Macdonald seamount

Macdonald seamount was discovered in 1967, when hydrophones noted earthquake activity in the area.^[2] The seamount was named in 1970 after Gordon A. Macdonald.^[3] It is also known as Tamarii,^[4] while MacDonald appears to be an incorrect capitalization.^[3]

The Pacific Ocean is characterized by long island chains, which typically extend from the southeast to the northwest in direction of the motion of the Pacific Plate. Often, such chains begin in the southeast with volcanoes such as Hawaii that become progressively more eroded northwestward and eventually end as series of atolls. This has led to the suggestion that they are formed by deep sources over which the Pacific Plate drifts and eventually carries the volcano away from its magma source.^[5] These sources are known as "hotspots", and their total number has been estimated to be between 42 and 117.^[6] Hotspots may also be formed by cracks propagating in the crust, and such hotspots would not necessarily show an age progression.^[7]

Macdonald seamount is located off the southeastern end of the Austral Islands.^[8] The Austral Islands extend away from the southern Cook Islands to Îles Maria and eventually Marotiri southeastward,^[5] including the islands Rimatara, Rurutu, Tubuai, Raivavae and Rapa.^[9] A relatively large gap separates Marotiri from the Macdonald volcano.^[10] The Ngatemato seamounts and Taukina seamounts lie north of Macdonald,^[11] they are considerably older and appear to have a very different origin.^[12] Even farther southeast lies the Foundation seamount chain,^[13] and the associated hotspot may have generated some of the seamounts close to Macdonald.^[14]

The seamount lies close to the southeastern end of an area of shallower ocean, which extends northwestward towards Marotiri,^[15] and includes Annie seamount, Simone seamount and President Thiers Bank.^[16] The 3,000 metres (9,800 ft) high Ra seamount (named after Polynesian term for "sun") rises 100 kilometres (62 mi) northwest of Macdonald to a depth of 1,040 metres (3,410 ft); it is apparently an extinct volcano and may have once emerged above sea level.^[17] A smaller seamount, Macdocald, rises from the southern foot of Macdonald 850 metres (2,790 ft) to depths of 3,150 metres (10,330 ft).^[18] Additional small seamounts that appear to have formed at the East Pacific Rise are also found in the area.^[19] The crust beneath Macdonald is of Eocene age,^[4] and away from the area of shallower ocean it is covered with hills and sediment.^[20]

Macdonald seamount rises 4,200 metres (13,800 ft) from the seafloor to a depth of about 40 metres (130 ft) below sea level;^[21] surveys in 1979 found a pinnacle reaching to a depth of 49 metres (161 ft) below sea level^[22] and a 150 by 100 metres (490 ft × 330 ft) wide summit plateau with small (6 metres (20 ft) high and 3 metres (9.8 ft) wide) spatter cones.^[23] Other sources indicate a surface area of 2.4 square kilometres (0.93 sq mi) for the summit plateau.^[24] Ongoing volcanic activity may have modified the topography of the summit of Macdonald between surveys in 1975 and 1982, forming another elliptical pinnacle reaching a depth of 29 metres (95 ft) at the northwestern margin of the plateau and raising the summit plateau to depths of 50–34 metres (164–112 ft).^[23] By the time of a new survey in 1986, the pinnacle had been replaced by a pile of rocks which only reached a depth of 42 metres (138 ft).^[25]

The upper parts of the edifice are covered by 50 centimetres (20 in) thick lapilli with lava flows underneath. Some hydrothermal alteration products are also found,^[17] and a thick ash cover occurs to depths of 2,000 metres (6,600 ft).^[26] Aside from these lapilli deposits, scoriaceous lava flows are exposed on the edifice as well.^[27] Farther down, lava flow fronts form scarps which become particularly noticeable at depths of 620–1,000 metres (2,030–3,280 ft), except on the northern flank. Even deeper, pillow lavas predominate.^[28]

Below the summit area, the slopes fall down steeply to a depth of 600 metres (2,000 ft) and then flatten out.^[17] Save for a debris-covered ridge to the northwest, Macdonald has a circular shape,^[29] with a width of 45 kilometres (28 mi) at a depth of 3,900 metres (12,800 ft). The slopes of Macdonald display radial ridges which may reflect tectonically-controlled rift zones, as well as isolated parasitic cones.^[17] The volume of the whole edifice has been estimated to be 820 cubic kilometres (200 cu mi).^[24] Macdonald seamount bears traces of landslides, including collapse scars up on the edifice and smooth terrain formed by debris on its lower slopes;^[30] collapses have been inferred on the eastern, southern, western and northwestern flank.^[31] The seafloor further shows evidence of turbidity currents, including ripples.^[30]

Geomagnetic analysis of the edifice has demonstrated the existence of a normally magnetized structure at the base of the volcano and an additional anomaly which seems to be the magma chamber at a depth of 2 kilometres (1.2 mi) within the edifice, close to the northern flank.^[32] Data obtained in gabbroic rocks expelled by the volcano during its eruptions also suggest that another magma reservoir exists at depths of 5 kilometres (3.1 mi), that is within the crust beneath Macdonald.^[33]

Macdonald has principally erupted basalt. This basalt contains phenocrysts of clinopyroxene, olivine and especially plagioclase.^[34] Additional rocks are basanite, mugearite,^[26] picrite^[35] and tephrite.^[36] The overall composition is alkaline^[4] and nephelinic.^[37] Rock debris found on Macdonald seamount includes intrusive rocks such as gabbro, metadolerite, picrite and pyroxenite;^[28] the gabbros appear to originate from slow crystallization of basaltic magma^[38] within a magma reservoir, followed by low temperature alteration.^[39] Such rocks were uprooted by explosive activity. In addition, hydrothermal and thermal alteration has formed amphibole, chlorite, epidote, phyllosilicates, pyrite, quartz and smectite,^[34] with additional components including albite, biotite, labradorite, leucodiorite and orthopyroxene.^[40]

The vulcanites are typical ocean island basalts,^[41] whose alkaline nature is unlike the tholeiite that is found on other hotspot volcanoes such as Hawaii, Iceland and Reunion. In these volcanoes alkaline lavas are erupted in the post-shield stage but Macdonald is clearly a developing volcano, and further research is needed to explain the chemical history of Macdonald.^[42] These magmas in the case of Macdonald were derived from the partial melting of spinel-lherzolite and further influenced by fractional crystallization^[36] and carbon dioxide,^[37] but with no influence of the overlying plate.^[43]