Kerguelen Plateau

Topography of the Kerguelen Plateau. On either side of the Central Kerguelen Plateau, the Elan Bank and William Ridge protrude west and east.
Location of the plateau - white spot is Kerguelen Island

The Kerguelen Plateau (/ˈkɜrɡələn/, /kərˈɡlən/) is an oceanic plateau and a large igneous province (LIP) in the southern Indian Ocean. It is also a microcontinent and submerged continent. It lies about 3,000 km to the southwest of Australia and is nearly three times the size of Japan. The plateau extends for more than 2,200 km in a northwest-southeast direction and lies in deep water.

The plateau was produced by the Kerguelen hotspot, starting with or following the breakup of Gondwana about 130 million years ago. There is a small portion of the plateau that breaks sea level, forming the Kerguelen Islands plus the Heard and McDonald Islands. Intermittent volcanism continues on the Heard and McDonald Islands.

    Geographical extent

    Symmetrically located across the Indian Ocean ridge and due west of Australia is the Broken Ridge underwater volcanic plateau, which at one time was contiguous with the Kerguelen Plateau prior to rifting by the mid-ocean ridge.

    To the north of Broken Ridge lies the linear Ninety East Ridge which continues almost due north into the Bay of Bengal and is considered to be a hotspot track.

    One of the largest LIPs in the world, the Kerguelen Plateau covers an area of 1,250,000 km2 (480,000 sq mi) and rises 2,000 m (6,600 ft) above the surrounding oceanic basins.

    Located on the Antarctic Plate, the Kerguelen Plateau is separated from Australia by the Southeast Indian Ridge (SEIR) and from Africa by the Southwest Indian Ridge (SWIR). These two ridge meet at the Rodriguez Triple Junction. It is separated from Antarctica by and the Cooperation Sea. The eastern margin north of the William Ridge is steep and formed during the break-up between the Kerguelen Plateau and the Broken Ridge. The southern part of the margin is separated from the Australian-Antarctic Basin by the deep .

    Geological history

    The Kerguelen Plateau is surrounded by the Crozet Basin, Australia-Antarctica Basin, Labuan Basin, and Enderby Basin.

    From the initial opening of the Indian Ocean until present, the Kerguelen hotspot has produced several now widely dispersed large scale structures. The Southern Kerguelen Plateau (SKP) formed 119-110 Ma; the Elan Bank 108-107 Ma; the Central Kerguelen Plateau (CKP) 101-100 Ma; the Broken Ridge (connected to CKP before the Eocene break-up) formed 95-94 Ma; the Skiff Bank (east of Kerguelen archipelago) 69-68 Ma; Northern Kerguelen Plateau (NKP) 35-34 Ma; Ninety East Ridge formed 82-38 ma north to south; the (western Australia) formed 132-123 Ma; the Rajmahal Traps in north-east India 118-117 Ma; and finally lamprophyres in India and Antarctica 115-114 Ma.

    India-Australia break-up

    The oldest volcanism that can be attributed to the Kerguelen plume are the Bunbury Basalt in south-western Australia (132–123 Ma) and the Rajmahal Traps in eastern India (118 Ma). The formation of the oldest portion of the Kerguelen LIP and these continental basalts are linked to the opening of the eastern Indian Ocean. The Bunbury Basalt is not of flood basalt dimension which suggest that the mantle underlying the newly formed Kerguelen hotspot was neither significantly hot, wet, or voluminous. In contrast, the magmatism that produced the Australia-India break-up 136-158 Ma created the Wallaby Plateau, but no known hotspot has been linked to this event.

    India-Antarctica break-up

    The output from the Kerguelen hotspot peaked 120-95 Ma, 12-70 Ma after the India-Antarctica break-up. No ridges or hotspot tracks such as Walvis-Rio Grande, Chagos-Laccadive, have been found in the between SKP and Antarctica or along India's conjugate eastern continental margin. The relation between the Kerguelen hotspot and these continental break-up and volcanic margins is instead similar to that between the Réunion hotspot and the Deccan Traps and the break-up between western India and the Seychelles.

    The peak output of the Kerguelen hotspot coincides with one or several microcontinent formations, such as the Elan Bank. Since the Indian Ocean began to open about 130 Ma, the Kerguelen hotspot has moved 3-10° southward and, consequently, the spreading ridge between India and Antarctica has jumped northward one or several times. Parts of the Kerguelen Plateau, the Elan Bank and the SKP, were originally attached to India and are composed of continental lithosphere. One or several ridge jumps transformed the Elan Bank into a microcontinent and dispersed continental fragments in the SKP, and these structures were eventually left behind as India moved northward. The ridge jump that made the Elan Bank a microcontinent occurred after 124 Ma. The construction of the SKP 118–119 Ma contributed to the oceanic anoxic event 1.

    Around 83.5 Ma sea floor spreading between India and Antarctica was asymmetric in the Kerguelen Plateau region with two-thirds of the sea floor created being added to the Antarctic Plate. A ridge jump eventually resulted in parts of the Kerguelen Plateau being transferred from the Indian to the Antarctic Plate.

    Cenozoic volcanism

    The Kerguelen hotspot produced the 5,000 km (3,100 mi)-long Ninety East Ridge 82-38 Ma, and geochemical evidence suggests that this occurred at or near a spreading ridge. The lack of a conjugate structure on the Antarctic Plate, however, makes it unlikely that the hotspot was located at a spreading ridge during this long period. As the Antarctic Plate then moved over the Kerguelen hotspot the NKP formed over relatively old oceanic crust. Flood basalts in the Kerguelen archipelago formed 30-24 Ma and less voluminous and more recent volcanism occurred until 1 Ma. During the last 21 Ma volcanic structures have formed on the CKP, including Heard Island, and both Heard and McDonald Islands have had recent eruptions.

    65 Ma, the CKP-Broken Ridge LIP was located near the Kerguelen plume and the plate boundaries of the Indian Ocean. The LIP was the product of 25 Ma of relatively high magmatic activity followed by a 40 Ma period of lower activity.


    Schlich et al. 1971 described tilted basement blocks near the Kerguelen archipelago and was the first to identify the Kerguelen Plateau as of continental origin, in contrast to other LIPs.

    The presence of soil layers in the basalt with included charcoal and conglomerate fragments of gneiss indicate that much of the plateau was above sea level as what is termed a microcontinent for three periods between 100 million years ago and 20 million years ago. Large parts of the now submarine Southern (SKP) and Central Kerguelen Plateaus (CKP) were subaerial during the formation of the LIP. The SKP probably formed an island of 500,000 km2 (190,000 sq mi) with major peaks reaching 1–2 km (0.62–1.24 mi) above sea level.

    The Kerguelen microcontinent may have been covered by dense conifer forest in the mid-Cretaceous.

    It finally sank 20 million years ago and is now 1 to 2 km (0.6 to 1.2 mi) below sea level.


    During the austral summer there is a high density of baleen whales, such as sperm, minke, and humpback, along the southern end of the Kerguelen Plateau and the northern part of the adjacent Princess Elizabeth Trough. These whales choose this location for foraging because the Southern Front of the Antarctic Circumpolar Current is steered off by the plateau — resulting in a poleward extent for the Southern Front only found near the Kerguelen Plateau. This brings shoaled, nutrient-rich Upper Circumpolar Deep Water to the surface which brings macro-nutrients to the surface. Ice is additionally advected north along the eastern side of the plateau.

    See also

    • List of Antarctic and subantarctic islands