Centuries of intense surface melt on Larsen C Ice Shelf

Following a southward progression of ice-shelf disintegration along the Antarctic Peninsula (AP), Larsen C Ice Shelf (LCIS) has become the focus of ongoing investigation regarding its future stability. The ice shelf experiences surface melt and commonly features surface meltwater ponds. Here, we use...
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Autor*in:	S. L. Bevan [verfasserIn] A. Luckman [verfasserIn] B. Hubbard [verfasserIn] B. Kulessa [verfasserIn] D. Ashmore [verfasserIn] P. Kuipers Munneke [verfasserIn] M. O'Leary [verfasserIn] A. Booth [verfasserIn] H. Sevestre [verfasserIn] D. McGrath [verfasserIn]

Format:	E-Artikel
Sprache:	Englisch

Erschienen:	2017

Übergeordnetes Werk:	In: The Cryosphere - Copernicus Publications, 2007, 11(2017), Seite 2743-2753
Übergeordnetes Werk:	volume:11 ; year:2017 ; pages:2743-2753

Links:	Link aufrufen Link aufrufen Link aufrufen Journal toc Journal toc

DOI / URN:	10.5194/tc-11-2743-2017

Katalog-ID:	DOAJ07371223X

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spelling	10.5194/tc-11-2743-2017 doi (DE-627)DOAJ07371223X (DE-599)DOAJbc411c8768f1475bb9376698c2373f7e DE-627 ger DE-627 rakwb eng GE1-350 QE1-996.5 S. L. Bevan verfasserin aut Centuries of intense surface melt on Larsen C Ice Shelf 2017 Text txt rdacontent Computermedien c rdamedia Online-Ressource cr rdacarrier Following a southward progression of ice-shelf disintegration along the Antarctic Peninsula (AP), Larsen C Ice Shelf (LCIS) has become the focus of ongoing investigation regarding its future stability. The ice shelf experiences surface melt and commonly features surface meltwater ponds. Here, we use a flow-line model and a firn density model (FDM) to date and interpret observations of melt-affected ice layers found within five 90 m boreholes distributed across the ice shelf. We find that units of ice within the boreholes, which have densities exceeding those expected under normal dry compaction metamorphism, correspond to two climatic warm periods within the last 300 years on the Antarctic Peninsula. The more recent warm period, from the 1960s onwards, has generated distinct sections of dense ice measured in two boreholes in Cabinet Inlet, which is close to the Antarctic Peninsula mountains – a region affected by föhn winds. Previous work has classified these layers as refrozen pond ice, requiring large quantities of mobile liquid water to form. Our flow-line model shows that, whilst preconditioning of the snow began in the late 1960s, it was probably not until the early 1990s that the modern period of ponding began. The earlier warm period occurred during the 18th century and resulted in two additional sections of anomalously dense ice deep within the boreholes. The first, at 61 m in one of our Cabinet Inlet boreholes, consists of ice characteristic of refrozen ponds and must have formed in an area currently featuring ponding. The second, at 69 m in a mid-shelf borehole, formed at the same time on the edge of the pond area. Further south, the boreholes sample ice that is of an equivalent age but which does not exhibit the same degree of melt influence. This west–east and north–south gradient in the past melt distribution resembles current spatial patterns of surface melt intensity. Environmental sciences Geology A. Luckman verfasserin aut B. Hubbard verfasserin aut B. Kulessa verfasserin aut D. Ashmore verfasserin aut P. Kuipers Munneke verfasserin aut M. O'Leary verfasserin aut A. Booth verfasserin aut H. Sevestre verfasserin aut D. McGrath verfasserin aut In The Cryosphere Copernicus Publications, 2007 11(2017), Seite 2743-2753 (DE-627)548126011 (DE-600)2393169-3 19940424 nnns volume:11 year:2017 pages:2743-2753 https://doi.org/10.5194/tc-11-2743-2017 kostenfrei https://doaj.org/article/bc411c8768f1475bb9376698c2373f7e kostenfrei https://www.the-cryosphere.net/11/2743/2017/tc-11-2743-2017.pdf kostenfrei https://doaj.org/toc/1994-0416 Journal toc kostenfrei https://doaj.org/toc/1994-0424 Journal toc kostenfrei GBV_USEFLAG_A SYSFLAG_A GBV_DOAJ GBV_ILN_11 GBV_ILN_20 GBV_ILN_22 GBV_ILN_23 GBV_ILN_24 GBV_ILN_31 GBV_ILN_39 GBV_ILN_40 GBV_ILN_60 GBV_ILN_62 GBV_ILN_63 GBV_ILN_65 GBV_ILN_69 GBV_ILN_70 GBV_ILN_73 GBV_ILN_95 GBV_ILN_105 GBV_ILN_110 GBV_ILN_151 GBV_ILN_161 GBV_ILN_170 GBV_ILN_206 GBV_ILN_213 GBV_ILN_230 GBV_ILN_267 GBV_ILN_285 GBV_ILN_293 GBV_ILN_370 GBV_ILN_602 GBV_ILN_2003 GBV_ILN_2005 GBV_ILN_2009 GBV_ILN_2011 GBV_ILN_2014 GBV_ILN_2055 GBV_ILN_2111 GBV_ILN_4012 GBV_ILN_4037 GBV_ILN_4112 GBV_ILN_4125 GBV_ILN_4126 GBV_ILN_4249 GBV_ILN_4305 GBV_ILN_4306 GBV_ILN_4307 GBV_ILN_4313 GBV_ILN_4322 GBV_ILN_4323 GBV_ILN_4324 GBV_ILN_4325 GBV_ILN_4335 GBV_ILN_4338 GBV_ILN_4367 GBV_ILN_4700 AR 11 2017 2743-2753
allfields_unstemmed	10.5194/tc-11-2743-2017 doi (DE-627)DOAJ07371223X (DE-599)DOAJbc411c8768f1475bb9376698c2373f7e DE-627 ger DE-627 rakwb eng GE1-350 QE1-996.5 S. L. Bevan verfasserin aut Centuries of intense surface melt on Larsen C Ice Shelf 2017 Text txt rdacontent Computermedien c rdamedia Online-Ressource cr rdacarrier Following a southward progression of ice-shelf disintegration along the Antarctic Peninsula (AP), Larsen C Ice Shelf (LCIS) has become the focus of ongoing investigation regarding its future stability. The ice shelf experiences surface melt and commonly features surface meltwater ponds. Here, we use a flow-line model and a firn density model (FDM) to date and interpret observations of melt-affected ice layers found within five 90 m boreholes distributed across the ice shelf. We find that units of ice within the boreholes, which have densities exceeding those expected under normal dry compaction metamorphism, correspond to two climatic warm periods within the last 300 years on the Antarctic Peninsula. The more recent warm period, from the 1960s onwards, has generated distinct sections of dense ice measured in two boreholes in Cabinet Inlet, which is close to the Antarctic Peninsula mountains – a region affected by föhn winds. Previous work has classified these layers as refrozen pond ice, requiring large quantities of mobile liquid water to form. Our flow-line model shows that, whilst preconditioning of the snow began in the late 1960s, it was probably not until the early 1990s that the modern period of ponding began. The earlier warm period occurred during the 18th century and resulted in two additional sections of anomalously dense ice deep within the boreholes. The first, at 61 m in one of our Cabinet Inlet boreholes, consists of ice characteristic of refrozen ponds and must have formed in an area currently featuring ponding. The second, at 69 m in a mid-shelf borehole, formed at the same time on the edge of the pond area. Further south, the boreholes sample ice that is of an equivalent age but which does not exhibit the same degree of melt influence. This west–east and north–south gradient in the past melt distribution resembles current spatial patterns of surface melt intensity. Environmental sciences Geology A. Luckman verfasserin aut B. Hubbard verfasserin aut B. Kulessa verfasserin aut D. Ashmore verfasserin aut P. Kuipers Munneke verfasserin aut M. O'Leary verfasserin aut A. Booth verfasserin aut H. Sevestre verfasserin aut D. McGrath verfasserin aut In The Cryosphere Copernicus Publications, 2007 11(2017), Seite 2743-2753 (DE-627)548126011 (DE-600)2393169-3 19940424 nnns volume:11 year:2017 pages:2743-2753 https://doi.org/10.5194/tc-11-2743-2017 kostenfrei https://doaj.org/article/bc411c8768f1475bb9376698c2373f7e kostenfrei https://www.the-cryosphere.net/11/2743/2017/tc-11-2743-2017.pdf kostenfrei https://doaj.org/toc/1994-0416 Journal toc kostenfrei https://doaj.org/toc/1994-0424 Journal toc kostenfrei GBV_USEFLAG_A SYSFLAG_A GBV_DOAJ GBV_ILN_11 GBV_ILN_20 GBV_ILN_22 GBV_ILN_23 GBV_ILN_24 GBV_ILN_31 GBV_ILN_39 GBV_ILN_40 GBV_ILN_60 GBV_ILN_62 GBV_ILN_63 GBV_ILN_65 GBV_ILN_69 GBV_ILN_70 GBV_ILN_73 GBV_ILN_95 GBV_ILN_105 GBV_ILN_110 GBV_ILN_151 GBV_ILN_161 GBV_ILN_170 GBV_ILN_206 GBV_ILN_213 GBV_ILN_230 GBV_ILN_267 GBV_ILN_285 GBV_ILN_293 GBV_ILN_370 GBV_ILN_602 GBV_ILN_2003 GBV_ILN_2005 GBV_ILN_2009 GBV_ILN_2011 GBV_ILN_2014 GBV_ILN_2055 GBV_ILN_2111 GBV_ILN_4012 GBV_ILN_4037 GBV_ILN_4112 GBV_ILN_4125 GBV_ILN_4126 GBV_ILN_4249 GBV_ILN_4305 GBV_ILN_4306 GBV_ILN_4307 GBV_ILN_4313 GBV_ILN_4322 GBV_ILN_4323 GBV_ILN_4324 GBV_ILN_4325 GBV_ILN_4335 GBV_ILN_4338 GBV_ILN_4367 GBV_ILN_4700 AR 11 2017 2743-2753
allfieldsGer	10.5194/tc-11-2743-2017 doi (DE-627)DOAJ07371223X (DE-599)DOAJbc411c8768f1475bb9376698c2373f7e DE-627 ger DE-627 rakwb eng GE1-350 QE1-996.5 S. L. Bevan verfasserin aut Centuries of intense surface melt on Larsen C Ice Shelf 2017 Text txt rdacontent Computermedien c rdamedia Online-Ressource cr rdacarrier Following a southward progression of ice-shelf disintegration along the Antarctic Peninsula (AP), Larsen C Ice Shelf (LCIS) has become the focus of ongoing investigation regarding its future stability. The ice shelf experiences surface melt and commonly features surface meltwater ponds. Here, we use a flow-line model and a firn density model (FDM) to date and interpret observations of melt-affected ice layers found within five 90 m boreholes distributed across the ice shelf. We find that units of ice within the boreholes, which have densities exceeding those expected under normal dry compaction metamorphism, correspond to two climatic warm periods within the last 300 years on the Antarctic Peninsula. The more recent warm period, from the 1960s onwards, has generated distinct sections of dense ice measured in two boreholes in Cabinet Inlet, which is close to the Antarctic Peninsula mountains – a region affected by föhn winds. Previous work has classified these layers as refrozen pond ice, requiring large quantities of mobile liquid water to form. Our flow-line model shows that, whilst preconditioning of the snow began in the late 1960s, it was probably not until the early 1990s that the modern period of ponding began. The earlier warm period occurred during the 18th century and resulted in two additional sections of anomalously dense ice deep within the boreholes. The first, at 61 m in one of our Cabinet Inlet boreholes, consists of ice characteristic of refrozen ponds and must have formed in an area currently featuring ponding. The second, at 69 m in a mid-shelf borehole, formed at the same time on the edge of the pond area. Further south, the boreholes sample ice that is of an equivalent age but which does not exhibit the same degree of melt influence. This west–east and north–south gradient in the past melt distribution resembles current spatial patterns of surface melt intensity. Environmental sciences Geology A. Luckman verfasserin aut B. Hubbard verfasserin aut B. Kulessa verfasserin aut D. Ashmore verfasserin aut P. Kuipers Munneke verfasserin aut M. O'Leary verfasserin aut A. Booth verfasserin aut H. Sevestre verfasserin aut D. McGrath verfasserin aut In The Cryosphere Copernicus Publications, 2007 11(2017), Seite 2743-2753 (DE-627)548126011 (DE-600)2393169-3 19940424 nnns volume:11 year:2017 pages:2743-2753 https://doi.org/10.5194/tc-11-2743-2017 kostenfrei https://doaj.org/article/bc411c8768f1475bb9376698c2373f7e kostenfrei https://www.the-cryosphere.net/11/2743/2017/tc-11-2743-2017.pdf kostenfrei https://doaj.org/toc/1994-0416 Journal toc kostenfrei https://doaj.org/toc/1994-0424 Journal toc kostenfrei GBV_USEFLAG_A SYSFLAG_A GBV_DOAJ GBV_ILN_11 GBV_ILN_20 GBV_ILN_22 GBV_ILN_23 GBV_ILN_24 GBV_ILN_31 GBV_ILN_39 GBV_ILN_40 GBV_ILN_60 GBV_ILN_62 GBV_ILN_63 GBV_ILN_65 GBV_ILN_69 GBV_ILN_70 GBV_ILN_73 GBV_ILN_95 GBV_ILN_105 GBV_ILN_110 GBV_ILN_151 GBV_ILN_161 GBV_ILN_170 GBV_ILN_206 GBV_ILN_213 GBV_ILN_230 GBV_ILN_267 GBV_ILN_285 GBV_ILN_293 GBV_ILN_370 GBV_ILN_602 GBV_ILN_2003 GBV_ILN_2005 GBV_ILN_2009 GBV_ILN_2011 GBV_ILN_2014 GBV_ILN_2055 GBV_ILN_2111 GBV_ILN_4012 GBV_ILN_4037 GBV_ILN_4112 GBV_ILN_4125 GBV_ILN_4126 GBV_ILN_4249 GBV_ILN_4305 GBV_ILN_4306 GBV_ILN_4307 GBV_ILN_4313 GBV_ILN_4322 GBV_ILN_4323 GBV_ILN_4324 GBV_ILN_4325 GBV_ILN_4335 GBV_ILN_4338 GBV_ILN_4367 GBV_ILN_4700 AR 11 2017 2743-2753
allfieldsSound	10.5194/tc-11-2743-2017 doi (DE-627)DOAJ07371223X (DE-599)DOAJbc411c8768f1475bb9376698c2373f7e DE-627 ger DE-627 rakwb eng GE1-350 QE1-996.5 S. L. Bevan verfasserin aut Centuries of intense surface melt on Larsen C Ice Shelf 2017 Text txt rdacontent Computermedien c rdamedia Online-Ressource cr rdacarrier Following a southward progression of ice-shelf disintegration along the Antarctic Peninsula (AP), Larsen C Ice Shelf (LCIS) has become the focus of ongoing investigation regarding its future stability. The ice shelf experiences surface melt and commonly features surface meltwater ponds. Here, we use a flow-line model and a firn density model (FDM) to date and interpret observations of melt-affected ice layers found within five 90 m boreholes distributed across the ice shelf. We find that units of ice within the boreholes, which have densities exceeding those expected under normal dry compaction metamorphism, correspond to two climatic warm periods within the last 300 years on the Antarctic Peninsula. The more recent warm period, from the 1960s onwards, has generated distinct sections of dense ice measured in two boreholes in Cabinet Inlet, which is close to the Antarctic Peninsula mountains – a region affected by föhn winds. Previous work has classified these layers as refrozen pond ice, requiring large quantities of mobile liquid water to form. Our flow-line model shows that, whilst preconditioning of the snow began in the late 1960s, it was probably not until the early 1990s that the modern period of ponding began. The earlier warm period occurred during the 18th century and resulted in two additional sections of anomalously dense ice deep within the boreholes. The first, at 61 m in one of our Cabinet Inlet boreholes, consists of ice characteristic of refrozen ponds and must have formed in an area currently featuring ponding. The second, at 69 m in a mid-shelf borehole, formed at the same time on the edge of the pond area. Further south, the boreholes sample ice that is of an equivalent age but which does not exhibit the same degree of melt influence. This west–east and north–south gradient in the past melt distribution resembles current spatial patterns of surface melt intensity. Environmental sciences Geology A. Luckman verfasserin aut B. Hubbard verfasserin aut B. Kulessa verfasserin aut D. Ashmore verfasserin aut P. Kuipers Munneke verfasserin aut M. O'Leary verfasserin aut A. Booth verfasserin aut H. Sevestre verfasserin aut D. McGrath verfasserin aut In The Cryosphere Copernicus Publications, 2007 11(2017), Seite 2743-2753 (DE-627)548126011 (DE-600)2393169-3 19940424 nnns volume:11 year:2017 pages:2743-2753 https://doi.org/10.5194/tc-11-2743-2017 kostenfrei https://doaj.org/article/bc411c8768f1475bb9376698c2373f7e kostenfrei https://www.the-cryosphere.net/11/2743/2017/tc-11-2743-2017.pdf kostenfrei https://doaj.org/toc/1994-0416 Journal toc kostenfrei https://doaj.org/toc/1994-0424 Journal toc kostenfrei GBV_USEFLAG_A SYSFLAG_A GBV_DOAJ GBV_ILN_11 GBV_ILN_20 GBV_ILN_22 GBV_ILN_23 GBV_ILN_24 GBV_ILN_31 GBV_ILN_39 GBV_ILN_40 GBV_ILN_60 GBV_ILN_62 GBV_ILN_63 GBV_ILN_65 GBV_ILN_69 GBV_ILN_70 GBV_ILN_73 GBV_ILN_95 GBV_ILN_105 GBV_ILN_110 GBV_ILN_151 GBV_ILN_161 GBV_ILN_170 GBV_ILN_206 GBV_ILN_213 GBV_ILN_230 GBV_ILN_267 GBV_ILN_285 GBV_ILN_293 GBV_ILN_370 GBV_ILN_602 GBV_ILN_2003 GBV_ILN_2005 GBV_ILN_2009 GBV_ILN_2011 GBV_ILN_2014 GBV_ILN_2055 GBV_ILN_2111 GBV_ILN_4012 GBV_ILN_4037 GBV_ILN_4112 GBV_ILN_4125 GBV_ILN_4126 GBV_ILN_4249 GBV_ILN_4305 GBV_ILN_4306 GBV_ILN_4307 GBV_ILN_4313 GBV_ILN_4322 GBV_ILN_4323 GBV_ILN_4324 GBV_ILN_4325 GBV_ILN_4335 GBV_ILN_4338 GBV_ILN_4367 GBV_ILN_4700 AR 11 2017 2743-2753
language	English
source	In The Cryosphere 11(2017), Seite 2743-2753 volume:11 year:2017 pages:2743-2753
sourceStr	In The Cryosphere 11(2017), Seite 2743-2753 volume:11 year:2017 pages:2743-2753
format_phy_str_mv	Article
institution	findex.gbv.de
topic_facet	Environmental sciences Geology
isfreeaccess_bool	true
container_title	The Cryosphere
authorswithroles_txt_mv	S. L. Bevan @@aut@@ A. Luckman @@aut@@ B. Hubbard @@aut@@ B. Kulessa @@aut@@ D. Ashmore @@aut@@ P. Kuipers Munneke @@aut@@ M. O'Leary @@aut@@ A. Booth @@aut@@ H. Sevestre @@aut@@ D. McGrath @@aut@@
publishDateDaySort_date	2017-01-01T00:00:00Z
hierarchy_top_id	548126011
id	DOAJ07371223X
language_de	englisch
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callnumber-first	G - Geography, Anthropology, Recreation
author	S. L. Bevan
spellingShingle	S. L. Bevan misc GE1-350 misc QE1-996.5 misc Environmental sciences misc Geology Centuries of intense surface melt on Larsen C Ice Shelf
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topic_title	GE1-350 QE1-996.5 Centuries of intense surface melt on Larsen C Ice Shelf
topic	misc GE1-350 misc QE1-996.5 misc Environmental sciences misc Geology
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title	Centuries of intense surface melt on Larsen C Ice Shelf
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title_full	Centuries of intense surface melt on Larsen C Ice Shelf
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author_browse	S. L. Bevan A. Luckman B. Hubbard B. Kulessa D. Ashmore P. Kuipers Munneke M. O'Leary A. Booth H. Sevestre D. McGrath
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title_sort	centuries of intense surface melt on larsen c ice shelf
callnumber	GE1-350
title_auth	Centuries of intense surface melt on Larsen C Ice Shelf
abstract	Following a southward progression of ice-shelf disintegration along the Antarctic Peninsula (AP), Larsen C Ice Shelf (LCIS) has become the focus of ongoing investigation regarding its future stability. The ice shelf experiences surface melt and commonly features surface meltwater ponds. Here, we use a flow-line model and a firn density model (FDM) to date and interpret observations of melt-affected ice layers found within five 90 m boreholes distributed across the ice shelf. We find that units of ice within the boreholes, which have densities exceeding those expected under normal dry compaction metamorphism, correspond to two climatic warm periods within the last 300 years on the Antarctic Peninsula. The more recent warm period, from the 1960s onwards, has generated distinct sections of dense ice measured in two boreholes in Cabinet Inlet, which is close to the Antarctic Peninsula mountains – a region affected by föhn winds. Previous work has classified these layers as refrozen pond ice, requiring large quantities of mobile liquid water to form. Our flow-line model shows that, whilst preconditioning of the snow began in the late 1960s, it was probably not until the early 1990s that the modern period of ponding began. The earlier warm period occurred during the 18th century and resulted in two additional sections of anomalously dense ice deep within the boreholes. The first, at 61 m in one of our Cabinet Inlet boreholes, consists of ice characteristic of refrozen ponds and must have formed in an area currently featuring ponding. The second, at 69 m in a mid-shelf borehole, formed at the same time on the edge of the pond area. Further south, the boreholes sample ice that is of an equivalent age but which does not exhibit the same degree of melt influence. This west–east and north–south gradient in the past melt distribution resembles current spatial patterns of surface melt intensity.
abstractGer	Following a southward progression of ice-shelf disintegration along the Antarctic Peninsula (AP), Larsen C Ice Shelf (LCIS) has become the focus of ongoing investigation regarding its future stability. The ice shelf experiences surface melt and commonly features surface meltwater ponds. Here, we use a flow-line model and a firn density model (FDM) to date and interpret observations of melt-affected ice layers found within five 90 m boreholes distributed across the ice shelf. We find that units of ice within the boreholes, which have densities exceeding those expected under normal dry compaction metamorphism, correspond to two climatic warm periods within the last 300 years on the Antarctic Peninsula. The more recent warm period, from the 1960s onwards, has generated distinct sections of dense ice measured in two boreholes in Cabinet Inlet, which is close to the Antarctic Peninsula mountains – a region affected by föhn winds. Previous work has classified these layers as refrozen pond ice, requiring large quantities of mobile liquid water to form. Our flow-line model shows that, whilst preconditioning of the snow began in the late 1960s, it was probably not until the early 1990s that the modern period of ponding began. The earlier warm period occurred during the 18th century and resulted in two additional sections of anomalously dense ice deep within the boreholes. The first, at 61 m in one of our Cabinet Inlet boreholes, consists of ice characteristic of refrozen ponds and must have formed in an area currently featuring ponding. The second, at 69 m in a mid-shelf borehole, formed at the same time on the edge of the pond area. Further south, the boreholes sample ice that is of an equivalent age but which does not exhibit the same degree of melt influence. This west–east and north–south gradient in the past melt distribution resembles current spatial patterns of surface melt intensity.
abstract_unstemmed	Following a southward progression of ice-shelf disintegration along the Antarctic Peninsula (AP), Larsen C Ice Shelf (LCIS) has become the focus of ongoing investigation regarding its future stability. The ice shelf experiences surface melt and commonly features surface meltwater ponds. Here, we use a flow-line model and a firn density model (FDM) to date and interpret observations of melt-affected ice layers found within five 90 m boreholes distributed across the ice shelf. We find that units of ice within the boreholes, which have densities exceeding those expected under normal dry compaction metamorphism, correspond to two climatic warm periods within the last 300 years on the Antarctic Peninsula. The more recent warm period, from the 1960s onwards, has generated distinct sections of dense ice measured in two boreholes in Cabinet Inlet, which is close to the Antarctic Peninsula mountains – a region affected by föhn winds. Previous work has classified these layers as refrozen pond ice, requiring large quantities of mobile liquid water to form. Our flow-line model shows that, whilst preconditioning of the snow began in the late 1960s, it was probably not until the early 1990s that the modern period of ponding began. The earlier warm period occurred during the 18th century and resulted in two additional sections of anomalously dense ice deep within the boreholes. The first, at 61 m in one of our Cabinet Inlet boreholes, consists of ice characteristic of refrozen ponds and must have formed in an area currently featuring ponding. The second, at 69 m in a mid-shelf borehole, formed at the same time on the edge of the pond area. Further south, the boreholes sample ice that is of an equivalent age but which does not exhibit the same degree of melt influence. This west–east and north–south gradient in the past melt distribution resembles current spatial patterns of surface melt intensity.
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title_short	Centuries of intense surface melt on Larsen C Ice Shelf
url	https://doi.org/10.5194/tc-11-2743-2017 https://doaj.org/article/bc411c8768f1475bb9376698c2373f7e https://www.the-cryosphere.net/11/2743/2017/tc-11-2743-2017.pdf https://doaj.org/toc/1994-0416 https://doaj.org/toc/1994-0424
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Centuries of intense surface melt on Larsen C Ice Shelf

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Vorhandene Bände

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