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Journal articles on the topic 'Antarctic plate'

Author: Grafiati

Published: 4 June 2021

Last updated: 2 February 2022

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1

Uchida, Mayuka, Ippei Suzuki, Keizo Ito, Mayumi Ishizuka, Yoshinori Ikenaka, Shouta M. M. Nakayama, Tsutomu Tamura, Kenji Konishi, Takeharu Bando, and Yoko Mitani. "Estimation of the feeding record of pregnant Antarctic minke whales (Balaenoptera bonaerensis) using carbon and nitrogen stable isotope analysis of baleen plates." Polar Biology 44, no. 3 (February 22, 2021): 621–29. http://dx.doi.org/10.1007/s00300-021-02816-5.

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AbstractAntarctic minke whales (Balaenoptera bonaerensis) are migratory capital breeders that experience intensive summer feeding on Antarctic krill (Euphausia superba) in the Southern Ocean and winter breeding at lower latitudes, but their prey outside of the Antarctic is unknown. Stable isotope analyses were conducted on δ13C and δ15N from the baleen plates of ten pregnant Antarctic minke whales to understand the growth rate of the baleen plate and their diet in lower latitudes. Two to three oscillations along the length of the edge of the baleen plate were observed in δ15N, and the annual growth rate was estimated to be 75.2 ± 20.4 mm, with a small amplitude (0.97 ± 0.21 ‰). Bayesian stable isotope mixing models were used to understand the dominant prey that contributed to the isotopic component of the baleen plate using Antarctic krill from the stomach contents and reported values of Antarctic coastal krill (Euphausia crystallorophias), Antarctic silver fish (Pleuragramma antarcticum), Australian krill spp., and Australian pelagic fish spp.. The models showed that the diet composition of the most recent three records from the base of the baleen plates (model 1) and the highest δ15N values in each baleen plate (model 2) were predominantly Antarctic krill, with a contribution rate of approximately 80%. The rates were approximately 10% for Antarctic coastal krill and less than 2.0% for the two Australian prey groups in both models. These results suggest that pregnant Antarctic minke whales did not feed on enough prey outside of the Antarctic to change the stable isotope values in their baleen plates.

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2

Storey, Bryan C., and Roi Granot. "Chapter 1.1 Tectonic history of Antarctica over the past 200 million years." Geological Society, London, Memoirs 55, no. 1 (2021): 9–17. http://dx.doi.org/10.1144/m55-2018-38.

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AbstractThe tectonic evolution of Antarctica in the Mesozoic and Cenozoic eras was marked by igneous activity that formed as a result of simultaneous continental rifting and subduction processes acting during the final stages of the southward drift of Gondwana towards the South Pole. For the most part, continental rifting resulted in the progressive disintegration of the Gondwana supercontinent from Middle Jurassic times to the final isolation of Antarctica at the South Pole following the Cenozoic opening of the surrounding ocean basins, and the separation of Antarctica from South America and Australia. The initial rifting into East and West Gondwana was proceeded by emplacement of large igneous provinces preserved in present-day South America, Africa and Antarctica. Continued rifting within Antarctica did not lead to continental separation but to the development of the West Antarctic Rift System, dividing the continent into the East and West Antarctic plates, and uplift of the Transantarctic Mountains. Motion between East and West Antarctica has been accommodated by a series of discrete rifting pulses with a westward shift and concentration of the motion throughout the Cenozoic leading to crustal thinning, subsidence, elevated heat flow conditions and rift-related magmatic activity. Contemporaneous with the disintegration of Gondwana and the isolation of Antarctica, subduction processes were active along the palaeo-Pacific margin of Antarctica recorded by magmatic arcs, accretionary complexes, and forearc and back-arc basin sequences. A low in magmatic activity between 156 and 142 Ma suggests that subduction may have ceased during this time. Today, following the gradual cessation of the Antarctic rifting and surrounding subduction, the Antarctic continent is situated close to the centre of a large Antarctic Plate which, with the exception of an active margin on the northern tip of the Antarctic Peninsula, is surrounded by active spreading ridges.

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3

DeMets, C., S. Merkouriev, and D. Sauter. "High resolution reconstructions of the Southwest Indian Ridge, 52 Ma to present: implications for the breakup and absolute motion of the Africa plate." Geophysical Journal International 226, no. 3 (March 17, 2021): 1461–97. http://dx.doi.org/10.1093/gji/ggab107.

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SUMMARY We reconstruct the post-52 Ma seafloor spreading history of the Southwest Indian Ridge at 44 distinct times from inversions of ≈20 000 magnetic reversal, fracture zone and transform fault crossings, spanning major regional tectonic events such as the Arabia–Eurasia continental collision, the Arabia Peninsula’s detachment from Africa, the arrival of the Afar mantle plume below eastern Africa and the initiation of rifting in eastern Africa. Best-fitting and noise-reduced rotation sequences for the Nubia–Antarctic, Lwandle–Antarctic and Somalia–Antarctic Plate pairs indicate that spreading rates everywhere along the ridge declined gradually by ≈50 per cent from ≈31 to 19–18 Ma. A concurrent similar-magnitude slowdown in the component of the Africa Plate’s absolute motion parallel to Southwest Indian Ridge spreading suggests that both were caused by a 31–18 Ma change in the forces that drove and resisted Africa’s absolute motion. Possible causes for this change include the effects of the Afar mantle plume on eastern Africa or the Arabia Peninsula’s detachment from the Somalia Plate, which culminated at 20–18 Ma with the onset of seafloor spreading in the Gulf of Aden. At earlier times, an apparently robust but previously unknown ≈6-Myr-long period of rapid kinematic change occurred from 43 to 37 Ma, consisting of a ≈50 per cent spreading rate slowdown from 43 to 40 Ma followed by a full spreading rate recovery and 30–40° clockwise rotation of the plate slip direction from 40 to 37 Ma. Although these kinematic changes coincided with a reconfiguration of the palaeoridge geometry, their underlying cause is unknown. Southwest Indian Ridge abyssal hill azimuths are consistent with the slip directions estimated with our newly derived Somalia–Antarctic and Lwandle–Antarctic angular velocities, adding confidence in their reliability. Lwandle–Antarctica Plate motion has closely tracked Somalia–Antarctic Plate motion since 50 Ma, consistent with slow-to-no motion between the Lwandle and Somalia plates for much of that time. In contrast, Nubia–Somalia rotations estimated from our new Southwest Indian Ridge rotations indicate that 189 ± 34 km of WNW–ESE divergence between Nubia and Somalia has occurred in northern Africa since 40 Ma, including 70–80 km of WNW–ESE divergence since 17–16 Ma, slow to no motion from 26 to 17 Ma, and 109 ± 38 km of WNW–ESE divergence from 40 to ≈26 Ma absent any deformation within eastern Antarctica before 26 Ma.

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4

Panter, Kurt Samuel. "Chapter 1.3 Antarctic volcanism: petrology and tectonomagmatic overview." Geological Society, London, Memoirs 55, no. 1 (2021): 43–53. http://dx.doi.org/10.1144/m55-2020-10.

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AbstractPetrological investigations over the past 30 years have significantly advanced our knowledge of the origin and evolution of magmas emplaced within and erupted on top of the Antarctic Plate. Over the last 200 myr Antarctica has experienced: (1) several episodes of rifting, leading to the fragmentation of Gondwana and the formation byc.83 Ma of the current Antarctica Plate; (2) long-lived subduction that shut down progressively eastwards along the Gondwana margin in the Late Cretaceous and is still active at the northernmost tip of the Antarctic Peninsula; and (3) broad extension across West Antarctica that produced one of the Earth's major continental rift systems. The dynamic tectonic history of Antarctica since the Triassic has led to a diversity of volcano types and igneous rock compositions with correspondingly diverse origins. Many intriguing questions remain about the petrology of mantle sources and the mechanisms for melting during each tectonomagmatic phase. For intraplate magmatism, the upwelling of deep mantle plumes is often evoked. Alternatively, subduction-related metasomatized mantle sources and melting by more passive means (e.g. edge-driven flow, translithospheric faulting, slab windows) are proposed. A brief review of these often competing models is provided in this chapter along with recommendations for ongoing petrological research in Antarctica.

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5

Guo, J., K. Wang, Z. Zeng, L. Li, J. Liu, X. Tang, X. Cui, Y. Wang, B. Sun, and J. Zhang. "PRELIMINARY LONG-PERIOD MAGNETOTELLURIC INVESTIGATION AT THE EDGE OF ICE SHEET IN EAST ANTARCTICA." ISPRS - International Archives of the Photogrammetry, Remote Sensing and Spatial Information Sciences XLIII-B3-2020 (August 21, 2020): 875–80. http://dx.doi.org/10.5194/isprs-archives-xliii-b3-2020-875-2020.

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Abstract. The lithospheric mantle structure of the Antarctic continent is of great significance of studying the polymerization and fragmentation mechanism of Gondwana and the plate movement law. Long-period magnetotelluric (LMT) is an important method to study the electrical structure of earth crust and mantle. However, been limited by the bad natural environment and logistics supply difficulties, there is no LMT record of Antarctica before. In 2018, China's 34th Antarctic scientific expedition carried out the LMT survey at the eastern edge of the Antarctic continent with a frequency range of 0.00015 Hz to 0.1 Hz. After the processing and analysis, we get three points as fellow: (1) The lithospheric mantle of Antarctica has a three-dimensional resistivity structure; (2) There are low resistivity regions in the Antarctic mantle, which may be related to thermal activity. (3) It is possible to carry out LMT measurements in eastern Antarctic and more can be done in the future.

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6

Farrar, Edward, and John M. Dixon. "Ridge subduction: kinematics and implications for the nature of mantle upwelling." Canadian Journal of Earth Sciences 30, no. 5 (May 1, 1993): 893–907. http://dx.doi.org/10.1139/e93-074.

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Ridge subduction follows the approach of an oceanic spreading centre towards a trench and subduction of the leading oceanic plate beneath the overriding plate. There are four possible kinematic scenarios: (1) welding of the trailing and overriding plates (e.g., Aluk–Antarctic Ridge beneath Antarctica); (2) slower subduction of the trailing plate (e.g., Nazca–Antarctic Ridge beneath Chile and Pacific–Izanagi Ridge beneath Japan); (3) transform motion between the trailing and overriding plates (e.g., San Andreas Transform); or (4) divergence between the overriding and trailing plates (e.g., Pacific – North America). In case 4, the divergence may be accommodated in two ways: the overriding plate may be stretched (e.g., Basin and Range Province extension, which has brought the continental margin into collinearity (and, therefore, transform motion) with the Pacific – North America relative motion); or divergence may occur at the continental margin and be manifest as a change in rate and direction of sea-floor spreading because the pair of spreading plates changes (e.g., from Pacific–Farallon to Pacific – North America), spawning a secondary spreading centre (i.e., Gorda – Juan de Fuca – Explorer ridge system) that migrates away from the overriding plate.Mantle upwelling associated with sea-floor spreading ridges is widely regarded as a passive consequence, rather than an active cause, of plate divergence. Geological and geophysical phenomena attendant to ridge–trench interaction suggest that regardless of the kinematic relations among the three plates, a thermal anomaly formerly associated with the ridge migrates beneath the overriding plate. The persistence of this thermal anomaly demonstrates that active mantle upwelling may continue for tens of millions of years after ridge subduction. Thus, regardless of whether the mantle upwelling was active or passive at its origin, it becomes active if the spreading continues for sufficient time and, thus, must contribute to the driving mechanism of plate tectonics.

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7

Thomson, M. R. A., and Alan P. M. Vaughan. "The role of Antarctica in the development of plate tectonic theories: from Scott to the present." Archives of Natural History 32, no. 2 (October 2005): 362–93. http://dx.doi.org/10.3366/anh.2005.32.2.362.

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One hundred years of geological research in and around Antarctica since Scott's Discovery expedition of 1901–1904 have seen the continent move from a great unknown at the margins of human knowledge to centre stage in the development of plate tectonics, continental break-up and global climate evolution. Research in Antarctica has helped make the Gondwana supercontinent a scientific fact. Discoveries offshore have provided some of the key evidence for plate tectonics and extended the evidence of global glaciation back over 30 million years. Studies of Antarctica's tectonic evolution have helped elucidate the details of continental break-up, and the continent continues to provide the best testing ground for competing scientific models. Antarctica's deep past has provided support for the “Snowball Earth” hypothesis, and for the pre-Gondwana, Rodinia supercontinent. Current research is focusing on Antarctica's subglacial lakes and basins, the possible causes of Antarctic glaciation, the evolution of its surrounding oceanic and mantle gateways, and its sub-ice geological composition and structure. None of this would have been possible without maps, and these have provided the foundation stone for Antarctic research. New mapping and scientific techniques, and new research platforms hold great promise for further major contributions from Antarctica to Earth system science in the twenty-first century.

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8

Nettles, Meredith, Terry C. Wallace, and Susan L. Beck. "The March 25, 1998 Antarctic Plate Earthquake." Geophysical Research Letters 26, no. 14 (July 15, 1999): 2097–100. http://dx.doi.org/10.1029/1999gl900387.

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9

Anderson-Fontana, Sandra, Joseph F. Engeln, Paul Lundgren, Roger L. Larson, and Seth Stein. "Tectonics of the Nazca-Antarctic plate boundary." Earth and Planetary Science Letters 86, no. 1 (November 1987): 46–56. http://dx.doi.org/10.1016/0012-821x(87)90187-7.

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10

Grad, M., A. Guterch, and T. Janik. "Seismic structure of the lithosphere across the zone of subducted Drake plate under the Antarctic plate, West Antarctica." Geophysical Journal International 115, no. 2 (November 1993): 586–600. http://dx.doi.org/10.1111/j.1365-246x.1993.tb01209.x.

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11

ELLIOT, D. H., D. LARSEN, C. M. FANNING, T. H. FLEMING, and J. D. VERVOORT. "The Lower Jurassic Hanson Formation of the Transantarctic Mountains: implications for the Antarctic sector of the Gondwana plate margin." Geological Magazine 154, no. 4 (July 27, 2016): 777–803. http://dx.doi.org/10.1017/s0016756816000388.

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AbstractThe Hanson Formation, Antarctica, consists of interbedded sandstones and tuffaceous rocks of Early Jurassic age. The sandstones, pebbly to medium-grained, range between quartzo-feldspathic and volcaniclastic, with some of the former being coarse-grained arkoses that imply proximal sources. Geochronology of detrital zircons provides evidence for source rock ages, whereas sandstone petrology demonstrates a mixed provenance. Tuffaceous strata are reworked fine to very fine-grained tuffs resulting from distal Plinian eruptions. Dated tuffs provide time constraints on the duration of volcanism. The sandstones and tuffs accumulated in a rift environment. Geochemically the tuffs are rhyolitic in composition, and the Sr and Nd isotope data together with the patterns on multi-element diagrams suggest they were derived from a volcanic arc, which is interpreted to have been located along the West Antarctic Gondwana margin. The silicic volcanism extends the distribution and timing of magmatism in the Early Jurassic along that margin. The Early Jurassic extensional regime was delimited by the plate margin region and the East Antarctic craton. The rift valley system along the East Antarctic craton margin, in which the Hanson strata accumulated, was the focus for subsequent emplacement of the intrusive and extrusive rocks of the Lower Jurassic Ferrar Large Igneous Province. The Early Jurassic extensional rifts may have been reactivated during Cretaceous–Cenozoic development of the West Antarctic Rift System.

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12

Anonymous. "Volcanoes of the Antarctic Plate and Southern Oceans, Antarctic Research Series, Volume 48." Eos, Transactions American Geophysical Union 71, no. 28 (1990): 799. http://dx.doi.org/10.1029/90eo00230.

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13

Klepeis, Keith A., and Lawrence A. Lawver. "Tectonics of the Antarctic-Scotia plate boundary near Elephant and Clarence Islands, West Antarctica." Journal of Geophysical Research: Solid Earth 101, B9 (September 10, 1996): 20211–31. http://dx.doi.org/10.1029/96jb01510.

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14

Weaver, S. D. "Volcanoes of the Antarctic Plate and Southern Oceans." Journal of Volcanology and Geothermal Research 47, no. 3-4 (September 1991): 368–69. http://dx.doi.org/10.1016/0377-0273(91)90013-p.

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15

Long, Douglas J. "An Eocene wrasse (Perciformes; Labridae) from Seymour Island." Antarctic Science 4, no. 2 (June 1992): 235–37. http://dx.doi.org/10.1017/s095410209200035x.

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A nearly complete lower pharyngeal tooth-plate from a large (over 60 cm long) fossil wrasse (Perciformes: Labridae) was recently recovered from the middle to late Eocene La Meseta Formation on Seymour Island, Antarctic Peninsula. This find increases the number of teleosts from the Eocene of Antarctica to five taxa, and further illustrates the diversity of the ichthyofauna in the Eocene Weddellian Sea prior to wide-scale climatic change in the Southern Ocean. The fossil wrasse represents the first occurrence of this family in Antarctica, and is one of the oldest fossils of this family from the Southern Hemisphere. Wrasses are not found in Antarctic waters today, and probably became extinct during the Oligocene due to a combination of climatic change, loss of shallow-water habitat, and changes in the trophic structure of the Wedell Sea.

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16

Conder, James A., and Donald W. Forsyth. "Do the 1998 Antarctic Plate earthquake and its aftershocks delineate a plate boundary?" Geophysical Research Letters 27, no. 15 (August 1, 2000): 2309–12. http://dx.doi.org/10.1029/1999gl011126.

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17

Schmeltz, Marjorie, Eric Rignot, and Douglas MacAyeal. "Tidal flexure along ice-sheet margins: comparison of InSAR with an elastic-plate model." Annals of Glaciology 34 (2002): 202–8. http://dx.doi.org/10.3189/172756402781818049.

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AbstractWe compare interferometric synthetic aperture radar (InSAR) observations of tidal flexure on Antarctic and Greenland glaciers with a finite-element model simulation of tidal flexure on an elastic plate of ice. The results show that the elastic-plate model is able to reproduce with good fidelity the pattern of tidal flexure observed with InSAR. In the case of David Glacier, Antarctica, the model provides independent confirmation of its grounding-line position and unusual pattern of tidal flexure. A detailed analysis of temporal changes in tidal flexing on Petermann Gletscher, Greenland, and Pine Island Glacier, West Antarctica, however, reveals that Young’s elastic modulus of ice, E, employed in the simulations to match observations, needs to vary between 0.8 and 3.5 GPa. This time dependence of E is attributed to visco-plastic effects, not to a migration of the grounding line with tide, or measurement errors.

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18

Antolik, Michael, Asya Kaverina, and Douglas S. Dreger. "Compound rupture of the great 1998 Antarctic plate earthquake." Journal of Geophysical Research: Solid Earth 105, B10 (October 10, 2000): 23825–38. http://dx.doi.org/10.1029/2000jb900246.

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19

JIANG, Wei-Ping, Dong-Chen E, Bi-Wei ZHAN, and You-Wen LIU. "New Model of Antarctic Plate Motion and Its Analysis." Chinese Journal of Geophysics 52, no. 1 (January 2009): 23–32. http://dx.doi.org/10.1002/cjg2.1323.

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20

SAN VICENTE, CARLOS. "New Mysida (Crustacea) in the genus Pseudomma from the Bellingshausen Sea (Southern Ocean)." Zootaxa 2833, no. 1 (April 27, 2011): 15. http://dx.doi.org/10.11646/zootaxa.2833.1.2.

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Two new Erythropinae mysids, Pseudomma bellingshausensis and P. melandi are described from specimens sampled with a suprabenthic sled in the Bellingshausen Sea (Southern Ocean). P. bellingshausensis and P. melandi are distinguishable from its closest congeners, P. antarcticum Zimmer, 1914, P. jasi Meland & Brattegard, 1995 and P. islandicum Meland & Brattegard, 2007 by ocular plate sculpturing and telson armature. A key for the Antarctic and Subantarctic Pseudomma species is also included.

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21

Graham, Felicity S., Jason L. Roberts, Ben K. Galton-Fenzi, Duncan Young, Donald Blankenship, and Martin J. Siegert. "A high-resolution synthetic bed elevation grid of the Antarctic continent." Earth System Science Data 9, no. 1 (May 5, 2017): 267–79. http://dx.doi.org/10.5194/essd-9-267-2017.

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Abstract. Digital elevation models of Antarctic bed topography are smoothed and interpolated onto low-resolution ( > 1 km) grids as current observed topography data are generally sparsely and unevenly sampled. This issue has potential implications for numerical simulations of ice-sheet dynamics, especially in regions prone to instability where detailed knowledge of the topography, including fine-scale roughness, is required. Here, we present a high-resolution (100 m) synthetic bed elevation terrain for Antarctica, encompassing the continent, continental shelf, and seas south of 60° S. Although not identically matching observations, the synthetic bed surface – denoted as HRES – preserves topographic roughness characteristics of airborne and ground-based ice-penetrating radar data measured by the ICECAP (Investigating the Cryospheric Evolution of the Central Antarctic Plate) consortium or used to create the Bedmap1 compilation. Broad-scale ( > 5 km resolution) features of the Antarctic landscape are incorporated using a low-pass filter of the Bedmap2 bed elevation data. HRES has applicability in high-resolution ice-sheet modelling studies, including investigations of the interaction between topography, ice-sheet dynamics, and hydrology, where processes are highly sensitive to bed elevations and fine-scale roughness. The data are available for download from the Australian Antarctic Data Centre (doi:10.4225/15/57464ADE22F50).

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22

Galindo-Zaldı́var, J., J. C. Balanyá, F. Bohoyo, A. Jabaloy, A. Maldonado, J. M. Martı́nez-Martı́nez, J. Rodrı́guez-Fernández, and E. Suriñach. "Active crustal fragmentation along the Scotia–Antarctic plate boundary east of the South Orkney Microcontinent (Antarctica)." Earth and Planetary Science Letters 204, no. 1-2 (November 2002): 33–46. http://dx.doi.org/10.1016/s0012-821x(02)00959-7.

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23

Jagoda, Marcin, Miłosława Rutkowska, Czesław Suchocki, and Jacek Katzer. "Determination of the tectonic plates motion parameters based on SLR, DORIS and VLBI stations positions." Journal of Applied Geodesy 14, no. 2 (April 26, 2020): 121–31. http://dx.doi.org/10.1515/jag-2019-0053.

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AbstractOn the base of International Terrestrial Reference Frame 2008 (ITRF2008) a new global plate model of station positions and velocities with accuracy 1–3 mm and 1 mm per year respectively was established. Next, this model was used in our paper for plate motion parameters estimation for the major plates as Eurasian, North American, Pacific and small plates as Australian, African and Antarctic on the base of the observation campaigns for three techniques: Satellite Laser Ranging (SLR), Doppler Orbitography by Radiopositioning Integrated on Satellite system (DORIS) and Very Long Baseline Interferometry (VLBI), each technique was analyzed separately. Investigation for GNSS technique is scheduled to take place in the future. The plate motion parameters were adjusted using least squares method and sequential solution. In the first stage, the plate motion parameters were determined for two selected stations and next stations were added until stability of the solution was observed. Final results of our solution were compared with the APKIM 2005 IGN model by H. Drewes. Agreement of solutions is order 2 degrees or better.

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24

Whittaker, J. M., R. D. Muller, G. Leitchenkov, H. Stagg, M. Sdrolias, C. Gaina, and A. Goncharov. "Major Australian-Antarctic Plate Reorganization at Hawaiian-Emperor Bend Time." Science 318, no. 5847 (October 5, 2007): 83–86. http://dx.doi.org/10.1126/science.1143769.

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25

Tretyak, Kornylii, Al-Alusi Forat, and Yurii Holubinka. "Investigation of Changes of the Kinematic Parameters of Antarctic Tectonic Plate Using Data Observations of Permanent GNSS Stations." Reports on Geodesy and Geoinformatics 103, no. 1 (June 27, 2017): 119–35. http://dx.doi.org/10.1515/rgg-2017-0010.

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Abstract The paper describes a modified algorithm of determination of the Euler pole coordinates and angular velocity of the tectonic plate, considering the continuous and uneven distribution of daily measurements of GNSS permanent stations. Using developed algorithm were determined the mean position of Euler pole and angular velocity of Antarctic tectonic plate and their annual changes. As the input data, we used the results of observations, collected on 28 permanent stations of the Antarctic region, within the period from 1996 to 2014.

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LÖRZ, ANNE-NINA. "Synopsis of Amphipoda from two recent Ross Sea voyages with description of a new species of Epimeria (Epimeriidae, Amphipoda, Crustacea)." Zootaxa 2167, no. 1 (July 24, 2009): 59–68. http://dx.doi.org/10.11646/zootaxa.2167.1.4.

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Two recent voyages to the Ross Sea in 2004 and 2008 collected over 3000 benthic Amphipoda. The composition of 30 amphipod families is presented, and a focus is given to the family Epimeriidae from which a new species described. Epimeria larsi sp. nov. from 1950 m depth, is the deepest occurring species of the genus known from Antarctic waters. This increases the number of known species of Epimeriidae from Antarctica to 27. Epimeria larsi can be distinguished from similar species by the unique combination of following characters: coxa 5 posteroventral corner produced, epimeral plate posteroventral corner rounded, and coxa 1–3 apically rounded.

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27

George, R. W. "Tectonic plate movements and the evolution of Jasus and Panulirus spiny lobsters (Palinuridae)." Marine and Freshwater Research 48, no. 8 (1997): 1121. http://dx.doi.org/10.1071/mf97202.

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Jasus is at least as old as early Miocene (20 Ma). Genetic differentiation between J. verreauxi in Australia and New Zealand indicates larval isolation across the northern Tasman Sea following a northward retreat of a strong south-flowing warm current. After South Africa and Australia separated from Antarctica, stocks of the temperate J. lalandii subgroup of three species became genetically isolated because of reduced larval exchange by tracking of local environments. Once the full strength of the Antarctic Circumpolar Current was established, a series of subantarctic islands and seamounts provided new habitats for four species of the J. frontalis subgroup, and their larvae responded to local circulation systems. Speciation of nine species or subspecies of Indo–West Pacific Panulirus probably occurred between 9 and 3.5 Ma (late Miocene to early Pliocene) as a result of the formation of new habitats after collisions of India and Australia with the Asian plate. Major mountain chains resulted in high continental run-off, produced regular tropical monsoon systems, enhanced regional upwelling, altered oceanographic circulation patterns and restricted larval transport between the Pacific and Indian Oceans.

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Eagles, Graeme. "Tectonic evolution of the Antarctic–Phoenix plate system since 15 Ma." Earth and Planetary Science Letters 217, no. 1-2 (January 1, 2004): 97–109. http://dx.doi.org/10.1016/s0012-821x(03)00584-3.

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29

Bouin, Marie-Noëlle, and Christophe Vigny. "New constraints on Antarctic plate motion and deformation from GPS data." Journal of Geophysical Research: Solid Earth 105, B12 (December 10, 2000): 28279–93. http://dx.doi.org/10.1029/2000jb900285.

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30

Cande, Steven C., and Joann M. Stock. "Pacific-Antarctic-Australia motion and the formation of the Macquarie Plate." Geophysical Journal International 157, no. 1 (April 2004): 399–414. http://dx.doi.org/10.1111/j.1365-246x.2004.02224.x.

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31

Eagles, Graeme, and Benjamin G. C. Scott. "Plate convergence west of Patagonia and the Antarctic Peninsula since 61Ma." Global and Planetary Change 123 (December 2014): 189–98. http://dx.doi.org/10.1016/j.gloplacha.2014.08.002.

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32

Turner, Ross J., Anya M. Reading, and Matt A. King. "Separation of tectonic and local components of horizontal GPS station velocities: a case study for glacial isostatic adjustment in East Antarctica." Geophysical Journal International 222, no. 3 (May 30, 2020): 1555–69. http://dx.doi.org/10.1093/gji/ggaa265.

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SUMMARY Accurate measurement of the local component of geodetic motion at GPS stations presents a challenge due to the need to separate this signal from the tectonic plate rotation. A pressing example is the observation of glacial isostatic adjustment (GIA) which constrains the Earth’s response to ice unloading, and hence, contributions of ice-covered regions such as Antarctica to global sea level rise following ice mass loss. While both vertical and horizontal motions are of interest in general, we focus on horizontal GPS velocities which typically contain a large component of plate rotation and a smaller local component primarily relating to GIA. Incomplete separation of these components introduces significant bias into estimates of GIA motion vectors. We present the results of a series of tests based on the motions of GPS stations from East Antarctica: (1) signal separation for sets of synthetic data that replicate the geometric character of non-separable, and separable, GIA-like horizontal velocities; and (2) signal separation for real GPS station data with an appraisal of uncertainties. For both synthetic and real motions, we compare results where the stations are unweighted, and where each station is areal-weighted using a metric representing the inverse of the spatial density of neighbouring stations. From the synthetic tests, we show that a GIA-like signal is recoverable from the plate rotation signal providing it has geometric variability across East Antarctica. We also show that areal-weighting has a very significant effect on the ability to recover a GIA-like signal with geometric variability, and hence on separating the plate rotation and local components. For the real data, assuming a rigid Antarctic plate, fitted plate rotation parameters compare well with other studies in the literature. We find that 25 out of 36 GPS stations examined in East Antarctica have non-zero local horizontal velocities, at the 2σ level, after signal separation. We make the code for weighted signal separation available to assist in the consistent appraisal of separated signals, and the comparison of likely uncertainty bounds, for future studies.

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Maestro, A., J. López-Martínez, F. Bohoyo, M. Montes, F. Nozal, S. Santillana, and S. Marenssi. "Geodynamic implications of the Cenozoic stress field on Seymour Island, West Antarctica." Antarctic Science 20, no. 2 (January 21, 2008): 173–84. http://dx.doi.org/10.1017/s0954102007000892.

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AbstractPalaeostress inferred from brittle mesostructures in Seymour (Marambio) Island indicates a Cenozoic to Recent origin for an extensional stress field, with only local compressional stress states. Minimum horizontal stress (σ3) orientations are scattered about two main NE–SW and NW–SE modes suggesting that two stress sources have been responsible for the dominant minimum horizontal stress directions in the north-western Weddell Sea. Extensional structures within a broad-scale compressional stress field can be linked to both the decrease in relative stress magnitudes from active margins to intraplate regions and the rifting processes that occurred in the northern Weddell Sea. Stress states with NW–SE trending σ3are compatible with back-arc extension along the eastern Antarctic Peninsula. We interpret this as due to the opening of the Larsen Basin during upper Cretaceous to Eocene and to the spreading, from Pliocene to present, of the Bransfield Basin (western Antarctic Peninsula), both due to former Phoenix Plate subduction under the Antarctic Plate. NE–SW σ3orientations could be expressions of continental fragmentation of the northern Antarctic Peninsula controlling eastwards drifting of the South Orkney microcontinent and other submerged continental blocks of the southern Scotia Sea.

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Maestro, Adolfo, and Jerónimo López-Martínez. "Cenozoic stress field in the southwestern Antarctic Peninsula from brittle mesostructures in Wright Peninsula, Adelaide Island." Polish Polar Research 32, no. 1 (January 1, 2011): 39–58. http://dx.doi.org/10.2478/v10183-011-0006-8.

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Cenozoic stress field in the southwestern Antarctic Peninsula from brittle mesostructures in Wright Peninsula, Adelaide IslandPalaeostresses inferred from brittle mesostructures in the southern Wright Peninsula show a stress field characterized by compressional, strike-slip and extensional regime stress states. The compressional stress (σ1) shows a main NW-SE direction and the extensional stress (σ3) shows a relative scattering with two main modes: NE-SW to E-W and NW-SE. The maximum horizontal stress (σy) has a bimodal distribution with NW-SE and NE-SW direction. The compressional orientation is related to subduction of the former Phoenix Plate under the Antarctic Plate from the Early Jurassic to the Early Miocene. Extensional structures within a broad-scale compressional stress field can be related to both the decrease in relative stress magnitudes from active margins to intraplate regions and stretching processes occurring in eastern Adelaide Island, which develop a fore-arc or intra-arc basin from the Early Miocene. Stress states with NW-SE-trending σ1are compatible with the dominant pattern established for the western Antarctic Peninsula. NW-SE orientations of σ3suggest the occurrence of tectonic forces coming from fore-arc extension along the western Antarctic Peninsula.

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35

D'ACOZ, CÉDRIC D'UDEKEM, and SAMMY DEGRAVE. "A new genus and species of large-bodied caridean shrimp from the Crozet Islands, Southern Ocean (Crustacea, Decapoda, Lipkiidae) with a checklist of Antarctic and sub-Antarctic shrimps." Zootaxa 4392, no. 2 (March 8, 2018): 201. http://dx.doi.org/10.11646/zootaxa.4392.2.1.

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A new, over 10 cm long, sub-Antarctic shrimp, Fresnerhynchus crozeti n. gen., n. sp. is described based on a unique specimen collected with long lines at 1889 m on the slope of a seamount northwest of the Crozet Islands. It is included in the previously monotypic family Lipkiidae Burukovsky, 2012 based on morphological and molecular data. However, the posterior pereiopods of Fresnerhynchus are reminiscent to those of the Rhynchocinetidae, especially by the short spinose dactyli, and by the absence of a sternal plate. The elusive nature of F. crozeti, which is a large and highly characteristic shrimp, is attributed to its putative habitat (hard bottom, steep deep sea slopes), which is difficult to sample with conventional gear, and the remote geographical location. A brief discussion on the biogeography of Antarctic and sub-Antarctic decapods is provided. A review of Antarctic and sub-Antarctic dendrobranchiate and caridean shrimps is appended.

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Barker, P. F., and L. A. Lawver. "South American-Antarctic plate motion over the past 50 Myr, and the evolution of the South American-Antarctic ridge." Geophysical Journal International 94, no. 3 (September 1, 1988): 377–86. http://dx.doi.org/10.1111/j.1365-246x.1988.tb02261.x.

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37

Antonioli, A. "Dynamic Stress Triggering during the Great 25 March 1998 Antarctic Plate Earthquake." Bulletin of the Seismological Society of America 92, no. 3 (April 1, 2002): 896–903. http://dx.doi.org/10.1785/0120010164.

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38

Lodolo, Emanuele, and Franco Coren. "A Late Miocene plate boundary reorganization along the westernmost Pacific-Antarctic ridge." Tectonophysics 274, no. 4 (June 1997): 295–305. http://dx.doi.org/10.1016/s0040-1951(97)00005-x.

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39

Kristoffersen, Yngve, and Kristen Haugland. "Geophysical evidence for the East Antarctic plate boundary in the Weddell Sea." Nature 322, no. 6079 (August 1986): 538–41. http://dx.doi.org/10.1038/322538a0.

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40

Tikku, A. A., and N. G. Direen. "Comment on "Major Australian-Antarctic Plate Reorganization at Hawaiian-Emperor Bend Time"." Science 321, no. 5888 (July 25, 2008): 490. http://dx.doi.org/10.1126/science.1157163.

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41

Dietrich, Reinhard, Axel Rülke, Johannes Ihde, Klaus Lindner, Hubert Miller, Wolfgang Niemeier, Hans-Werner Schenke, and Günter Seeber. "Plate kinematics and deformation status of the Antarctic Peninsula based on GPS." Global and Planetary Change 42, no. 1-4 (July 2004): 313–21. http://dx.doi.org/10.1016/j.gloplacha.2003.12.003.

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42

Croon, Marcel B., Steven C. Cande, and Joann M. Stock. "Revised Pacific-Antarctic plate motions and geophysics of the Menard Fracture Zone." Geochemistry, Geophysics, Geosystems 9, no. 7 (July 2008): n/a. http://dx.doi.org/10.1029/2008gc002019.

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43

Solari, M. A., F. Hervé, J. Martinod, J. P. Le Roux, L. E. Ramírez, and C. Palacios. "Geotectonic evolution of the Bransfield Basin, Antarctic Peninsula: insights from analogue models." Antarctic Science 20, no. 2 (January 23, 2008): 185–96. http://dx.doi.org/10.1017/s095410200800093x.

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AbstractThe Bransfield Strait, located between the South Shetland Islands and the north-western end of the Antarctic Peninsula, is a back-arc basin transitional between rifting and spreading. We compiled a geomorphological structural map of the Bransfield Basin combining published data and the interpretation of bathymetric images. Several analogue experiments reproducing the interaction between the Scotia, Antarctic, and Phoenix plates were carried out. The fault configuration observed in the geomorphological structural map was well reproduced by one of these analogue models. The results suggest the establishment of a transpressional regime to the west of the southern segment of the Shackleton Fracture Zone and a transtensional regime to the south-west of the South Scotia Ridge by at least c. 7 Ma. A probable mechanism for the opening of the Bransfield Basin requires two processes: 1) Significant transtensional effects in the Bransfield Basin caused by the configuration and drift vector of the Scotia Plate after the activity of the West Scotia Ridge ceased at c. 7 Ma. 2) Roll-back of the Phoenix Plate under the South Shetland Islands after cessation of spreading activity of the Phoenix Ridge at 3.3 ± 0.2 Ma, causing the north-westward migration of the South Shetland Trench.

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Ricci, C. A., F. Talarico, R. Palmeri, G. Di Vincenzo, and P. C. Pertusati. "Eclogite at the Antarctic palaeo-Pacific active margin of Gondwana (Lanterman Range, northern Victoria Land, Antarctica)." Antarctic Science 8, no. 3 (September 1996): 277–80. http://dx.doi.org/10.1017/s0954102096000399.

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Well-preserved eclogites were found for the first time in Antarctica, at the Lanterman Range, northern Victoria Land. They are part of a mafic–ultramafic belt that lies between the Wilson Terrane, representing part of the palaeo-Pacific margin of Gondwana, and the Bowers Terrane, a Cambro-Ordovician volcanic are and related sediments, accreted to the margin during the Ross Orogeny. The eclogites formed at temperatures in the range 750–850°C and pressures above 15 kbar and subsequently experienced a decompressional path to low pressure amphibolite facies conditions. The formation and exhumation of eclogites and the attainment of the metamorphic peak in adjacent rock units is consistent with a plate convergent setting model at the palaeo-Pacific margin of Gondwana.

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45

Henry, C., S. Das, and J. H. Woodhouse. "The great March 25, 1998, Antarctic Plate earthquake: Moment tensor and rupture history." Journal of Geophysical Research: Solid Earth 105, B7 (July 10, 2000): 16097–118. http://dx.doi.org/10.1029/2000jb900077.

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46

Danesi, S., and A. Morelli. "Structure of the upper mantle under the Antarctic Plate from surface wave tomography." Geophysical Research Letters 28, no. 23 (December 1, 2001): 4395–98. http://dx.doi.org/10.1029/2001gl013431.

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47

Tretyak, K. R., and F. K. F. Al-Alusi. "About relationship of uneven of the Earth rotational movement and Antarctic tectonic plate." Ukrainian Antarctic Journal, no. 14 (2015): 43–57. http://dx.doi.org/10.33275/1727-7485.14.2015.171.

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48

Galindo-Zaldívar, J., A. Jabaloy, A. Maldonado, and C. Sanz de Galdeano. "Continental fragmentation along the South Scotia Ridge transcurrent plate boundary (NE Antarctic Peninsula)." Tectonophysics 258, no. 1-4 (June 1996): 275–301. http://dx.doi.org/10.1016/0040-1951(95)00211-1.

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49

Abneuf, Mohammed A., Abiramy Krishnan, Marcelo Gonzalez Aravena, Ka-Lai Pang, Peter Convey, Nuradilla Mohamad-Fauzi, Mohammed Rizman-Idid, and Siti Aisyah Alias. "Antimicrobial activity of microfungi from maritime Antarctic soil." Czech Polar Reports 6, no. 2 (July 1, 2016): 141–54. http://dx.doi.org/10.5817/cpr2016-2-13.

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The search for cold-adapted and cold-active fungi in extreme environments provides the potential for discovering new species and novel bioactive compounds. In this study, soil samples were collected from Deception Island, Wilhelmina Bay (north-west Antarctic Peninsula, Graham Land) and Yankee Bay (Greenwich Island), maritime Antarctica, for the isolation of soil fungi and determination of their antimicrobial activity. The soil-plate method, agar block, disc diffusion and broth micro-dilution assays were applied to characterize the thermal classes and antimicrobial activity of the isolated fungi. A total of 27 isolates of fungi were obtained from 14 soil samples, including 13 Ascomycota, 4 Zygomycota and 10 anamorphic fungi. Cold-active (psychrotolerant) fungi predominated over cold-adapted (psychrophilic) fungi. In the antimicrobial assay, 16 isolates showed substantial inhibitory activity against test bacterial pathogens. Ethyl acetate extracts of 10 competent isolates showed significant inhibition of bacterial pathogens. Antifungal activity was observed in the disc diffusion assay, but not in the agar block assay. Minimum inhibitory, bactericidal and fungicidal concentrations were determined using the broth micro-dilution method, with an average in the range of 0.78-25 mg ml-1 on the test microorganisms. Isolate WHB-sp. 7 showed the best broad spectrum antimicrobial activity, with the potential for biotechnological studies in antibiotic development.

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Hill, K. A., D. M. Finlayson, K. C. Hill, and G. T. Cooper. "MESOZOIC TECTONICS OF THE OTWAY BASIN REGION: THE LEGACY OF GONDWANA AND THE ACTVE PACIFIC MARGIN—A REVIEW AND ONGOING RESEARCH." APPEA Journal 35, no. 1 (1995): 467. http://dx.doi.org/10.1071/aj94030.

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Mesozoic extension along Australia's southern margin and the evolution and architecture of the Otway Basin were probably controlled by three factors: 1) changes in global plate movements driven by mantle processes; 2) the structural grain of Palaeozoic basement; and, 3) changes in subduction along Gondwana's Pacific margin. Major plate realignments controlled the Jurassic onset of rifting, the mid-Cretaceous break-up and the Eocene onset of rapid spreading in the Southern Ocean.The initial southern margin rift site was influenced by the northern limit of Pacific margin (extensional) Jurassic dolerites and the rifting may have terminated dolerite emplacement. Changed conditions of Pacific margin subduction (e.g. ridge subduction) in the Aptian may have placed the Australia-Antarctic plates into minor compression, abating Neocomian southern margin rifting. It also produced vast amounts of volcanolithic sediment from the Pacific margin arc that was funnelled down the rift graben, causing additional regional subsidence due to loading. Albian orogenic collapse of the Pacific margin, related to collision with the Phoenix Plate, influenced mid-Cretaceous breakup propagating south of Tasmania and into the Tasman Sea.Major offsets of the spreading axis during breakup, at the Tasman and Spencer Fracture zones, were most likely controlled by the location of Palaeozoic terrane boundaries. The Tasman Fracture System was reactivated during break-up, with considerable uplift and denudation of the Bass failed rift to the east, which controlled Otway Basin facies distribution. Palaeozoic structures also had a significant effect in determining the half graben orientations within a general N-S extensional regime during early Cretaceous rifting. The late Cretaceous second stage of rifting, seaward of the Tartwaup, Timboon and Sorell fault zones, left a stable failed rift margin to the north, but the attenuated lithosphere of the Otway-Sorell microplate to the south records repeated extension that led to continental separation and may be part of an Antarctic upper plate.

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