagioclass and ground mass sampling of dredging rock from the European Steam Scale (ESC and NR) (a-f). Platform aging (i.e. the weighting of the related, congruent stage aging, which accounts for >50% of the entire amount of emitted gas) is given. 40Ar-39Ar stage heater ostensible aging spectrum for plagioclass and ground mass sampling of dredging rock from the European Steam Scale (ESC and NR) (a-f).

Platform aging (i.e. the weighting of the related, congruent stage aging, which accounts for >50% of the entire amount of emitted gas) is given. 40Ar-39Ar stage heater for plagioclass and solid stone specimens from the excavated material class 40Ar-39Ar (a-d). You can see the name of the platform. 40Ar-39Ar stage heater for plagioclass and solid stone specimens from the excavated material class 40Ar-39Ar (a-d).

The age of the platform is indicated. Apparent changes were taken from the specimens with a stone saw. Afterwards, we comminuted the specimens with a china cheek-breaker, a high-grade grinding ring and partly a china manual morter until ??m% of the granules were screened into the 210-300??m group. A number of soil specimens were further treated with a Frantz magnet for the separation of plagioclases.

All specimens were purified in 1M liquid chlorine (60 min), 6M liquid chlorine (60 min), 1M HNO3 (60 min) and high-purity deionised hydrogenated liquid (60 min) in an ultrasound solution preheated to ?min°C. Plagioclas algae specimens were produced in the same way, except that the leachate contained an additional stage with min-5M HF (15 min) to softly remove the (altered) edges of the beads.

Predisposed specimens were radiated for 6-Renne et al., 1998 in the TRIGA nuclei of Oregon State University together with the FCT-3 biotope (28-03?±?-18 Ma, 1?). Radiated specimens were charged into a tube which was injected into the Ta pot of the oven or into a Cu-planchette in an ultra-high pressure test cell and scanned with a defocussed CO2-laserbeam in predetermined pattern and heats up over the specimen to evenly liberate the gas of Argon.

Concerning the admission times of the gaseous samples into the massprobe, the intensity of the peaks was decreased by means of straight or explicit curves. The Steiger & Jäger (1977) decomposition constant was used to calculate all age groups. Ingremental hotplate age and isochronal age were obtained as weighed averages with 1/http://earthref.org/tools/ararcalc. as weights (Taylor, 1997) and as YORK2 Least Squares Fit with corrected faults (York, 1969) using Koppers' ArArCALC v2.5 utility (2002) available on the http://earthref.org/tools/ararcalc. htm website.

Platform aging and isochrones with MSWD higher than the unit were used to indicate elevated dispersion due to geologic uncertainty beyond the accuracy of the incremental aging itself. Any error aged 40Ar-39Ar is indicated with a 95% probability of occurrence (2?), unless otherwise stated. Adjoining, coincident stage altitudes, especially over the medium to high range of temperatures of the gaseous emission spectra, constitute a platform era.

Dependable specimen cristallization is achieved when the platform and Isochronic AoAs are within the analytic insecurity and do not indicate significant occurrence of Ar originating from the cladding ("excess"). Calculating the entire melting time by adding all stage composition as if the experiments would consist of a simple one. U-boat specimens are usually subject to a certain (high) level of change.

E.g. DRFT 121-1 provided age from 19-01 -23 Ma (matrix) and 19-19 _09 Ma (plagioclase), and rock from GS7202 DR62-1 and 2 excavators were dating at 29-86?±?-29?Ma and 30-74?±?-80 Ma, respectively. Main and micronutrient levels (Table 3) and isotope proportions (Table 4) were determined at the University of Hawaii using phenocrystal-free hand-picked crystal chip or aluminum oxide powder from hand-picked hand-picked chip of the least modified, relatively phenocrystal-free holo-crystalline rock.

Before assembly, glass-chips were treated with 1-5M H2O, 1-5M HCI and 18 M??cm cmL water for majority elements or resolution for microelement and Nd-Pb-Sr isotope analisys. For most of the basic chemistry and isotope measurement, jars were used. Sawed plates of holo-crystalline stone were used for the other specimens.

Dehydrated plates were comminuted into shavings of 1-3?mm which were successively washed out in an ultrasound solution of 3M cool 3M acettic acids, 3M hydroxide and 1M hydroxyamine trihydrochloride to eliminate carbonates, phosphates, organics and ferromanganous oxide (each stage was permeated with flushing and ultrasound purification in water) before being pulverized for dry and Nd-Sr-Pb isotope analysis.

Sr, Pb and Nd spectra were analyzed for all specimens with split of the same resolution. Additionally, powder splitting of two of the most visually modified holo-crystalline specimens (GS7202-58, DRFT 121-1) was subject to a multistage, strongly sour leach-out process (Mahoney, 1987) only for Sr-isotopic analysis (see also note in table 4).

A Cameca SX-60 electronic micro probe was used to determine the essential content of elements in the sample area. For holo-crystalline specimens a Siemens 303-AS X-ray fluorescent analyzer was used. Neodyme, Sr and double-tip Pb isotopic ratios were measured on select specimens (Table 4) using a Mahoney et al. (1994, 2005) and Galer (1999) ionisation thermic mass spectrometry from the University of Hawaii.

The ages adjusted figures in Tab. 4 were computed using the parental and child elements concentration (Tab. 3 for Sm, Nd, Rb, Sr, U and Th and Tab. 4 for Pb) of the same powder samples used for chromatographic analyses. To correct the aging of the Sr and Rb ratio of the highly depleted cleavages of GS7202-58 and DRFT 121-1, the Sr and Rb concentration was obtained by diluting the isotopes (values see key in Tbl. 4).

The isotopic proportions observed (index m) were adjusted for ageing (t) using information from Chart 1 or, for excavator trains without 40Ar-39Ar information, from the best fitting line in Fig. 3. Figures are calculated in relation to the 87Sr/86Sr =n -710238 to -000014 (2Sr?, n =to ) for NBS987 Sr and 143Nd/144Nd =?-511843 to -000008 (2?, n = ; this insecurity is equal to to?±n?-2 ? units) for La Jolla Nd.

Pb ratio was determined using a double-tip multistatic sampling technique (Galer, 1999) at 5-10 ng samples; the error in the above given samples are less than or the same as the uncertainty of these ISO. In the case of DRFT 121-1, the concentration for the caustic splitting is Rb = -45Sr?, Sr = -69-68 Rb = -69 GmbH and for GS7202-58 Rb = -40COPY10.

86Sr was assayed on strong acids leach powder for these specimens and the aging adjustment uses the Rb and Sr concentration values obtained by diluting isotopes. The isotopic proportions observed (index m) were adjusted for ageing (t) using information from Chart 1 or, for excavator trains without 40Ar-39Ar information, from the best fitting line in Fig. 3.

Figures are calculated in relation to the 87Sr/86Sr =Nd -710238 -000014 (2Sr?, n =?) for NBS987 Sr and 143Nd/144Nd =n -511843 ?-00000008 (2?, n =n ; this insecurity is equivalent to to?±Nd?-2 ? units) for La Jolla Nd. Pb ratio was determined using a double-tip multistatic sampling technique (Galer, 1999) at 5-10 ng samples; the error in the above given samples are less than or the same as the standard's outside insecurities.

In the case of DRFT 121-1, the concentration for the caustic splitting is Rb =Rb -45Sr?, Sr = -69Sr?, and for GS7202-58 Rb = ppm-40Sr?, Sr = ppm-8Sr?. 86Sr was assayed on strongly acidic powder for these specimens and the aging adjustment uses the Rb and Sr concentration values obtained by diluting isotopes. Thirty two of the 40 NR and the 40 Excavator rock provided 40Ar-39Ar platform or isochronous aging (Table 2).

Specimens contained whole boulders as well as basal mass and plagioclaseparates. Generally, the specimens made good plateaus, which make up 90-100% of the overall atmosphere, and we consider these to be accurate estimations of the crystallisation time. Appropriate isochrons are congordant and have 40Ar/36Ar sections within the fault of atmosphere value. Old spectrum for several solid and base mass specimens show the effect of rebound (rearrangement of 37 Ar and 39 Ar atom during radiation ), characterised by declining stage aging with rising warming temperatures (e.g. DM14-1028-11 specimen in Fig. 3).

Recent sampling, GS7202-72-2, is from the Salas y Gomez U-boat Hill, while the oldest groups (29-9 -3 Ma and 30-8 -8 Ma) are for sampling from one of the two most easterly excavator locations on the NR (GS7202-62; Fig. 1). A clear, altogether straight line effect of aging east of Salas y Gomez exists, with the exception of two specimens (DRFT 84-1 and 85-1) of an NR mount with a platform aging of 4-5 Ma and 5-0 Ma in the middle of mounts with an aging of 24?Ma (Table 2).

So these anomalous young volcanoes are not related to the vulcanism that created the remainder of the NR; they are further debated in the following paragraphs. Deployment of 40Ar-39Ar age of NR, ESC and Easter Island (EI) igneous rock vs along the Salas y Gomez (SyG) removal chains. It also shows the dates for Lavafields and small Seeberge just westwards of EI.

Easter microplate lava from the east trench (ER-EMP) are rated at 0 Ma. All our values (plateau aging for all specimens from Table 2 except the overall fusion aging for DRFT 100-2 and isochronous aging for DRFT 115-2 and 126-1) are given by full circle and for two abnormally young NR specimens (DRFT 84-1 and 85-1) by hexaagons.

The open circle and other icons are dates from O'Connor et al (1995). Sloping continous and dotted line represents rectilinear corrections made using the York et al. (2004) algorithms on information for the ERC and NR, taking into account only the 2? defects by date (years) (i.e., provided that there is no significant defect in the excavator locations).

The regression does not include datasets for the anomalous young DRFT 84 and 85 specimens, EI and mounts and western of them. Deployment of 40Ar-39Ar age of NR, ESC and Easter Island (EI) igneous rock vs along the Salas y Gomez (SyG) removal chains. It also shows the dates for Lavafields and small Seeberge just westwards of EI.

Easter microplate lava from the east trench (ER-EMP) are rated at 0 Ma. All our values (plateau aging for all specimens from Table 2 except the overall fusion aging for DRFT 100-2 and isochronous aging for DRFT 115-2 and 126-1) are given by full circle and for two abnormally young NR specimens (DRFT 84-1 and 85-1) by hexaagons.

The open circle and other icons are dates from O'Connor et al (1995). Sloping continous and dotted line represents rectilinear corrections made using the York et al. (2004) algorithms on information for the ERC and NR, taking into account only the 2? defects by date (years) (i.e., provided that there is no significant defect in the excavator locations).

The regression does not include datasets for the anomalous young DRFT 84 and 85 specimens, EI and mounts and western of them. Most of the long-lasting basalt is of moderate development, transitioning to moderate alkaline basalt (MgO =--7 wt6%, TIO 2?=MgO?-4?wt%, K2O?=MgO?-5-1-MgO??wt%). However there are also some Tholeiite (DRFT 101-2 and 130-1, 130-4 and 130-5), more alkaline (Na2O + KO KO> -5 wt> -5 wt%; DRFT 84-1, 85-1, 115-1, 135-6 and GS7202-DR72-2) and more silicate compounds (especially DRFT 121-1, a trachyt with 64-50 wt% SiO2) (Fig. 5a).

Of the most alkaline specimens, a Tephritol and a Foidit (DRFT 84-1 and 85-1), the above anomalous young NR specimens are not clear whether they are an anomalous young seed mount or some kind of tapered volcanic activity on a much older (>24 Ma) seed mount. Three are Tholeiite and one is Tephritol, which is holistic crystalline.

Each of the four specimens contains olivin-phenocrystals. Overall, Mg#[=100 +/(Mg2+ +11 ?Fe+/ ), mole, suppose 85% of the entire Fe is Fe2+] ranges from 65 to 42, with a modus around 55, which reflects the fairly developed natures of most lava. There is no recognisable correlation between aggregate and sample site on a seamount such as the top vs. bottom flank.

Parenteraldehyde (a) compounds vs. silicic acid (% by weight) for glasses and holo-crystalline specimens. They were planted in Le Maitre (1989), and the border between subalkaline and alkaline lava composition for the Hawaiians was drawn by Macdonald & Katsura (1964). Specimens with composition outside the box for bass are inscribed. Tephrit DRFT 84-1 and Foidit DRFT 85-1 from the young NR mount are shown with hexaagons.

Datapoints for modified specimens that are outside the trends are marked in corresponding boxes. Parenteraldehyde (a) compounds vs. silicic acid (% by weight) for glasses and holo-crystalline specimens. They were planted in Le Maitre (1989), and the border between subalkaline and alkaline lava composition for the Hawaiians was drawn by Macdonald & Katsura (1964). Specimens with composition outside the box for bass are inscribed.

Tephrit DRFT 84-1 and Foidit DRFT 85-1 from the young NR mount are shown with hexaagons. Datapoints for modified specimens that are outside the trends are marked in corresponding fields. All of these specimens (DRFT 112-1, DRFT 130-5, GS7202-58) contain ample amounts of phosphorous, and one of the most remarkable properties in the columns used is the extremely high concentration of phosphorus in relation to the concentration of similar incompatible substances, such as Nd and Zr.

Additionally, a mixture of high V in relation to Th and Nb (DRFT 112-1, GS7202-58), high C in relation to Th and Nb (DRFT 130-5, GS7202-58) and/or low Na2O is present for a given MgO concentration (DRFT 112-1, GS7202-58; Fig. 5f). The DRFT 112-1 sample also has a significantly higher Pb concentration compared to Nd, Pr and Ce.

Pb is even greater in another DRFT 131-1 dry solid probe, which has only a moderate P2O5 uptake. In two further stone specimens, Phonotephrit DRFT 115-1 and DRFT 127-1 base, the ratio of Th and Nb is low compared to Th and Nb (Th/U =U -30 and 6-45 respectively); this may be a change effect from a suberaerial decomposition state or a consequence of our specimen purification and leach-out.

Although the rock ranges from alkaline to tholeitic, the results indicate moderately correlated MgO with CaO, Na2O, K2O, SiO2 and CaO/Al2O3 when the presence of foido and tephrites and the modified specimens mentioned above are ruled out (Fig. 5b, d, f). Coarse adverse cross-relation is also seen for P2O5 vs. MgO, with the exclusion of the DRFT 121-1 trachyt; the very low P2O5 (0-05 wt% at MgO of 0-51 wt%) of this developed volcanic eruption is compatible with avatite harvest.

It was Pan & Batiza (1998) who saw a similar outcome for escal lava westwards of Salas y Gomez as proof of a series of medium fractionating and smelting pressure. Large oxidation of the transition and alkali basalt is similar to that of Salas y Gomez (Haase & Devey, 1996; Haase et al., 1997; Pan & Batiza, 1998).

Like the western lava, the Na2O, Na2O3 and K/Ti levels of our specimens are generally higher at a given MgO concentration than at basalt from the south of the lava and cracks from the Easter microplate. Fig. 6 compared the Na2O, SiO2 and CaO/Al2O3 levels on 8 wt% in order to minimise the effect of flattening.

The most of our specimens from the NR and ESC eastwards of Salas y Gomez are, like most from the ESC westwards of Salas y Gomez with relatively low (CaO/Al2O3)8 and (SiO2)8 for a given value of (Na2O)8[also the levels of (FeOT)8 are tending to be higher, but the absence of FeOT with MgO makes the computation and reading of (FeOT)8 difficult for these specimens].

This difference is in line with smaller mean quantities of part melts and larger mean melt depth for lava of the NR and ESC located to the west of Salas y Gomez than for basalt of the south of the MPR and cracks of the Easter microplate. Fig. 7 shows prestigious primitive-mantle-normalized, non-compatible patterned elements as well as mean samples for OIB and standard and incompatible elements enhanced mid-oceanic crest basalt (N- and E-MORB).

DRFT 101 and 130 Tholeiite show similar pattern as N-MORB, with relatively impoverishment in the high degree of incompatibility (e.g. primary coat normalised (La/Lu)p = -35 in DRFT 101-2], but all other laves are relatively accumulated in the high incompatibility similar to the most common OIB or E-MORB (La/Lu)p between 1-7 and 9-2; the DRFT 85-1 Foidit has a value of 26].

Laven generally show the highest concentration of Nb and Ta, a property of many OIB. Crucibles in Ti (e.g. DRFT 85-1, 121-1, 135-4 and GS7202-72-2), as well as Sr ( e.g. DRFT 121-1, 127-1 and 127-4) and Sr (e.g. DRFT 121-1, 127-1, 127-4 and 135-4) in different samples indicate significant monitoring of oxides, apatites and plagioclases.

Primitively -mant-normalized incompatibles of elements from different parts of the NR and ESC. Primitively -mant-normalized incompatibles of elements from different parts of the NR and ESC. For the DRFT 121-1 trachytes, the most distinct trays in P, Ti and Sr can be seen (Fig. 7b). The developed specimen also has the highest inflammation-weakness rate of any of our specimens (6-07 wt %), but its incompatibility does not have the characteristic properties of other modified specimens, such as DRFT 112-1.

Instead, unlike our other specimens, the DRFT 121-1 has a large sample tray at Ba. The correlation between the proportions of the incompatibles is similar to that found by former ESC operators just outside Salas y Gomez (Fig. 8a-d), but in some proportions shows slightly more variation, especially in those that are the more change-sensitive ones in the solid specimens (e.g. U in Nb/U, Fig. 8c).

Like many other hot spots, almost all of our hot spots are in the Nb/Y vs. Zr/Y area, determined by the lava of the arctic hot spot (Fig. 8d). Only exception are the N-MORB-like Tholeiite Basalt (DRFT 101-2 and three DRFT 130 samples), whose value is below this N-MORB.

Figures for two sea mountains westward of Easter Island (Haase & Devey, 1996) and one Easter Island rhyolith (Haase et al., 1997) are also significantly below the Icelandic area. NR & E. ESC' and'DRFT 84 & 85' are figures from this study;'W. ESC, literally " means literary information for the ESC western of Salas y Gomez (Haase et al., 1996, 1997; Haase & Devey, 1996) and "Cheng" means the information from Cheng et al.

The proportions in (a), (b) and (d) were selected to contain items jointly analysed by different operators, while in (c) only the NR & E. ESC and solid rocks (wr) are used. NR & E. ESC' and'DRFT 84 & 85' are figures from this study;'W.

ESC, literally " means literary information for the ESC western of Salas y Gomez (Haase et al., 1996, 1997; Haase & Devey, 1996) and "Cheng" means the information from Cheng et al. The proportions in (a), (b) and (d) were selected to contain items jointly analysed by different operators, while in (c) only the NR & E. ESC and solid rocks (wr) are used.

One important distinction between our specimens and ESC laves located to the east of Salas y Gomez is that our results show no overall association of chemistry with the position of the sail mount (Fig. 9a-f). These results contrast with the longitudinal trend between the East Rift and Salas y Gomez (Haase & Devey, 1996; Pan & Batiza, 1998; Kingsley et al., 2007).

micronutrient (a-d) and isotope proportions (e, f) vs along the SyG large diameter spacing. As shown in Fig. 8, the source of the information is shown. micronutrient (a-d) and isotope proportions (e, f) vs along the SyG large diameter spacing. As shown in Fig. 8, the source of the information is shown. Fig. 10 contrasts our adjusted Sr-Nd-Pb isotope values with already released values for the EPC, the SPR and youth (ca. 0-4 Ma; Haase et al.

2000 ) San Felix and San Ambrosio isles, which are about 200?km SE of the ESC-ESC?NR 'Elbows' in the ESC-NR-System. Fig. 11 compares the agesighted Nd-Pb isotope datasets of Sunnydale's ecosystem and NR with those for the Hawaii and Samoa Isascots.

Overall, the different isotopic relationships are very strongly correlated, and the entire area of our data[?Nd(t) = +8-7 to +2-9, (206Pb/204Pb)t = -709-20-012 and, with three exeptions, (87Sr/86Sr)-t =--70270-0-70388] is similar to the previously observed ecc area, which is almost entirely 30 Ma, hot spot trails and coincide with a hot spot centre near the island Salas y Gomez.

It seems that the location of the hot spot in relation to the Pacific-Nazca propagation line changed over a fairly narrow area during the building of the oriental seed mounts (i.e. eastwards of Salas y Gomez) and generally of the NR, as most lava on the seabed were between 5 and 13 myr old.

This is also the case for the ESC just south of Salas y Gomez, but some of these lava seem to have been placed on the younger seabed, probably nearer to the propagation centre. The most lava eastwards of Salas y Gomez are moderate alkaline to transition-basalt. The isotope composition is in the region of the values previously obtained for the occidental ESC volcanos and indicates that the cladding spring has been composed of the same two main constituents for at least 30 Ma.

Most of our clusters, however, are in a relatively small isotope range[e.g. ?Nd(t) +4 to +6] nearer to the derived C/FOZO-like compound. This latter version corresponds to the rather low distribution of seabed age at the point of volcanic activity (i.e. the separation of a sail mount from the expansion axis) for most of our reample.

It' s possible that similar laves are also found along the east side of the East side of the river but few have been found because we have focused our excavation work on the top slopes of the bigger sea mountains. Thank you Doug Pyle, Kevin Johnson and Hetu Sheth for their help with excavation and subsampling, and Kent Ross and Denys Vonderhaar for their assistance with the analysis of sample chemistry at the University of Hawaii.

Thanx to Debra Stakes for rehearsals from R.V. Dmitry Mendeleev CRUCK 14, Jim Natland for GS7202 rehearsals from the University of Miami Excavator Rocks and Charles Lesher for the REEBOX programme. Vol. ratio in basaltic glass from the Salas y Gomez coat vane in interaction with the East Pacific Rise: Waters from old D-rich recovered scab or virgin waters from the lower coat?