The Central Scotia Sea Floor – Palaeo-Oceanic Plate, Young Riftogenous Plate or Palaeo-Land Scotia?
Although the bathymetry and geophysics of the Scotia Sea basin is rather well studied in general and is discussed in many publications there are still remaining questions about tectonics of its Central Part. In the western part of the Sea tectonic nature is well demonstrated by West rifted ridge and...
Збережено в:
| Опубліковано в: : | Український антарктичний журнал |
|---|---|
| Дата: | 2009 |
| Автори: | , |
| Формат: | Стаття |
| Мова: | English |
| Опубліковано: |
Національний антарктичний науковий центр МОН України
2009
|
| Теми: | |
| Онлайн доступ: | https://nasplib.isofts.kiev.ua/handle/123456789/128550 |
| Теги: |
Додати тег
Немає тегів, Будьте першим, хто поставить тег для цього запису!
|
| Назва журналу: | Digital Library of Periodicals of National Academy of Sciences of Ukraine |
| Цитувати: | The Central Scotia Sea Floor – Palaeo-Oceanic Plate, Young Riftogenous Plate or Palaeo-Land Scotia? / H.W. Schenke, G.B. Udintsev // Український антарктичний журнал. — 2009. — № 8. — С. 57-66. — Бібліогр.: 44 назв. — англ. |
Репозитарії
Digital Library of Periodicals of National Academy of Sciences of Ukraine| id |
nasplib_isofts_kiev_ua-123456789-128550 |
|---|---|
| record_format |
dspace |
| spelling |
Schenke, H.W. Udintsev, G.B. 2018-01-11T18:40:10Z 2018-01-11T18:40:10Z 2009 The Central Scotia Sea Floor – Palaeo-Oceanic Plate, Young Riftogenous Plate or Palaeo-Land Scotia? / H.W. Schenke, G.B. Udintsev // Український антарктичний журнал. — 2009. — № 8. — С. 57-66. — Бібліогр.: 44 назв. — англ. 1727-7485 https://nasplib.isofts.kiev.ua/handle/123456789/128550 551.462.543(1-923) Although the bathymetry and geophysics of the Scotia Sea basin is rather well studied in general and is discussed in many publications there are still remaining questions about tectonics of its Central Part. In the western part of the Sea tectonic nature is well demonstrated by West rifted ridge and in the eastern part by East back-arc rift. The floor of the central part does not show such well expressed tectonic features. The usual interpretation of that part of basin floor is described as introduced fragment of the Pacific paleo-Plate or as newly created oceanic plate resulted by supposed rifting. Recent bathymetry and other geophysics survey is complemented with geological sampling lead to hypothesis on the existence there of a large relict of continental bridge between South America and West Antarctica. Хотя рельеф дна и геофизические параметры ложа котловины моря Скоша в общем изучены довольно хорошо и рассматривались во многих публикациях, всё же до сих пор остаются вопросы о тектонике центральной части ложа этой котловины. Тектоническая природа западной части дна моря Скоша хорошо демонстрируется Западным рифтогенным хребтом, а в восточной части – Восточным задуговым рифтом. Центральная часть ложа котловины обычно интерпретируется как внедрённый фрагмент Тихоокеанской плиты или как заново созданная океаническая плита, результатпредполагаемого рифтогенеза. Новейшие исследования рельефа дна и другие геофизические съёмки в сочетании со сбором геологических образцов приводят к предположению о существовании там большого реликта континентального моста между Южной Америкой и Западной Антарктидой – палео-Земли Скоша. Хоча рельєф дна і геофізичні параметри ложа котловини моря Скоша загалом вивчені досить добре і роглядалися в багатьох публікаціях, усе ж таки й досі залишаються питання щодо тектоніки центральної частини ложа цієї котловини. Тектонічна частина природи західної частини дна моря Скоша добре демонструється Західним рифтогенним хребтом, а у східній частині – Східним задуговим рифтом. Центральна частина ложа котловини зазвичай інтерпретується як упроваджений фрагмент Тихоокеанської плити або як заново створена океанічна плита, результат гаданого рифтогенезу. Найновіші дослідження рельєфу дна та інші геофізичні зйомки у сполученні зі збиранням геологічних зразків приводять до припущень про існування там великого релікту континентального моста поміж Південною Америкою і Західною Антарктидою – палео-Землі Скоша. en Національний антарктичний науковий центр МОН України Український антарктичний журнал Геолого-геофізичні дослідження The Central Scotia Sea Floor – Palaeo-Oceanic Plate, Young Riftogenous Plate or Palaeo-Land Scotia? Article published earlier |
| institution |
Digital Library of Periodicals of National Academy of Sciences of Ukraine |
| collection |
DSpace DC |
| title |
The Central Scotia Sea Floor – Palaeo-Oceanic Plate, Young Riftogenous Plate or Palaeo-Land Scotia? |
| spellingShingle |
The Central Scotia Sea Floor – Palaeo-Oceanic Plate, Young Riftogenous Plate or Palaeo-Land Scotia? Schenke, H.W. Udintsev, G.B. Геолого-геофізичні дослідження |
| title_short |
The Central Scotia Sea Floor – Palaeo-Oceanic Plate, Young Riftogenous Plate or Palaeo-Land Scotia? |
| title_full |
The Central Scotia Sea Floor – Palaeo-Oceanic Plate, Young Riftogenous Plate or Palaeo-Land Scotia? |
| title_fullStr |
The Central Scotia Sea Floor – Palaeo-Oceanic Plate, Young Riftogenous Plate or Palaeo-Land Scotia? |
| title_full_unstemmed |
The Central Scotia Sea Floor – Palaeo-Oceanic Plate, Young Riftogenous Plate or Palaeo-Land Scotia? |
| title_sort |
central scotia sea floor – palaeo-oceanic plate, young riftogenous plate or palaeo-land scotia? |
| author |
Schenke, H.W. Udintsev, G.B. |
| author_facet |
Schenke, H.W. Udintsev, G.B. |
| topic |
Геолого-геофізичні дослідження |
| topic_facet |
Геолого-геофізичні дослідження |
| publishDate |
2009 |
| language |
English |
| container_title |
Український антарктичний журнал |
| publisher |
Національний антарктичний науковий центр МОН України |
| format |
Article |
| description |
Although the bathymetry and geophysics of the Scotia Sea basin is rather well studied in general and is discussed in many publications there are still remaining questions about tectonics of its Central Part. In the western part of the Sea tectonic nature is well demonstrated by West rifted ridge and in the eastern part by East back-arc rift. The floor of the central part does not show such well expressed tectonic features. The usual interpretation of that part of basin floor is described as introduced fragment of the Pacific paleo-Plate or as newly created oceanic plate resulted by supposed rifting. Recent bathymetry and other geophysics survey is complemented with geological sampling lead to hypothesis on the existence there of a large relict of continental bridge between South America and West Antarctica.
Хотя рельеф дна и геофизические параметры ложа котловины моря Скоша в общем изучены довольно хорошо и рассматривались во многих публикациях, всё же до сих пор остаются вопросы о тектонике центральной части ложа этой котловины. Тектоническая природа западной части дна моря Скоша хорошо демонстрируется Западным рифтогенным хребтом, а в восточной части – Восточным задуговым рифтом. Центральная часть ложа котловины обычно интерпретируется как внедрённый фрагмент Тихоокеанской плиты или как заново созданная океаническая плита, результатпредполагаемого рифтогенеза. Новейшие исследования рельефа дна и другие геофизические съёмки в сочетании со сбором геологических образцов приводят к предположению о существовании там большого реликта континентального моста между Южной Америкой и Западной Антарктидой – палео-Земли Скоша.
Хоча рельєф дна і геофізичні параметри ложа котловини моря Скоша загалом вивчені досить добре і роглядалися в багатьох публікаціях, усе ж таки й досі залишаються питання щодо тектоніки центральної частини ложа цієї котловини. Тектонічна частина природи західної частини дна моря Скоша добре демонструється Західним рифтогенним хребтом, а у східній частині – Східним задуговим рифтом. Центральна частина ложа котловини зазвичай інтерпретується як упроваджений фрагмент Тихоокеанської плити або як заново створена океанічна плита, результат гаданого рифтогенезу. Найновіші дослідження рельєфу дна та інші геофізичні зйомки у сполученні зі збиранням геологічних зразків приводять до припущень про існування там великого релікту континентального моста поміж Південною Америкою і Західною Антарктидою – палео-Землі Скоша.
|
| issn |
1727-7485 |
| url |
https://nasplib.isofts.kiev.ua/handle/123456789/128550 |
| citation_txt |
The Central Scotia Sea Floor – Palaeo-Oceanic Plate, Young Riftogenous Plate or Palaeo-Land Scotia? / H.W. Schenke, G.B. Udintsev // Український антарктичний журнал. — 2009. — № 8. — С. 57-66. — Бібліогр.: 44 назв. — англ. |
| work_keys_str_mv |
AT schenkehw thecentralscotiaseafloorpalaeooceanicplateyoungriftogenousplateorpalaeolandscotia AT udintsevgb thecentralscotiaseafloorpalaeooceanicplateyoungriftogenousplateorpalaeolandscotia AT schenkehw centralscotiaseafloorpalaeooceanicplateyoungriftogenousplateorpalaeolandscotia AT udintsevgb centralscotiaseafloorpalaeooceanicplateyoungriftogenousplateorpalaeolandscotia |
| first_indexed |
2025-11-25T06:56:09Z |
| last_indexed |
2025-11-25T06:56:09Z |
| _version_ |
1850509777774313472 |
| fulltext |
THE CENTRAL SCOTIA SEA FLOOR – IS IT AN PALEO-OCEANIC PLATE, AN YOUNG
RIFTED PLATE OR AN PALEO-LAND SCOTIA?
1 2Schenke H.W. , Udintsev G.B.
1 Alfred-Wegener Institute of Polar and Marine Research, Bremerhaven, Germany
2 Vernadsky Institute of geochemistry and analytical chemistry, Russian Academy of sciences, Moscow, Russia
Abstract. Although the bathymetry and geophysics of the Scotia Sea basin is rather well studied in general and is
discussed in many publications there are still remaining questions about tectonics of its Central Part. In the
western part of the Sea tectonic nature is well demonstrated by West rifted ridge and in the eastern part by East
back-arc rift. The floor of the central part does not show such well expressed tectonic features. The usual
interpretation of that part of basin floor is described as introduced fragment of the Pacific paleo-Plate or as newly
created oceanic plate resulted by supposed rifting. Recent bathymetry and other geophysics survey is
complemented with geological sampling lead to hypothesis on the existence there of a large relict of continental
bridge between South America and West Antarctica.
Key words: the Scotia Sea, rift, geophysical surveys, West Antarctica.
Ðåôåðàò. Õîòÿ ðåëüåô äíà è ãåîôèçè÷åñêèå ïàðàìåòðû ëîæà êîòëîâèíû ìîðÿ Ñêîøà â îáùåì èçó÷åíû
äîâîëüíî õîðîøî è ðàññìàòðèâàëèñü âî ìíîãèõ ïóáëèêàöèÿõ, âñ¸ æå äî ñèõ ïîð îñòàþòñÿ âîïðîñû î
òåêòîíèêå öåíòðàëüíîé ÷àñòè ëîæà ýòîé êîòëîâèíû. Òåêòîíè÷åñêàÿ ïðèðîäà çàïàäíîé ÷àñòè äíà ìîðÿ
Ñêîøà õîðîøî äåìîíñòðèðóåòñÿ Çàïàäíûì ðèôòîãåííûì õðåáòîì, à â âîñòî÷íîé ÷àñòè – Âîñòî÷íûì
çàäóãîâûì ðèôòîì. Öåíòðàëüíàÿ ÷àñòü ëîæà êîòëîâèíû îáû÷íî èíòåðïðåòèðóåòñÿ êàê âíåäð¸ííûé
ôðàãìåíò Òèõîîêåàíñêîé ïëèòû èëè êàê çàíîâî ñîçäàííàÿ îêåàíè÷åñêàÿ ïëèòà, ðåçóëüòàò
ïðåäïîëàãàåìîãî ðèôòîãåíåçà. Íîâåéøèå èññëåäîâàíèÿ ðåëüåôà äíà è äðóãèå ãåîôèçè÷åñêèå ñú¸ìêè â
ñî÷åòàíèè ñî ñáîðîì ãåîëîãè÷åñêèõ îáðàçöîâ ïðèâîäÿò ê ïðåäïîëîæåíèþ î ñóùåñòâîâàíèè òàì
áîëüøîãî ðåëèêòà êîíòèíåíòàëüíîãî ìîñòà ìåæäó Þæíîé Àìåðèêîé è Çàïàäíîé Àíòàðêòèäîé – ïàëåî-
Çåìëè Ñêîøà.
Êëþ÷åâûå ñëîâà: ìîðå Ñêîøà, ðèôò, îêåàíè÷åñêàÿ ïëèòà, ãåîôèçè÷åñêèå ñú¸ìêè, Çàïàäíàÿ
Àíòàðêòèäà.
Ðåôåðàò. Õî÷à ðåëüºô äíà ³ ãåîô³çè÷í³ ïàðàìåòðè ëîæà êîòëîâèíè ìîðÿ Ñêîøà çàãàëîì âèâ÷åí³ äîñèòü
äîáðå ³ ðîãëÿäàëèñÿ â áàãàòüîõ ïóáë³êàö³ÿõ, óñå æ òàêè é äîñ³ çàëèøàþòüñÿ ïèòàííÿ ùîäî òåêòîí³êè
öåíòðàëüíî¿ ÷àñòèíè ëîæà ö³º¿ êîòëîâèíè. Òåêòîí³÷íà ÷àñòèíà ïðèðîäè çàõ³äíî¿ ÷àñòèíè äíà ìîðÿ Ñêîøà
äîáðå äåìîíñòðóºòüñÿ Çàõ³äíèì ðèôòîãåííèì õðåáòîì, à ó ñõ³äí³é ÷àñòèí³ – Ñõ³äíèì çàäóãîâèì ðèôòîì.
Öåíòðàëüíà ÷àñòèíà ëîæà êîòëîâèíè çàçâè÷àé ³íòåðïðåòóºòüñÿ ÿê óïðîâàäæåíèé ôðàãìåíò
Òèõîîêåàíñüêî¿ ïëèòè àáî ÿê çàíîâî ñòâîðåíà îêåàí³÷íà ïëèòà, ðåçóëüòàò ãàäàíîãî ðèôòîãåíåçó.
Íàéíîâ³ø³ äîñë³äæåííÿ ðåëüºôó äíà òà ³íø³ ãåîô³çè÷í³ çéîìêè ó ñïîëó÷åíí³ ç³ çáèðàííÿì ãåîëîã³÷íèõ
çðàçê³â ïðèâîäÿòü äî ïðèïóùåíü ïðî ³ñíóâàííÿ òàì âåëèêîãî ðåë³êòó êîíòèíåíòàëüíîãî ìîñòà ïîì³æ
ϳâäåííîþ Àìåðèêîþ ³ Çàõ³äíîþ Àíòàðêòèäîþ – ïàëåî-Çåìë³ Ñêîøà.
Êëþ÷îâ³ ñëîâà: ìîðå Ñêîøà, ðèôò, îêåàí³÷íà ïëèòà, ãåîô³çè÷í³ çéîìêè, Çàõ³äíà Àíòàðêòèäà.
1. Introduction
Regional setting and history of previous investigations
The Scotia Sea is a large basin located between continental plates of South America and West
Antarctica. In the Scotia Sea bordered by volcanic South Sandwich Arc while the western side is
ÓÊÐÀ¯ÍÑÜÊÈÉ ÀÍÒÀÐÊÒÈ×ÍÈÉ
ÆÓÐÍÀË
ÓÀÆ ¹ 8, 57-66 (2009)
ÓÄÊ 551.462.543(1-923)
57
opened to Pacific Ocean. The Sea has received its geographical names in memory of works in
1901–1904 of the small research vessel «Scotia», operated by National Scottish Antarctic Expedition,
headed by William Bruce. Two shallow water banks in southern area of basin of the Scotia Sea were
named in memory of William Bruce and naturalist of his expedition James Pirie as Bruce and Pirie
banks. One other bank in environs was named as Discovery bank in memory of RRS «Discovery»,
headed by Captain Robert Scott.
The tectonic frame around the Scotia Sea is well expressed on the maps of «Tectonic Map of
the Scotia Arc» [BAS Misc. Sheets, scale 1;3 000 000, Cambridge,1985. Dalziel, Elliot, 1973, Barker,
Dalziel, Storey, 1991].The main tectonic features of this frame-work are huge Gondwanal cratonic
continental blocks - that are one of the extra-Andean Patagonia on the North side of the Sea and other
one the set of Antarctic Peninsula with the South Orkney micro-continent on the South side. The
mostly clear morphostructural framing of the Basin of the Scotia Sea are the Scotia Arc, surrounding
the Sea along three sides – on the north, on the east and at the south. On the western side of the Sea the
Gondwanal Andean oroclyn don't bend to the east, as it was supposed some time ago [Suess, 1883].
Now it is considered more probable that after continuation along the western side of the Terra del
Fuego this oroclyn was cutten by series of faults with horizontal displacements to the south while
opening of the Drake Passage in Cenozoic Time (Eocen-Oligocen) [Livermore, Eagles et al., 2004,
Herve, Miller, Pimpirev, 2006].
The geology of the Scotia Arc is unlike to classical island arcs of the Fiery Circum-Pacific
Ring. The North and South Ridges of the Scotia Arc are formed by systems of tectonic blocks –
splinters of the neighbor Precambrian Gondwanaland cratons. Only the east part of the arc, connecting
the North and South Ridges and closing the Scotia Sea from the Atlantic Ocean, is similar to majority
of the island arcs of the Pacific Belt. That is the volcanic South Sandwich Arc. That Arc are very
young. It consist of 11 islands and numerous banks – constructed by basalt and ryolite lavas with the
age 0,7 to 4 Ma [Tectonic map of the Scotia Arc, 1985].
The Eastern continuation of the extra-Andean Patagonia are the Falkland Plateau with
Maurice Ewing Bank, gradually submersing into the Northeast Georgia Rise in the area north of the
South Georgia island [Ludwig, 1983, Ludwig, Rabinowitz, 1982, Ludwig et al. 1978, Kristoffersen,
LaBrecque, 1991].
The narrow North Scotia Ridge, splinted from the huge pre-Cambrian craton of the extra-
Andean Patagonia, is separated from it by as well narrow Falkland trough. The depth of the trough are
lesser of the typical oceanic depths. The floor of the trough is underlined supposedly by thinned
continental crust [Ewing J.I. et al., 1971, Lorenzo, Mutter,1988],
The geology at the blocks of the North Scotia Ridge – the Burdwood bank, Blake, Aurora and
Shag Rocks, and the South Georgia Island everywhere are identical to the uppermost layers of the
Falkland Plateau and the Maurice Ewing Bank. That is Mesozoic shallow water sedimentary rocks
with age from upper Jurassic to lower Cretaceous, overlying Precambrian basement [Dalziel, Elliott,
1973, Barker, Dalziel, Storey, 1991].
The southern branch of the Scotia Arc – the South Scotia Ridge with South Orkney micro-
continent and Antarctic Peninsula – is similar in its structure with the North Scotia Ridge. All these
blocks are fragments of Gondwanals pre-Cambrian cratons, combined into continent of the West
Antarctica. The mostly preserved the pre-Mesozoic structure are exposed in the huge micro-
continental block of the South Orkney Islands and in the eastern back part of the Antarctic Peninsula.
The basement there is submitted by Paleozoic-Mesozoic complexes also. The distinctive feature of the
South Scotia Ridge and Antarctic Peninsula is the chain of propagating rifts. They can be considered as
far extended to the West continuation of the rift system of the America-Antarctic branch of the South
Atlantic mid-oceanic Ridge. The propagation of this rift is marked by intensive splitting of east part of
the South Scotia Ridge, then emerged inside of the South Orkney Island micro-continent [Barker,
Dalziel, Storey, 1991, King, Barker, 1988, Kavun, Vinnikovskaja, 1993], weakly active at the
Schenke H.W.: THE CENTRAL SCOTIA SEA FLOOR – IS IT AN PALEO-OCEANIC PLATE...
58
Hesperide rift to the west from this micro-continent, and represented by active East and West
Bransfield rifts [Gracia et al., 1996, Lawver et.al., 1996, Galindo-Zaldivar, Jabaloy, Maldonado,
Galdeano, 1996]
The rear structures of the South Scotia Ridge are even more complicated by combination of
the rifting with ancient regional spreading in northern part of the Weddell Sea [Livermore, Hunter,
1996], by dissipation of the Trans-Antarctic Rift in southern part of this sea, and by dyed local back-
arc rift of the Jain Basin, accompanied with Jain paleo-arc and young Powell Basin [King E.C. et al.,
1997]. However all this mosaic of structural systems does not mask continental residual basement of
the blocks of the South Scotia Ridge.
The central part of the Scotia Sea floor was marked as rather stable Central Plate both in
topography and gravity field and also in distribution of seismic activity, [Livermore, McAdoo, Marks,
1994]. Probably by virtue of marked stability it has attracted lesser attention of the researchers. The
known here Pirie, Bruce and Discovery banks, were considered as fine splinters of the ancient
continental bridge between South America and West Antarctica. The destruction of the former bridge
in the area of the Drake Passage is interpreted as resulted by large scale horizontal displacements of
continental plates reflected in linear magnetic anomalies [Barker P.F., et al., 1991; Tectonic map…,
1985; Barker, 1990, Barker, Thomas, 2004, Eagles, Livermore, Fairhead, Morris, 2005]. The Central
Plate of the Scotia Sea was imaged as the mosaic collage of small continental fragments, represented
by banks in the southern periphery, and by newly formed rifted oceanic basins in middle and northern
areas[Eagles G. et al., 2005].
The scarcity of previous studies of the Central Plate of the Scotia Sea for understanding its
tectonic and position in the process of the oceanic gateway's opening, stimulated our interest to its
topography, structure, geophysics and geology. In the frame of the German-Russian program for
studies the West Antarctic's geodynamics in the period of 1994–2005 there were maintained while five
expeditions – in two cruises of r/v «Academik Boris Petrov» and in three cruises of the r/v
«Polarstern».
2. The data obtained
Bathymetry and seismic profiling
In 1994–1998 in the expedition of the 21 cruise r/v «Akademik Boris Petrov» according to
German Project of geokinematic monitoring in Western Antarctic Region there was created the basic
network of geodetic stations in vatious points of this area.
In the expedition of the 29 cruise of that vessel the geokinematic monitoring was carried out.
In parallel to that operations the multibeam echo sounding, seismic profiling along the 59°S, box
survey and sampling of the rocks have been made in the area of the South Scotia Ridge and in the
South part of the Central Plate of the Scotia Sea at the Pirie Bank and Discovery Bank [Galimov E.Ì.
et al., 1999, Udintsev, Schenke, 2003]. In 2003–2005 while the r/v «Polarstern» expedition ANT-19/5
the detailed bathymetric survey and sampling at the Discovery Bank, and while ANT-22/4 the
especially detailed great box-survey with 110% of covering by multibeam echo sounding was
maintained at the northern part of the Central Plate [H.W.Schenke and W. Zenk, eds. Berichte zur
Polar und Meeresforschung, 537, 2006].
Elaboration of the data obtained by the research vessels in combination with results of the
Satellite altimetry [Sandwell, Smith, 1997] permit us to compile preliminary bathymetric charts of the
Central plate of the Scotia Sea. These maps are more detailed as any previously available.
The topography of the Central Plate is now clearer in its macro-features and micro-features.
The Pirie bank appeared as the pick of a small part of the top of an extensive rise, contoured in the
upper part by isobaths 1500 m, and near the foot of slopes by isobaths 3000 m – the Pirie Rise. To the
Schenke H.W.: THE CENTRAL SCOTIA SEA FLOOR – IS IT AN PALEO-OCEANIC PLATE...
59
North of it, in the area 58°40'S–57°30'S there are the plane terrace with the depths lesser 3200 m. This
terrace we named the Pirie Plateau. To the North of 57°30'S the series of the hills and narrow ridges
are positioned on the depth of the interval between 3200–3000 in the area up to 56°30'S. The largest
and highest hill of that area rise up to depth lesser than 2500 m. This complex of irregular topography is
like the marginal part of another large rise positioned to the north of 56°30'S. Uniting that rise with the
above described marginal hills we propose to name it in whole as the Gettingen Rise. The morphology
of that rise and its size inside isobaths 3300 m and uppermost tops with depths lesser than 2500–2000
m – resembles the morphology of the Pirie Rise.
The Pirie Rise together with Pirie Plateau and Gettingen Rise can be considered as united into
the large morpho-structural province. We propose to name it as the Pirie-Gettingen Province. Its
morpho-structure considered by us remarkable different from the structure of the rifted West Scotia
Ridge Province, which lay to the west and can be limited along the line directed from the Elephant
island, South Scotia Ridge, to N-E, to Shag Rocks of the North Scotia Ridge. The Pirie-Gettingen
Province can be considered as the west marginal system of the Central Plate. The northern limit of the
Province can be estimated by the deep trench, the name to which would be logic to give by the
neighbor block of the North Scotia Ridge capped with Shag Rocks – as the Shag Trench. The southern
limit of the Province corresponds to the deep South Orkney Trench.
In the limits of the structure of the Gettingen Rise are allocated sharp vertical dislocations
having the form of the Graben with rather wide Trough. We offer the name for this structure as the
Polarstern Graben. The width of the Pirie Graben' trough reaches 30 miles. The amplitude of the slopes
of the trough reach 1000-2000 m and its steepness achieves 25°–30° . Especially step is the northern
slope – its steepness on some places reaches almost 50°. The narrow profound troughs by the side of
the trough's bottom surface leveled by sediments are positioned at the foot of the steep slopes on both
sides of the Graben. Their depths reach 4000-4500 m, while the central depth of graben trough is only
3700–3800 m. The margins of a surface of the North Pirie Rise on the both boards of the trough are
raised up to depths lesser than 2300–2200 ì, reflecting, apparently, former dome uplift of wide arch,
laterally collapsed in center with tensional failure and creation of the graben. Detailed bathymetry
shows a small transverse ridge inside the northern part of the graben and 2000-2500 m depth on its
crest.
To the east of the graben large circular depression is founded in the pattern of the 3500 m
isobaths. The lens form deep is about 80-90 miles in diameter with a central depth at 56°45`S,
42°10`W of about 4400 m, a total of about 900 m of relief. The rim of the feature rises above
surrounding seafloor by about 100–200 m, which would suggest a crater-like structure, as opposed to a
simple basin. We propose to name this feature the Schott Basin in memory of outstanding German
oceanographer. The diameter of this circular feature is comparable to diameter of crater Maniguan of
Canada and crater of a Jucatan peninsula in the Gulf of Mexico. The ring structure of a Schott Basin
seems too imposed on structures of east part trough of the Polarstern Graben and, by this, was formed
after it.
The intensive dislocations of the floor shown on the recent mostly detailed bathymetry
certainly are remarkable. However not of lesser, but especially important for the understanding of the
genesis of the Pirie-Gettingen Province, its rises and plateau in the morphology of small forms, which
are dominated at the surface. The detailed survey has allowed to establish regular character of
morphology of the type of the hilly plains prevailing on overall surface of a Province. We can consider
these hilly plains as genetically homogeneous surfaces. The statistical analysis of their morphology
has allowed first of all to recognize dominant lineation of hilly crests making an orthogonal network
with azimuths NE-NS-NE.
The statistical analysis shows also existence of several planar levels between the hilly plains.
We have found out thus surfaces of hilly plains on depths 3400–3200 ì, 3200–3000 ì, 3000–2800 ì.
According the type of morphology we consider these planar surfaces as probable levels of subaerial
erosion.
Schenke H.W.: THE CENTRAL SCOTIA SEA FLOOR – IS IT AN PALEO-OCEANIC PLATE...
60
On a background of the large forms of topography such as extensive Rises of the Province the
several detached flat-topped seamounts with character form of volcanic cones are grouped on fracture
lines along steep scarps and cracks of surfaces.. The flat tops of these volcanic seamounts are the
ancient terraces of marine erosion submerged now to depths about 2400 m (Hinz smt), 2350 m (Seeber
smt), 2220 m (Wenzel smt), and 2025 m (Kertz smt) and 1800 m (Seibold smt). The planar surfaces of
highest parts of the above described Pirie Bank – 740 m , Bruce Bank – 1089 m and Discovery Bank –
350 m, also are the result of marine erosion at the period when they were at the sea level under
influence of sea waves activity. The disparity of the depth of these planar surfaces can be the evidence
of the progressive and unequivocal submergence of the Pirie Province.
The Discovery and Bruce Banks according our survey are similarly to the Pirie Bank the
highest parts of the large Rises of Sea floor. Their crests have the depth in the limits about1500–2500 m
and their foots are contoured by isobaths 3200–3400 m. That Rises can be named as Bruce Rise and
Discovery Rise. The southern halves of these rises are incorporated by wide terrace with depths lesser
than 2800–3000 m. We propose to name this terrace as the Bruce-Discovery Plateau. This Plateau
continues to the north till 58°S and to the north of it Bruce and Discovery Rises continues separated by
trough with depths 3000–3300 m. The both this Rises approach 56°S and rather close to the foot of the
South Georgia block of the North Scotia Ridge. It is logical to name the unity these features of the floor
in their full extremity as the Bruce-Discovery Province. The east limit of this Province lay
approximately on 35°W. The Bruce-Discovery Province can be considered as the eastern structural
margin of the Central Plate. Several volcanic seamounts, some of them are flat topped, have been
surveyed while expedition ANT-19/5 on the west linear margin of the Discovery Rise close to 36°W.
The depths of their flat tops are 1100 m (Drigalsky smt) and 1200 (Lazarev smt). These volcanos are
clearly positioned along large fractures directed to the South Georgia Island and supply the evidences
of the submersion of the Discovery Rise block with vertical dislocation along these fractures.
Between the Pirie-Gettingen and Bruce-Discovery Provinces lay two rather large basins –
above mentioned lens-like Schott Basin and to the south of it wide Dove Basin, named in the memory
thof outstanding German hydro-meteorologist of the 19 century. The sedimentary smoothed surface of
its floor at the west and east periphery lays on depths about 3300–3800 ì. In the axial part –
approximately on 42°30' W it is depressed up to depths 4100–4200 ì. The morphostructure of the
middle part of the basins floor reflects small local dislocations. Approximately on an axis of the Dove
basin at the longitude about 42°37'W lays the small narrow Guevara ridge of an asymmetric contours
and asymmetric profile with depth above a crest 1670 m and abrupt eastern and gradual western
slopes. The width of it in the basis of slopes is about 6 miles. It extents along lineation on azimuth 360°
approximately 30 miles. To northeast from this ridge lay another ridge of asymmetric profile. Its crest
focused on an azimuth 45° and extent only 15 miles. The depths at its crest are about 3413 m. The
uplifted origin of this ridge is clearly shown on the seismic profile. The inclined fault planes of vertical
dislocation are accompanied with compressonal folding of sedimentary layer to the east of this fault.
Certain similarity of these two small ridges testifies their faulted origin which corresponds to
compressive type dislocations of the brittle basement of the basin. The eastern-faulted slopes of the
both ridges are straight-lined. These local structures have no similarity to typical structures of the
oceanic rifts and it is unlikely to be considered as the evidences of the oceanic crust of the basin The
seismic profile at the middle of the Scotia sea along 59°S demonstrates complex block structure of the
brittle basement, and have no records of any rifts responsible for development of the Ona, Protector
and Dove basins..
We suppose the both described large morphostructural Provinces together with Basins can be
considered as characteristics for homogenous unit Province of the whole Central Plate of the Scotia
Sea.
Schenke H.W.: THE CENTRAL SCOTIA SEA FLOOR – IS IT AN PALEO-OCEANIC PLATE...
61
Geology
Samples dredged on the western escarp of the Pirie Bank by N.A.Kurentsova are represented
by fragments of the rocks from ancient pre-Cambrian craton. There are gneisses, mica-slates of the
upper pre-Cambrian (absolute age 579 Ma), granites of the lower Jurassic (183 Ma), rhyolites,
liparites and basalts of the middle Jurassic (169–175 Ma) to aleurolites and sandstones of the
Cretaceous (113 ma) Their systematic set and breaking off forms lead us to presume local origin
more probable than ice rafting [Kurentsova, Udintsev, 2004].
Samples of stone breeds were reported for the Discovery Bank by Eagles (Livermore et al.,
2005) and were obtained there by us with trawling. These rocks appeared be similar to samples from
the outcrops of the slope of the Pirie Bank [Udintsev, Arntz et al., 2003].
The column of sediments obtained by corer at the Bruce Bank according to micro
paleontological data demonstrates the evidences of high position of the Bank in the middle Eocene
time. It contains relicts of Cretaceous fauna which confirms the continental nature of the Bruce Rise
[Eagles, Livermore et al., 2005; Mao et al.,1995; Toker et al., 1991].
The geological section submitted on the Pirie Bank is close very much to the section
demonstrated at hole drilled at DSDP sites 327, 329 and 330 of 36-th leg of d/v «Glomar Challenger»
and by core sampling by r/v «Robert Conrad» on the Maurice Ewing Bank, as well as the holes 698,
699 and 700 of 114 leg of d/v «Joides Resolution» on the North-East Georgia Rise at the east extremity
of the Falkland Plateau. Characterized by these holes and cores the geological section passes through
a layer of sea deposits from recent to Miocene-Paleocene and Cretaceous-Jurassic deposits,
overlaying the pre-Cambrian basement [Ludwig, 1983, Wise et al., 1982; Ciesielski et al.,1991]. The
sets of rocks obtained on Bruce and Discovery Banks well supplement that similarity.
Gravity
Structure of the anomalous gravity field on the Central Plate of the Scotia Sea based on the
satellite altimetry [Sandwell D.T., Smith, 1997] and onboard survey by «Polarstern», was
topographically corrected by V.G.Udintsev into Bouger reduction. The similarity of the gravity field
values are observed above the rises of the Pirie and Bruce-Discovery Provinces and above neighbor
cratonic platforms at north and south of the Scotia Sea.
Magnetic anomalies and origin of the Protector, Dove and Polarstern Basins.
The structure of an anomalous magnetic field is shown on map «Tectonic of the Scotia Arc»
[Tectonic map, 1985] and have been discussed for estimation of the age of the Central Plate [Barker,
1990, Barker, Dalziel, Storey, 1991, Eagles, Livermore, Fairhead, Morris, 2005]. A number of
anomalies of W-E lineation locate in the Schott Basin and partly in the area south of it in the Dove
Basin. These anomalies were identified according the age scale accepted by the authors as 5,5 ñ and 6,
that corresponds to the ages of 10 Ma, 17 Ma and 20 Ma. The axial anomaly of the assumed rift should
be laid probably along the axis of the Schott and Dove Basins. It was assumed by Barker and other
authors that these linear magnetic anomalies correspond to the history of spreading along the local rift.
It was accompanied with creation of the basins of the Central Plate and movements to the north the
large continental fragment. That fragment of former continental bridge being displaced to the north
and represent now by the South Georgia Island in the east end of the North Scotia Ridge. Similar
supposition was made about the rift along the axes of Protector Basin [Eagles, Livermore, Fairthead,
Morris, 2005, Eagles, Livermore, Morris, 2006]. However we not recognize in the topography of the
floor and in the structure of the basement of these basins any evidences of typical structure of the rifts.
We suppose the origin of the observed magnetic anomalies by diapirism of serpentinizied ultrabasic
rocks at the large plume of the upper mantle into large fissures of extension in the deep part of the
crustal basement. Identification of the Geological age of these anomalies seems to us rather equivocal.
Schenke H.W.: THE CENTRAL SCOTIA SEA FLOOR – IS IT AN PALEO-OCEANIC PLATE...
62
The origin of these basins can be considered as corresponding to the extension and block dislocations
of the brittle cratonic basement. Some parts of this basement experienced more deep submission
relative to rises. Other reason to submission of the floor of these basins can be supposed as obliged to
heating by upper mantle plums accompanied with out pouring the basalt flows and eclogitization of
the crustal roots.The origin of the Schott Basin can be assumed also as related with impact of a large
asteroid.
Geokinematics
Geodynamics of the structures inside of the Central Plate of Scotia Sea is revealed by results of
geokinematic monitoring based on observations made at the net of basic geodetic stations installed on
the Antarctic Peninsula, several Antarctic islands, South America, Gough Island, South Atlantic
Ridge, and at South Africa [Dietrich R., 2000]. The comparison of the established vectors of
horizontal displacement testifies to backlog of movement of the Antarctic Peninsula and Antarctic
islands from delayed in this movement from continents of Southern America and Africa
approximately on 5 mm/year. As the bodies of continents have very deep roots, their movements in
time have to be the inertial steady, and the observed nowadays displacements could be extrapolated
through the geological past. Probable result of extension of the crust between Patagonia and West
Antarctica through the period of 20-30 ma would be expressed in the series of fractures like Falkland
Trough, Shag, South Orkney Trenches and located inside the trough of the Polarstern Graben.
3. Interpretation
Figure. Morphostructure of the Central Part of Scotia Sea basin. The hypothetic relict of intercontinental
bridge between South America and West Antarctica (paleo-Land Scotia) is marked.
Schenke H.W.: THE CENTRAL SCOTIA SEA FLOOR – IS IT AN PALEO-OCEANIC PLATE...
63
Doing synthesis of data obtained we approach to hypothesis about Central Plate of the Scotia
Sea as the huge fragment of extra-Andean Patagonia (see figure). This fragment was separated from
both neighbor cratons in process of the long term regional extension, registered by geokinematic
monitoring, and submerged to the level of depth similar to the Maurice Ewing Bank and the Northeast
Georgia Rise. The reason for such hypothesis are data on morphology of the floor; on features of the
brittleness of its basement, similar to easternmost part of the Falkland Plateau and South Orkney
micro-continent; on identity of geology of the basement; using extrapolation of geological
information from the southern parts of the rises of the Central Plate to its northern parts, based on
similarity of the gravity field over the whole Central Plate and above neighbor extra-Andean cratons
of Patagonia and West Antarctica. The existence of numerously observed planar surfaces are the
unequivocal evidences of the submergence of that supposed cratonic fragment, which we would like
name as the Scotia paleo-Land.
Literature
Barker P.F. International.Geol.-Geophys. Atlas of the Atlantic Ocean M., 1990, p. 58–61.
Barker P.F., Dalziel I.W.D., Storey B.C. The Geology of Antarctica, Oxford, Clarendon
Press, 1991, P. 215–248.
Barker P.F., Thomas E. Earth-Science Reviews 66 (2004). 143–162.
Barker P., Thomas E. Potential of the Scotia Sea Region for Determining the Onset and
Development of the Antarctic Circumpolar Current //in: Futterer D.K. et al.,(eds) Antarctica,
Springer-Verlag, 2006, pp. 433–440.
Bohoyo F., Galindo-Zaldivar J., Hernandez-Molina F.J., Jabaloy A., Lobo F.J., Maldonado
A., Rodriguez-Fernandez J., Somoza L., Surinach E., Vazquez J.T. Oceanic gateways in between
Weddell and Scotia seas: tectonic development and global influence //Geophys. Res. Abstracts, 2006,
v. 8, 09372.
Bohoyo F. et al. Development of deep extensional basins associated with sinistral transcurrent
fault zone of the Scotia-Antarctic plate boundary // U.S.Geol.Survey a.The Nartional Academies,
USGS OF-2007-1047, Ext. Abstract 042, p.1–4.
Cieselski P.F. et al. Proceedings of the Ocean Drilling Program, Initial Reportss, vol. 144,
1988.
Cieselski P.F. et al. Proceedings of the Ocean Drilling Program, Scientific Results, vol. 114,
1991.
Ciesielski P.F. et al. Preliminary results of subantarctic South Atlantic Leg114 of the Ocean
Drilling Program (ODP) // Geol. Evol. Ant., p. 645–650, 1991.
Dalziel I.W.D., Elliot D.H. The Scotia Arc and Antarctic margin. In Nairn A.E.M., Stehl D.H.,
eds. The Ocean Basins and Margins, 1, the South Atlantic,1973, pp.171–245, Plenum Press, N.Y.
De Wit M.J. The evolution of the Scotia Arc as a key to the reconstruction of southwestern
Gonwanaland // Tectonophysics, 1997, 37, p. 53–81.
Dietrich R., Dach R., Engelhardt G. et al. Deutsche Geodatische Kommission bei der
Bayerischen Akademie der Wissenschaften, Munshen, 2000, Angewandte Geodasie, Rehhe B, Heft
Nr.310, pp. 11–20.
Eagles G. et al. Small basins in the Scotia Sea: The Eocene Drake Passage gateway // Jour.
Geophys. Res. V. 110, BO2401, 2005.
Eagles G. et al. Tectonic evolution of the west Scotia Sea // Jour. Geophys. Res. v.110, BO
2401, 2005.
Eagles G., Livermore R., Morris P. Small basins in the Scotia Sea: The Eocen Drake Passage
gateway // Earth and Planetary Science Letters, 2006, v. 242, p. 343–353.
Schenke H.W.: THE CENTRAL SCOTIA SEA FLOOR – IS IT AN PALEO-OCEANIC PLATE...
64
Ewing J.I., LudwigW.J., Ewing M., Eittreim S.L. Structure of the Scotia Sea and Falkland
Plateau //Jour.Geophys.Res, 1971, 7118–7137.
Galimov E.Ì., Udintsev G.B., Schenke H.-W., Schoene Ò. Herald of Russian Academy of
Sciences, 1999, v. 69, no 2, p. 111–119 (in russian).
Galindo-Zaldivar J., Jabaloy A., Maldonado A., Sanz de Galdeano C.S. Continental
fragmentation along the South Scotia Ridge transcurrent plate boundary // Tectonophysics, 1996, v.
258, pp. 275–301.
Galindo-Zaldivar J., Balanja J.C., Bohoyo F., Jabaloy A., Maldonado A., Martinez-
Martinez J.M., Rodriguez-Fernandez J., Surinach E. Crustal Thinning and the Development of Deep
Depressions at the Scotia-Antarctic Plate Boundary (Southern Margin of Discovery Bank, Antarctica)
// Futterer D.K., Damaske D., Kleinscmidt G., Miller H., Tessensohn F. Antarctica, Contribution to
Global Earth Sciences. Springer, 2006.
Galindo-Zaldivar J., Bohoyo F., Maldonado A., Schreider A., Vazquez J.T. Propagaiting rift
during the opening of a small oceanic basin: The Protector Basin (Scotia Arc, Antarctica) // Earth
a.Planet.Scie.Lett., 2006, 241, p. 398–412.
Gracia E., Canals M., Li Farran M. et al. Morphostructure and Evolution of the Central and
Eastern Bransfield Basins (NW Antarctic Peninsula) //Marine Geophysical Researches, 1996, v. 18,
p. 429–448.
GEBCO // IHO/IOC/CHS, 1984, 2003.
Hernandez-Molina F.J., Bohoyo F., Naveira Garabato A., Galindo-Zaldivar J., Lobo F.J.,
Maldonado A., Rodriguez-Fernandez J., Somoza L., Stow D.A.V., Vazquez J.T. The Sea basin
evolution: Oceanographic consequences of the deep connection between the Weddell and Scotia Seas
(Antarctica) // U.S.Geol. Surv. a.Nation.Academies, USGS of-2007 – 1047, ext.abs.086.
Herve F., Miller H., Pimpirev C. Patagonia – Antarctica Connections before Gondwana
Break-Up //in Futterer D.K., Damaske D., Kleinscmidt G., Tessensohn E. (eds.), Antarctica, 2006,
pp. 217–238.
Kavun Ì.Ì., Vinnikovskaya Î.S. Bulletin ÌÎIP, geol. depart., 1993, vol.6, iss. 6, p. 83–96
(in russian).
King E.C., Barker R.F. The tectonic history of the South Orkney microcontinental block //
Jour.Geol.Soc.London, 1988, 145, 317–331.
King E.C., Leitchenkov G., Galindo-Zaldivar J., Maldonado A., Lodolo E. Geology and
Seismic stratigraphy of the Antarctic Margin, p. 2 // Antarctic Research Series, vol. 71, 1997, pp.
75–93.
Kristoffersen Y., LaBrecque J. On the tectonic history and origin of the Northeast Georgia
Rise // Ciesielski P.F., Kristoffersen Y. et al. Proceed.Ocean Drill.Prog., Scie.Res., 1991, v.114, p.
23–38.
Kurentsova N.A., Udintsev G.B. The main features of the structure and evolution of the
sourthern part of the Scotia Sea, West Antarctic. – The Geology of Pasific Ocean. 2004, ò. 23,
¹ 5, p. 25–39 (in Russian).
Lawver L.A., Sloan B.J., Barker D.H. et al. Distributed Active Extension in Bransfield
Basin, Antarctic Peninsula: Evidence from Multibeam Bathymetry // Geol.Soc.Amer.Bull., 1996, v. 6,
No 11, p. 1–6.
Livermore R.A., McAdoo D., Marks K. // Earth Planet. Sci. Lett., 1994.
Livermore R.A., Hunter R.J. // King B.C., Livermore R.A. (eds). 1996, Weddell Sea
Tectonics and Gondwana Break-up, Geol. Soc. Spec. Publ. No. 108, pp. 227–241.
Livermore R.A. et al. // Earth. Planet. Sci. Lett. 1997, V. 150. P. 262–275.
Livermore R.A., Eagles G., Morris P., Maldonado A. // Geology, 2004, v. 32, no. 9,
p. 797–800.
Schenke H.W.: THE CENTRAL SCOTIA SEA FLOOR – IS IT AN PALEO-OCEANIC PLATE...
65
Lorenzo J.M., Mutter J.C. Seismic stratigraphy and tectonic evolution of the
Malvinas/Falkland Plateau //Revista Brasiliera de Geociencias, 1988, 18, 191–200.
Ludwig W.J. Geologic framework of the Falkland Plateau // Inint.Rep.DSDP, 71, Washington,
US Govt.Printing Office, 1983, 71, 281–292.
Ludwig W.J., Windisch C.C., Houtz R.E., Ewing J.I. Structure of Faalkland Plateau and
offshore Tierra del Fuego, Argentina., in Geological and geophysical investigations of continental
pargins // Am.Assoc. Petrol.Geol., 1978, memoir 29, Tulsa.
Ludwig W.J., Rabiniwitz P.D. Seismic stratigraphy and structure of Falkland Plateau //
Am.Assoc.Petrol.Geol.Bull., 1982, 64, 742.
Maldonado A. et al. Ocean basins near the Scotia-Antarctic plate boundary : Influence of
tectonics and paleoceanography on the Cenozoic deposits // Mar.Geophys.Res., 2006, v.27, pp. 83–107.
Maldonado A. et al. Seismic Stratigraphy of Miocene to Recent Sedimentary Deposits in the
Central Scotia Sea and Northern Weddell Sea : Influence of Bottom Flows (Antarctica) // in: Futterer D.K.
et al.,(eds) Antarctica, Springer-Verlag, 2006, pp. 441–446.
Maldonado A. et al. Contourite deposits in the central Scotia Sea: the importance of the
Antarctic Circumpolar Current and the Weddell Gyre flows // Palaegeogr.,Palaeoclim., Palaeoecol.,
2003, 198, p. 187–221.
Maldonado A. et al. Tectonics of an extinct ridge-transform intersection, Drake Passage
(Antarctica) // Mar.Geophys.Res. 2000, 21, pp. 43–68.
Mao S., Mohr B.A.R. Middle Eocene dinocysts from Bruce Bank (Scotia Sea, Antarctica) and
their paleoenvironmental and paleogeographic implications // 1994, Review of Palaeobotany and
Palynology.
Mao et al. Rev. Paleobot. Palykol. // 1995, 86, 235–263.
Olbers D., Borowski D., Volker C., Wolff J-O. // Antarctic Science 16 (4): 439–470 (2004).
Pearce J.A., Leat P.T., Barker P.F., Miller I.L. Geochemical tracing of Pacific-to-Atlantic
upper-mantle flow through the Drake passage // Nature, 2001, v. 410/22, p. 457–461.
Sandwell D.T., Smith W.H.F. // Science, 1997, V. 277, N 5334. P. 1956–1962.
Schenke H.W., Zenk W., editors. The Expeditions ANTATKTIS-XXII/4 and 5 of the Research
Vessel «Polarstern» in 2005 //Reports on Polar and Marine Research, 2006, Heft-Nr. 537.
Smith W.H.F., Sandwell D.T. // Science, 1997, V. 277, N 5334, P. 1956–1962.
Suess E. // Das Anblitz der Erde. Bd. 1-111, Leipzig, Wienn, 1883–1909.
Tectonic map of the Scotia Arc // Sheet BAS (Misc) 3 Ed.1, 1985. Scale 1:
3 000 000, British Antarctic Survey, Cambridge, 1985.
Toker V. at al. Middle Eocene carbonate-bearing marine sediments from the Bruce Bank off
northern Antarctic Peninsula // Geol. Evol. Antarctic, 1991, p. 639–644.
Udintsev G.B., Arntz W, Udintsev V.G. et al. //Dokl.Earth Scences, 2003, vol. 388, ¹ 3,
p. 121.
Udintsev G.B., Schenke H.-W. // Ì., GEOS,, 2004, p.132 (in russian)
Udintsev G.B., Schenke H.-W., Beyer A. et al. // Dokl.Earth Sciences, 2006, v.408, ¹ 1,
p. 575.
Vuan A., Lodolo E., Panza G.F., Sault C. Crustal structure beneath Discovery Bank in the
Scotia Sea from group velocity // Antarctic Science, 2005, 17, 97-106, Cambridge Univ. Press.
Vuan A. et al. Group Velocity Tomography in the Subantarctic Scotia Sea Region // Pure
a.Applied Geophys., 157, p. 1337–1357.
Vuan A. et al. Crustal and upper mantle S-wave velocity structure beneath the Bransfield
Strait (West Antarctica) from regional surface wave tomography // Tectonophysics, 2005, 397,
p. 241–259.
Wise C.W., Ciesielski P.F., MacKenzie D.T. et al. // Antarctic Geoscience, Intern. Union
Geol. Sci. Ser. B-N 4, 1982, Madison, Wisconsin, p. 157.
Schenke H.W.: THE CENTRAL SCOTIA SEA FLOOR – IS IT AN PALEO-OCEANIC PLATE...
66
Page 1
Page 2
Page 3
Page 4
Page 5
Page 6
Page 7
Page 8
Page 9
Page 10
|