Mount Melbourne

Not to be confused with Melbourne, Victoria, Australia.

For other uses, see Melbourne (disambiguation).

Mount Melbourne
Mount Melbourne seen from the ice-covered Ross Sea
Highest point
Elevation	2,730 m (8,960 ft)
Prominence	1,699 m (5,574 ft)
Listing	Ultra
Coordinates	74°21′S 164°42′E
Geography
Mount Melbourne Victoria Land, Antarctica
Geology
Age of rock	Unknown
Mountain type	Stratovolcano
Volcanic belt	McMurdo Volcanic Group
Last eruption	1892 ± 30 years

Mount Melbourne is a massive stratovolcano that makes up the projection of the coast between Wood Bay and Terra Nova Bay, in Victoria Land of Antarctica. It was discovered in 1841 by James Clark Ross.

Description

Mount Melbourne lies in North Victoria Land, facing the Wood Bay of the Ross Sea. To the southeast lies Cape Washington and due south lies Terra Nova Bay; Campbell Glacier runs west from the volcano. The seasonal Italian Zucchelli Station lies 40 kilometres (25 mi) from the volcano, the Korean Jang Bogo Station is also in the area and the German Gondwana Station is even closer; the volcano can be accessed from the two stations by helicopter, which is also the normal way to access the summit. Mount Melbourne was first recognized as a volcano by James Ross in 1841 and named after then-prime minister of the United Kingdom Melbourne. The volcano and its surroundings were investigated by New Zealand based parties in the 1960s, by German ones in the 1970-1980s and by Italian-based parties in the 1980s-1990s.

Mount Melbourne is an elongated stratovolcano formed by lava flows and tephra fall deposits, with gentle slopes. The volcano is uneroded and forms an almost perfect cone. Viewed from distance Mount Melbourne has a nearly perfect cone-like profile that has drawn comparisons to Mount Etna in Italy and Mount Ruapehu in New Zealand. The total volume of the edifice is about 180 cubic kilometres (43 cu mi). Part of the edifice rises from below sea level. Volcanic mounds, cones, lava domes and scoria cones dot its flanks; 6.4 kilometres (4 mi) from the summit is a large parasitic vent on the north-northeastern slope, which generated several lava flows. Pyroclastic flow deposits have also been reported, a rarity for Antarctic volcanoes.

A 1 kilometre (0.62 mi) wide caldera sits at the top of the volcano. The highest point of the volcano lies east-northeast of the caldera and reaches 2,733 metres (8,967 ft) elevation. The caldera has an incomplete rim and is filled with snow, leaving a 500 metres (1,600 ft) wide depression. The rim of the caldera is covered by volcanic ejecta including lapilli and lava bombs, probably the products of the most recent eruption of Mount Melbourne, which cover a 15 metres (49 ft) thick layer of pumice lapilli. Three small, nested craters formed by phreatomagmatic eruptions occur on the southern rim of the summit caldera. Pyroclastic fall deposits crop out in the northern rim of the caldera and there are more alternating lava-tephra sequences elsewhere in the summit region. There is evidence of past structural instability (collapse structures) on the eastern and southeastern flank and an arcuate 50–100 metres (160–330 ft) high scarp on the eastern flank appears to be an incipient sector collapse.

Except for geothermal areas, the ground is bouldery. Frost heave has been observed in the summit region. Small creeks flow down the eastern flank of Mount Melbourne; they are fed by meltwater during summer and quickly disappear together with the snow.

The mountain is covered with permanent ice, which extends to the coast and leaves only a few exposures of the underlying rock; rocky outcrops are best exposed on the eastern flank. The caldera hosts a nevé that generates a westward flowing glacier. An ice fall lies northwest of the caldera. Glaciers emanating from snowfields on the volcano have deposited moraines. Moraines and tills from both Pleistocene and Holocene glaciations crop out at Edmonson Point. Tephra layers crop out in ice cliffs and seracs and testify to recent eruptions, including the one that deposited the ejecta and lapilli pumice units on the summit; tephra bands are also found in other glaciers of the region. They form when snow accumulates on top of tephra that fell onto ice. Volcanic sediments from Mount Melbourne are also found in Terra Nova Bay.

Mount Melbourne is surrounded by a volcanic field consisting of 60 exposed volcanoes, which have the form of scoria cones and tuff rings with hyaloclastite deposits, lava flows and pillow lavas. Some of these volcanoes formed under ice. The volcanic field forms a peninsula which is separated by steep faults from the Transantarctic Mountains to the north. Among these volcanoes is Shield Nunatak southwest from Mount Melbourne, a subglacial volcano, now exposed, that may have formed during the latest Pleistocene. The Cape Washington ridge consists mostly of lava, including pillow lava, overlaid by scoria cones, and is the remnant of a shield volcano. Edmonson Point is another volcanic complex in the system that formed partly while interacting with glaciers and partly through phreatomagmatic activity. Other volcanoes in the field are Baker Rocks, Oscar Point and Random Hills. These volcanoes are aligned mainly in north-south direction and include both edifices that formed above and under ice, with palagonitized outcrops that expose dikes. Perfectly preserved scoria cones occur at Pinkard Table north of the volcanic field, while Harrow Peak is a heavily eroded lava plug. The total volume of volcanic rocks is about 250 cubic kilometres (60 cu mi) and their emplacement apparently altered the path of the Campbell Glacier. North of the volcanic field lies the Tinker Glacier.

Topographic map of Mount Melbourne (1:250,000 scale) from USGS Mount Melbourne

Geology

Mount Melbourne is part of the McMurdo Volcanic Group and together with Mount Erebus one of its active volcanoes. This volcanic group is one of the largest alkaline volcanic provinces in the world, comparable with that of the East African Rift, and is subdivided into the Melbourne, the Hallett and the Erebus volcanic provinces. The volcanic group consists of large shield volcanoes mainly near the coasts, stratovolcanoes and monogenetic volcanoes.

Volcanic activity of the McMurdo Volcanic Group is tied to continental rifting and commenced during the Oligocene. The West Antarctic Rift is one of the largest continental rifts on Earth but little known and possibly inactive today. The Ross Sea and the Victoria Land Basin developed along this rift and were deeply buried, while the Transantarctic Mountains were rapidly uplifted during the last 50 million years and are located on the "shoulder" of the rift. The line separating the two is a major crustal suture, with large differences in elevation and crustal thickness across the suture. Many of the volcanoes appear to have formed under the influence of fault zones in the area and increased activity in the last 30 million years has been correlated to the reactivation of faults.

Mount Melbourne and its volcanic field are emplaced over a basement of Precambrian to Ordovician age, which consists of volcanic and metamorphic rocks of the Wilson Terrane. The volcano is located at the intersection of three geological structures; the Rennick Graben of Cretaceous age, the Victoria Land Basin and the Polar 3 magnetic anomaly, which has been interpreted to be either a transform fault or a push-up structure formed by faulting. The Terror rift in the Victoria Land Basin runs between Mount Melbourne and Mount Erebus and appears to be related to their existence. The volcano appears to rise in a graben whose marginal faults are still active with earthquakes, on the eastern flank of Mount Melbourne. North-south trending faulting may also be responsible for the north-south-like trend in edifice structure, and strike-slip faulting takes place on the eastern flank. Holocene coastal uplift in the area indicates that tectonic activity is still ongoing.

It is part of a volcano alignment that includes The Pleiades (volcano group) and Mount Overlord, which together with the Malta Plateau form the Melbourne province of the McMurdo Volcanic Group. This province consists of the large stratovolcanoes Mount Rittmann, Mount Overlord, Mount Melbourne and The Pleiades, as well as numerous smaller volcanic centres, volcanic intrusions and sequences of volcanic rocks, and has been active for the past 25 million years.

Low seismic velocity anomalies have been found underneath Mount Melbourne and are connected to similar anomalies under the Terra Rift. A low gravity anomaly over Mount Melbourne may reflect either the presence of low density volcanic rocks or of a magma chamber under the volcano.

Composition

Trachyandesite and trachyte are the most common rocks on Mount Melbourne, with basalt being less common and mostly occurring around its base. The rocks define a mildly alkaline suite rich in potassium unlike the rocks elsewhere in the volcanic field. The rest of the volcanic field also features alkali basalts, basanite and mugearite. Phenocrysts include aegirine, amphibole, anorthoclase, augite, clinopyroxene, hedenbergite, ilmenite, magnetite, olivine, plagioclase and sanidine. Gneiss, granulite, harzburgite, lherzolite and tholeiite xenoliths are found in the volcanic field and form the core of many lava bombs. Inclusions in xenoliths indicate that the gaseous components of the Mount Melbourne volcanic field magmas consist mainly of carbon dioxide.

The trachytes and mugearites formed through magmatic differentiation in a crustal magma chamber from alkali basalts, defining an alkali basalt-trachyte differentiation series. Basalts were mainly erupted early in the history of the volcano. During the last 100,000 years, the magma chamber became established; this allowed both the differentiation of trachytes and the occurrence of large eruptions. A gap in the rock spectrum ("Daly gap") with a scarcity of benmoreite and mugearite has been noted at Mount Melbourne and other volcanoes in the region. There is no agreement on which processes contributed to petrogenesis in the Mount Melbourne volcanic field. The magmatic system that feeds Mount Melbourne appears to have a distinct composition from the one associated with the Mount Melbourne volcanic field.

Hydrothermal alteration has affected parts of the summit area, leaving yellow and white coloured deposits that contrast with the black volcanic rocks. Hydrothermal sinter deposits have formed in geothermal areas from past liquid water flow. Clay containing allophane, amorphous silica, allophane and feldspar are found in the summit area.

Climate

There are no detailed meteorological records of the summit region. Temperatures not exceeding −30 °C (−22 °F) or of −6 – −20 °C (21 – −4 °F) have been recorded in the summit region. Seasonal temperature variation is high and reaches 30 °C (54 °F). As part of climate change, temperatures on the Antarctic Peninsula have increased while the interior continent has cooled; at Mount Melbourne temperature declined between 1989 and 1998.

Winds blow mostly from the west and more rarely from the northwest. Catabatic winds blow from the Priestly and Reeves valleys. Precipitation is scarce. During winter, polar night lasts about three months.

During the Last Glacial Maximum (LGM), a marine ice sheet occupied Terra Nova Bay. The "Terra Nova Drift" was deposited between 25,000-7,000 years ago and is overlaid by later moraines from retreating ice during the post-LGM period. During the late Holocene after 5,000 years before present, glaciers advanced again as part of the Neoglacial. One minor advance occurred in the last c. 650 years.

Eruption history

Rocks at the summit have ages of between 260,000 and 10,000 years. Individual eruptions have been dated to 10,000±20,000, 80,000±15,000, 260,000±60,000 and 15,000±35,000 years ago. Highly inprecise ages of late Pleistocene to Holocene age have been obtained from the ejecta layer on the summit.

Mount Melbourne was active during the last 3-2.7 million years. Activity has been subdivided into an older Pliocene Cape Washington stage, an early Pleistocene Random Hills stage, the 400,000-100,000 years old Shield Nunatak stage and the recent Mount Melbourne stage. Volcanic activity migrated north from Cape Washington towards the Transantarctic Mountains and eventually became centralized at Mount Melbourne.

Ages obtained on its members include 2.96±0.2 million years, 740,000±100,000 years and 200,000±40,000 years for Baker Rocks, 2.7±0.2 million years and 450,000±50,000 years for Cape Washington, 74,000±110,000 years and 50,000±20,000 years for Edmonson Point, less than 400,000 years for Markham Island, 745,000±66,000 years for Harrows Peak, 1,368±0,09 million years for Pinkard Table, 1.55±0.05 million years, 431,000±82,000 and 110,000±70,000 years for Shield Nunatak, and 2.5±0.1 million years for Willows Nunatak.

Radiometric dating has shown that the appearance of a landform at Mount Melbourne is not indicative of its age; some well-preserved vents are older than heavily eroded ones. On the other hand, a lack of proper margin of errors and lack of details on which samples were dated has been problematic for radiometric dating efforts.

The Edmonson Point ignimbrite is a trachytic ignimbrite that crops out at Edmonson Point. It consists of three units of ash-supported, lapilli- and pumice-rich deposits with intercalated breccia lenses that reach a thickness of 30 metres (98 ft). They are two ignimbrite units separated by a base surge deposit. Faulting has offset the sequences, which are intruded by dikes. The Edmonson Point ignimbrite was produced by large Plinian eruptions and is about 120,000 years old. The eruption deposited tephra into the Ross Sea.

After this ignimbrite, a series of dikes gave rise to the probably subglacial Adelie Penguin Rookery lava field. This lava field is formed by numerous blocky lava flows with glassy margins, that reach a total thickness of 300 metres (980 ft) and are formed by hawaiite and benmoreite. They were fed through numerous dikes, which also gave rise to small scoria cones and spatter cones, and were emplaced non-contemporaneously. A tuff cone rises from the lava field and is formed by monogenetic volcano ejecta, including lava bombs encasing granite fragments and bombs large enough to leave craters in the ash they fell in. Ropy basalt lava flows with an uncertain source vent and a undissected scoria cone rise above the lava field and complete the Edmonson Point system. The Adelie Penguin Rookery lava field was erupted about 90,000 years ago.

A magma production rate of about 0.0015 cubic kilometres per year (0.00036 cu mi/a) has been inferred.

The northeastern parasitic cone formed after the bulk of the volcano and appears to be younger than the summit of Mount Melbourne.

Tephra found at the Allan Hills, in Dome C and Siple Dome ice cores may come from Mount Melbourne. Tephra layers in the latter indicate eruptions at Mount Melbourne 304 CE and less certainly 1810 AD, the former an eruption which deposited substantial amounts of sulfate on the ice sheet.

A tephra layer found in the Ross Sea has been interpreted as originating from an eruption of Mount Melbourne 9,700±5,300 years ago. A less than 30,000 years old tephra layer in a sediment core from the Ross Sea has a composition indicating that it was erupted at Mount Melbourne. Its deposition has been used to infer that that part of the western Ross Sea was ice-free at that time. Less than 500,000 years old tephra layers in the Frontier Mountain and Lichen Hills blue-ice areas have been attributed to volcanoes in the Mount Melbourne volcanic province.

The last eruption was a few centuries ago and tephrochronology has yielded an age of 1892±30 AD for it. This eruption deposited a major tephra layer around the volcano, which crops out mainly on its eastern side. At the end of the eruption, the three small craters on the rim of the Mount Melbourne summit crater formed.

No eruptions have been observed during historical time and the volcano is considered to be quiescent and a low hazard volcano. Ongoing deformation and seismic activity occurs at Mount Melbourne.

Future moderate explosive eruptions are possible. The prevailing winds would transport volcanic ash eastward across the Ross Sea. The hazards of Antarctic volcano eruptions are poorly known and while renewed eruptions of Mount Melbourne would likely not impact any human habitations, regional environmental or even global climate impacts are possible.

Italian scientists began to carry out a volcanology research program on Mount Melbourne in the late 1980 establishing a volcanological observatory in 1988. In 1990 they installed seismic stations around Mount Melbourne and between 1999 and 2001 a network of geodetic measurement stations around Terra Nova Bay, including several aimed at monitoring the Mount Melbourne volcano. Beginning in 2012, Korean scientists at the Jang Bogo Station added another seismic station network to monitor the volcano.

Geothermal activity

Geothermal activity occurs around the summit crater, on the upper parts of the volcano and on the northwestern slope, between 2,400–2,500 metres (7,900–8,200 ft) elevation. Another geothermal area exists close to Edmonson Point, including fumaroles and freshwater ponds with temperatures of 15–20 °C (59–68 °F) which is considerably higher than normal atmospheric temperatures in Antarctica.

Individual geothermally heated areas cover surfaces of a few hectares. Typically, the soil consists of a thin sand layer with organic matter covering scoria gravel. Mount Melbourne is one of several volcanoes in Antarctica that feature such geothermal soils.

Fumarole temperatures can reach 60 °C (140 °F), contrasting with the cold air; in some places, the ground is too hot to be touched.

The geothermal areas are visible in infrared light from aircraft. Satellite images have identified areas with temperatures of over 100–200 °C (212–392 °F).

Fumarolic landforms include ice towers, fumaroles, ice "roofs", caves in snow and firn, bare ground, ice hummocks surrounding fumarolic vents, puddles formed by condensed water vapour and steaming ground:

• Ice hummocks are hollow glacial structures that encase fumaroles. They reach heights of 4 metres (13 ft) and widths of 1–6 metres (3 ft 3 in – 19 ft 8 in). They mainly form over colder ground and widely spaced fumarolic vents.
• Ice towers are widespread around the caldera, especially in the north-northwestern and south-southeastern sectors, while warm ground is more restricted. In the northern sector of the volcano, ice towers and bare ground form a southeast-northwest trending lineament. Ice towers form when fumarolic gases freeze in the cold Antarctic air.
• Glacial caves form when geothermal heat melted ice, leaving cavities. Some of these caves are located in the summit caldera and reach lengths of several hundred metres, with ceilings reaching 3 metres (9.8 ft) height. Several caves have been accessed through ice towers or through gaps where the ice surrounding the cave rests on rock.

The caves and ice towers release water vapour rich, warm air. Hydrogen sulfide gas has been detected in fumaroles but is not common, facilitating the development of vegetation. Yellow deposits have been identified as sulfur.

The geothermal manifestations appear to be powered mainly by steam, as there is no evidence of geothermal landforms related to liquid water flow and heat conduction is not effective enough at most sites. It is possible that underground liquid water reservoirs form in some areas, however. The steam is produced by the melting and evaporation of snow and ice, and is then channelled through rocks to the vents. Atmospheric air likely circulates underground and is heated, eventually exiting in ice towers.

Geothermal activity has been steady between 1963 and 1983.

Life

Algae, lichens, liverworts and mosses grow on geothermally heated terrain on the upper parts of Mount Melbourne. Algae form crusts on the heated ground. Mosses form cushions and often occur around steam vents and under ice hummocks. The moss species Campylopus pyriformis does not grow leaves on Mount Melbourne. Pohlia nutans forms small shoots. The two moss species form separate stands that occur at different sites of the volcano and apart from Mount Erebus they constitute the highest mosses growing in Antarctica.

Vegetation is particularly common on a ridge within and south of the main crater. This ridge is known as "Cryptogam Ridge" and features a long snow-free area with a gravelly ground, small terraces and stone stripes. Soil temperatures recorded there reach 40–50 °C (104–122 °F). These are the only occurrences of Campylopus pyriformis on warm ground in Antarctica.

Vegetation on geothermally heated terrain exists elsewhere in Antarctica, such as on Bouvet, Deception Island, Mount Erebus and the South Sandwich Islands. Such systems are unusual for the continent. In South America, similar high-elevation geothermal environments to Mount Melbourne are found at Socompa.

Mount Melbourne along with Mount Erebus, Mount Rittmann and Deception Island is one of only four volcanoes in Antarctica known for having geothermal habitats, although other poorly studied volcanoes such as Mount Berlin, Mount Hampton and Mount Kauffman may also have them.

Small peat deposits have been found.

The geothermal area at the summit of Mount Melbourne makes up Antarctic Special Protected Area 118, which contains two specially restricted areas around Cryptogam Ridge and some markers used in studies of volcano deformation. Some algae from Mount Melbourne were accidentally transferred to Deception Island or Mount Erebus.

Edmonson Point and Cape Washington have Adelie penguin rookeries and south polar skuas and Weddel seals are also found. Over 24 lichen plus six moss species including Bryum argenteum moss has been found at Edmonson Point,. as well as microbial mats formed by cyanobacteria. Nematodes and collembola complete its biota.

Biology

The vegetation on Mount Melbourne grows mainly on terrain heated to temperatures of over 10–20 °C (50–68 °F), and there are gradations in vegetation type from colder to warmer temperatures.

These communities must have reached Mount Melbourne from far away. Transport was probably by wind as there is no flowing water in the region. Mount Melbourne was recently active, located south of the Antarctic Circle thus has a polar night lasting 13 weeks, the soils contain toxic elements such as mercury, the volcano is distant from ecosystems that could be the source of colonization events and away from the westerlies, which may explain why the vegetation is species-poor.

Condensing fumarole gases and meltwater from snow form the water supply of this vegetation. These are more available around fumarolic vents, thus mosses are concentrated there. In addition, the steam freezes in the cold air, forming the ice hummocks that act as a shelter and maintain stable humidity and temperature.

Some bacterial species are nitrogen fixing.

The geothermal heating and the availability of freshwater sets these volcanic biological communities apart from other Antarctic vegetation communities which are heated by the Sun.

There are differences between the vegetation and bacterial communities at Cryptogam Ridge and these on the northwest slope of Mount Melbourne, probably due to differences in soil components.

Genetic analysis has found that the mosses at Mount Melbourne might be evolving, yielding genetic variation.

Pohlia nutans may have arrived only recently on Mount Melbourne, or this volcano is not as favourable for its growth as Mount Rittmann where this moss is more common. Its colonies are less vigorous colonies on Mount Melbourne than Campylopus pyriformis.

Other species associated with the vegetation are the protozoan Corythion dubium, which is a testate amoeba common in Antarctica and the only invertebrate found in the geothermal habitats of Mount Melbourne, actinobacteria and various actinomycetes and fungal genera.

The hot, wet soils at Mount Melbourne host thermophilic organisms. That might make Mount Melbourne an island of thermophilic life on a ice-cold continent. Cold-tolerant microbes coexist with the thermophiles.

Several bacterial species were first described from Mount Melbourne's geothermal terrains:

• Alicyclobacillus pohliae from the northwest slope.
• Aneurinibacillus terranovensis from Cryptogam Ridge and also from Mount Rittmann volcano.
• Bacillus fumarioli from Cryptogam Ridge.
• Bacillus thermoantarcticus from Cryptogam Ridge, later renamed to Bacillus thermantarcticus.
• Brevibacillus levickii from the northwest slope.

See also

• List of volcanoes in Antarctica
• List of Ultras of Antarctica

References

Sources

• Adamson, R. G.; Cavaney, R. J. (May 1967). "Volcanic Debris-Layers near Mount Melbourne, Northern Victoria Land, Antarctica". New Zealand Journal of Geology and Geophysics. 10 (2): 418–421. doi:10.1080/00288306.1967.10426745.
• Allan, R. N.; Lebbe, L.; Heyrman, J.; De Vos, P.; Buchanan, C. J.; Logan, N. A. (2005). "Brevibacillus levickii sp. nov. and Aneurinibacillus terranovensis sp. nov., two novel thermoacidophiles isolated from geothermal soils of northern Victoria Land, Antarctica". International Journal of Systematic and Evolutionary Microbiology,. 55 (3): 1039–1050. doi:10.1099/ijs.0.63397-0. ISSN 1466-5026.{{cite journal}}: CS1 maint: extra punctuation (link)
• BADINO, Giovanni; MENEGHEL, Mirco (2001). Caves in the Glaciers of Terra Nova Bay (Victoria Land, Antarctica). Speleo Brasil 2001. Brasília – via ResearchGate.
• Bargagli, R.; Skotnicki, M. L.; Marri, L.; Pepi, M.; Mackenzie, A.; Agnorelli, C. (1 June 2004). "New record of moss and thermophilic bacteria species and physico-chemical properties of geothermal soils on the northwest slope of Mt. Melbourne (Antarctica)". Polar Biology. 27 (7): 423–431. doi:10.1007/s00300-004-0612-6. ISSN 1432-2056.
• Baroni, Carlo; et al. (2005). Mount Melbourne Quadrangle, Victoria Land, Antarctica (Map). 1:250,000. Antarctic Geomorphological and Glaciological Map Series. pp. 38–40 – via ResearchGate.
• Baroni, Carlo; Orombelli, Giuseppe (1994). "Holocene glacier variations in the Terra Nova Bay area (Victoria Land, Antarctica)". Antarctic Science. 6 (4): 497–505. doi:10.1017/S0954102094000751. ISSN 1365-2079.
• Berkeley, Roger; Heyndrickx, Marc; Logan, Niall; De Vos, Paul, eds. (2002-08-09). Applications and Systematics of Bacillus and Relatives (1 ed.). Wiley. doi:10.1002/9780470696743. ISBN 978-0-632-05758-0.
• Broady, Paul; Given, David; Greenfield, Laurence; Thompson, Keith (1 March 1987). "The biota and environment of fumaroles on Mt Melbourne, northern Victoria Land". Polar Biology. 7 (2): 97–113. doi:10.1007/BF00570447. ISSN 1432-2056.
• Burge, W.; Parker, D.C. (1968). "Infrared survey in Antarctica". Antarctic Journal of the United States.
• Capra, A.; Bitelli, G.; Gandolfi, S.; Mancini, F.; Sarti, P.; Vittuari, L. (2002). "Geodetic Network For Crustal Deformation Control of Northern Victoria Land (antarctica)". 27: 3191. {{cite journal}}: Cite journal requires |journal= (help)
• Convey, P.; Smith, R. I. Lewis; Hodgson, D. A.; Peat, H. J. (2000). "The flora of the South Sandwich Islands, with particular reference to the influence of geothermal heating". Journal of Biogeography. 27 (6): 1279–1295. doi:10.1046/j.1365-2699.2000.00512.x. ISSN 1365-2699.
• Cowan, Don A., ed. (2014). Antarctic Terrestrial Microbiology. Berlin, Heidelberg: Springer Berlin Heidelberg. doi:10.1007/978-3-642-45213-0. ISBN 978-3-642-45212-3.
• Del Carlo, P.; Di Roberto, A.; Di Vincenzo, G.; Bertagnini, A.; Landi, P.; Pompilio, M.; Colizza, E.; Giordano, G. (14 April 2015). "Late Pleistocene-Holocene volcanic activity in northern Victoria Land recorded in Ross Sea (Antarctica) marine sediments". Bulletin of Volcanology. 77 (5): 36. doi:10.1007/s00445-015-0924-0. ISSN 1432-0819.
• Dunbar, Nelia W.; Zielinski, Gregory A.; Voisins, Daniel T. (2003). "Tephra layers in the Siple Dome and Taylor Dome ice cores, Antarctica: Sources and correlations". Journal of Geophysical Research: Solid Earth. 108 (B8). doi:10.1029/2002JB002056. ISSN 2156-2202.
• Faure, Gunter; Mensing, Teresa M. (2011). The Transantarctic Mountains. Dordrecht: Springer Netherlands. doi:10.1007/978-90-481-9390-5. ISBN 978-1-4020-8406-5.
• Ferraccioli, F; Armadillo, E; Bozzo, E; Privitera, E (1 January 2000). "Magnetics and gravity image tectonic framework of the Mount Melbourne volcano area (Antarctica)". Physics and Chemistry of the Earth, Part A: Solid Earth and Geodesy. 25 (4): 387–393. doi:10.1016/S1464-1895(00)00061-2. ISSN 1464-1895.
• Gambino, Salvatore; Privitera, Eugenio (1 March 1996). "Mt. Melbourne volcano, antarctica: Evidence of seismicity related to volcanic activity". pure and applied geophysics. 146 (2): 305–318. doi:10.1007/BF00876495. ISSN 1420-9136.
• Gambino, Salvatore (2005). "Air and permafrost temperatures at Mount Melbourne (1989–98)". Antarctic Science. 17 (1): 151–152. doi:10.1017/S095410200500249X. ISSN 1365-2079.
• Giordano, Guido; Lucci, Federico; Phillips, David; Cozzupoli, Domenico; Runci, Valentina (1 November 2012). "Stratigraphy, geochronology and evolution of the Mt. Melbourne volcanic field (North Victoria Land, Antarctica)". Bulletin of Volcanology. 74 (9): 1985–2005. doi:10.1007/s00445-012-0643-8. ISSN 1432-0819.
• "Melbourne". Global Volcanism Program. Smithsonian Institution.
• Hall, Brenda L. (1 October 2009). "Holocene glacial history of Antarctica and the sub-Antarctic islands". Quaternary Science Reviews. 28 (21): 2213–2230. doi:10.1016/j.quascirev.2009.06.011. ISSN 0277-3791.
• Halloy, S. (1991). "Islands of Life at 6000 m Altitude: The Environment of the Highest Autotrophic Communities on Earth (Socompa Volcano, Andes)". Arctic and Alpine Research. 23 (3): 247–262. doi:10.2307/1551602. JSTOR 1551602.
• Hughes, P.; Krissek, L.A. "Modern sediments of the Terra Nova Bay polynya, Ross Sea, Antarctica". Antarctic Journal of the United States. 20 (5): 107–108.
• Hughes, Kevin A.; Convey, Pete (1 February 2010). "The protection of Antarctic terrestrial ecosystems from inter- and intra-continental transfer of non-indigenous species by human activities: A review of current systems and practices". Global Environmental Change. 20 (1): 96–112. doi:10.1016/j.gloenvcha.2009.09.005. ISSN 0959-3780.
• Imperio, T.; Viti, C.; Marri, L. (1 January 2008). "Alicyclobacillus pohliae sp. nov., a thermophilic, endospore-forming bacterium isolated from geothermal soil of the north-west slope of Mount Melbourne (Antarctica)". INTERNATIONAL JOURNAL OF SYSTEMATIC AND EVOLUTIONARY MICROBIOLOGY. 58 (1): 221–225. doi:10.1099/ijs.0.65092-0. ISSN 1466-5026.
• Kaminuma, Katsutada (2000). "A revaluation of the seismicity in the Antarctic": 145–157. {{cite journal}}: Cite journal requires |journal= (help)
• Keys, J. R.; McIntosh, W. C.; Kyle, P. R. (1983). "Volcanic activity of Mount Melbourne, northern Victoria Land". Antarctic journal of the United States. 18 (5): 10–11.
• Kurbatov, A. V.; Zielinski, G. A.; Dunbar, N. W.; Mayewski, P. A.; Meyerson, E. A.; Sneed, S. B.; Taylor, K. C. (2006). "A 12,000 year record of explosive volcanism in the Siple Dome Ice Core, West Antarctica". Journal of Geophysical Research. 111 (D12): D12307. doi:10.1029/2005JD006072.
• LeMasurier, W.E.; Thomson, J.W.; Baker, P.E.; Kyle, P.R.; Rowley, P.D.; Smellie, J.L.; Verwoerd, W.J., eds. (1990). "Volcanoes of the Antarctic Plate and Southern Oceans". Antarctic Research Series. doi:10.1029/ar048. ISSN 0066-4634.
• Licht, K. J.; Dunbar, N. W.; Andrews, J. T.; Jennings, A. E. (1 January 1999). "Distinguishing subglacial till and glacial marine diamictons in the western Ross Sea, Antarctica: Implications for a last glacial maximum grounding line". GSA Bulletin. 111 (1): 91–103. doi:10.1130/0016-7606(1999)1112.3.CO;2. ISSN 0016-7606.
• Linskens, H. F.; Bargagli, R.; Cresti, M.; Focardi, S. (1 March 1993). "Entrapment of long-distance transported pollen grains by various moss species in coastal Victoria Land, Antarctica". Polar Biology. 13 (2): 81–87. doi:10.1007/BF00238539. ISSN 1432-2056.
• Luporini, P.; Morbidoni, M., eds. (2004). Polarnet Technical Report. Proceedings of the Fifth PNRA Meeting on Antarctic Biology. SCIENTIFIC AND TECHNICAL REPORT SERIES. Messina: POLARNET COORDINATING UNIT. ISSN 1592-5064.
• Lyon, Graeme L. (January 1986). "Stable isotope stratigraphy of ice cores and the age of the last eruption at Mount Melbourne, Antarctica". New Zealand Journal of Geology and Geophysics. 29 (1): 135–138. doi:10.1080/00288306.1986.10427528.
• Lyon, G. L.; Giggenbach, W. F. (1 July 1974). "Geothermal activity in Victoria Land, Antarctica". New Zealand Journal of Geology and Geophysics. 17 (3): 511–521. doi:10.1080/00288306.1973.10421578.
• Marti, Joan; Ernst, Gerald G. J., eds. (2005). Volcanoes and the Environment. Cambridge: Cambridge University Press. ISBN 978-0-521-59725-8.
• Morin, Roger H.; Williams, Trevor; Henrys, Stuart A.; Magens, Diana; Niessen, Frank; Hansaraj, Dhiresh (1 August 2010). "Heat Flow and Hydrologic Characteristics at the AND-1B borehole, ANDRILL McMurdo Ice Shelf Project, Antarctica". Geosphere. 6 (4): 370–378. doi:10.1130/GES00512.1.
• Nathan, Simon; Schulte, F. J. (May 1967). "Recent Thermal and Volcanic activity on Mount Melbourne, Northern Victoria Land, Antarctica". New Zealand Journal of Geology and Geophysics. 10 (2): 422–430. doi:10.1080/00288306.1967.10426746.
• Nathan, Simon; Schulte, F. J. (1 November 1968). "Geology and petrology of the Campbell—Aviator Divide, Northern Victoria Land, Antarctica". New Zealand Journal of Geology and Geophysics. 11 (4): 940–975. doi:10.1080/00288306.1968.10420762. ISSN 0028-8306.
• Newsham, K. K. (2010). "The biology and ecology of the liverwort Cephaloziella varians in Antarctica". Antarctic Science. 22 (2): 131–143. doi:10.1017/S0954102009990630. ISSN 1365-2079.
• Nicolaus, B.; Marsiglia, F.; Esposito, E.; Trincone, A.; Lama, L.; Sharp, R.; di Prisco, G.; Gambacorta, A. (1 December 1991). "Isolation of five strains of thermophilic eubacteria in Antarctica". Polar Biology. 11 (7): 425–429. doi:10.1007/BF00233077. ISSN 1432-2056.
• Nicolaus, B.; Lama, L.; Esposito, E.; Manca, M. C.; Gambacorta, A.; Prisco, G. di. (1 February 1996). ""Bacillus thermoantarcticus" sp. nov., from Mount Melbourne, Antarctica: a novel thermophilic species". Polar Biology. 16 (2): 101–104. doi:10.1007/BF02390430. ISSN 1432-2056.
• Park, Y.; Lee, W. S.; Lee, C. K.; Kim, J. S. (2019-12-01). "P-wave tomograpy in the Northern Victoria Land, Antarctica: focus on the Terra Nova Bay". AGU Fall Meeting Abstracts. 21.
• Perchiazzi, Natale; Folco, Luigi; Mellini, Marcello (1999). "Volcanic ash bands in the Frontier Mountain and Lichen Hills blue-ice fields, northern Victoria Land". Antarctic Science. 11 (3): 353–361. doi:10.1017/S0954102099000449. ISSN 1365-2079.
• "Recommendations from the 14th Antarctic Treaty Consultative Meeting, Rio De Janeiro 5–6 October 1987". Polar Record. 24 (149): 173–191. 2009. doi:10.1017/S0032247400009116. ISSN 1475-3057.
• Ross, James Clark (2011) [1847]. A Voyage of Discovery and Research in the Southern and Antarctic Regions, During the Years 1839-43. Vol. 1. Cambridge University Press. p. 205. ISBN 9781108030854 – via Google Books.
• Salvini, Francesco; Storti, Fabrizio (1 December 1999). "Cenozoic tectonic lineaments of the Terra Nova Bay region, Ross Embayment, Antarctica". Global and Planetary Change. 23 (1): 129–144. doi:10.1016/S0921-8181(99)00054-5. ISSN 0921-8181.
• Schneider, David P.; Ammann, Caspar M.; Otto-Bliesner, Bette L.; Kaufman, Darrell S. (1 August 2009). "Climate response to large, high-latitude and low-latitude volcanic eruptions in the Community Climate System Model". Journal of Geophysical Research. 114 (D15): D15101. doi:10.1029/2008JD011222.
• Skotnicki, M.; Bargagli, R.; Ninham, J. (1 October 2002). "Genetic diversity in the moss Pohlia nutans on geothermal ground of Mount Rittmann, Victoria Land, Antarctica". Polar Biology. 25 (10): 771–777. doi:10.1007/s00300-002-0418-3. ISSN 1432-2056.
• Skotnicki, M. L.; Selkirk, P. M.; Broady, P.; Adam, K. D.; Ninham, J. A. (2004). "Dispersal of the moss Campylopus pyriformis on geothermal ground near the summits of Mount Erebus and Mount Melbourne, Victoria Land, Antarctica". Antarctic Science. 13 (3): 280–285. doi:10.1017/S0954102001000396. ISSN 1365-2079.
• Stenni, B.; Proposito, M.; Gragnani, R.; Flora, O.; Jouzel, J.; Falourd, S.; Frezzotti, M. (16 May 2002). "Eight centuries of volcanic signal and climate change at Talos Dome (East Antarctica): VOLCANIC SIGNAL AND CLIMATIC CHANGE AT TALOS DOME". Journal of Geophysical Research: Atmospheres. 107 (D9): ACL 3–1–ACL 3-13. doi:10.1029/2000JD000317.
• Tosi, Solveig; Casado, Begoña; Gerdol, Renato; Caretta, Giuseppe (1 April 2002). "Fungi isolated from Antarctic mosses". Polar Biology. 25 (4): 262–268. doi:10.1007/s00300-001-0337-8. ISSN 1432-2056.
• Wörner, G.; Viereck, L. (1987). "Subglacial to Emergent Volcanism at Shield Nunatak, Mt. Melbourne Volcanic Field, Antarctica". Polarforschung. 57 (1, 2): 27–41.
• Wörner, Gerhard; Orsi, Giovanni (1990). "Volcanic Geology of Edmonson Point, Mt.Melbourne Volcanic Field, North Victoria Land, Antarctica". Polarforschung. 60 (2): 84–86.
• Woerner, Gerhard; Fricke, Angelika; Burke, Ernst A. J. (1 August 1993). "Fluid-inclusion studies on lower crustal gabbroic xenoliths from the Mt. Melbourne volcanic field (Antarctica); evidence for the post-crystallization uplift history during Cenozoic Ross Sea rifting". European Journal of Mineralogy. 5 (4): 775–785. ISSN 0935-1221.
• Zibordi, Giuseppe; Frezzotti, Massimo (1996). "Orographic clouds in north Victoria Land from AVHRR images". Polar Record. 32 (183): 317–324. doi:10.1017/S003224740006753X. ISSN 1475-3057.
• Zucconi, L.; Pagano, S.; Fenice, M.; Selbmann, L.; Tosi, S.; Onofri, S. (1 January 1996). "Growth temperature preferences of fungal strains from Victoria Land, Antarctica". Polar Biology. 16 (1): 53–61. doi:10.1007/BF01876829. ISSN 1432-2056.

Bibliography

• LeMasurier, W. E. (1990). Thomson, J. W. (ed.). Volcanoes of the Antarctic Plate and Southern Oceans. American Geophysical Union. p. 512. ISBN 0-87590-172-7.
• "Skiing the Pacific Ring of Fire and Beyond". Amar Andalkar's Ski Mountaineering and Climbing Site. 2007 [1997]. Retrieved 14 January 2005.

External links

• "Mount Melbourne, Antarctica" on Peakbagger