Climatic variability of the sub-surface sea temperatures in the Aegean-Black Sea system and relation to meteorological forcing

Abstract Non-smoothed yearly temperature records with minimal statistical uncertainties are constructed for winter and summer of the period 1950–2000 in two areas in the Aegean Sea, for the sub-surface layer of 80–120 m, and two areas in the Black Sea, for the sub-surface layer of sigma-theta isopyc...
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Autor*in:	Kontoyiannis, H. [verfasserIn] Papadopoulos, V. [verfasserIn] Kazmin, A. [verfasserIn] Zatsepin, A. [verfasserIn] Georgopoulos, D. [verfasserIn]

Format:	E-Artikel
Sprache:	Englisch

Erschienen:	2012

Schlagwörter:	Aegean-Black Sea system Air–sea interaction Multi-decadal variability

Übergeordnetes Werk:	Enthalten in: Climate dynamics - Berlin : Springer, 1986, 39(2012), 6 vom: 01. Mai, Seite 1507-1525
Übergeordnetes Werk:	volume:39 ; year:2012 ; number:6 ; day:01 ; month:05 ; pages:1507-1525

Links:	Volltext

DOI / URN:	10.1007/s00382-012-1370-8

Katalog-ID:	SPR004646398

Internformat


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100	1		\|a Kontoyiannis, H. \|e verfasserin \|4 aut
245	1	0	\|a Climatic variability of the sub-surface sea temperatures in the Aegean-Black Sea system and relation to meteorological forcing
264		1	\|c 2012
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520			\|a Abstract Non-smoothed yearly temperature records with minimal statistical uncertainties are constructed for winter and summer of the period 1950–2000 in two areas in the Aegean Sea, for the sub-surface layer of 80–120 m, and two areas in the Black Sea, for the sub-surface layer of sigma-theta isopycnals between 14.5 and 15.4. The specific areas are selected mostly because of the dense hydrographic-data coverage they have during the period 1950–2000. Two trend regimes appear in both Seas: a period of decreasing sea temperatures from the early/mid 1960s to the early/mid 1990s and an apparent warming afterwards. Trends in sea temperatures correlate with trends in the North Atlantic Oscillation (NAO) and partly the East Atlantic West Russian (EAWR) indexes, but the signs of NAO and/or EAWR cannot sufficiently justify the winter-to-winter temperature changes in the entire study area. In examining the wind flows in the sea-level-pressure maps for characteristic winters in which local peaks in the sea-temperature records occur, we identify particular sea-level-pressure structures that are not accounted for by the typical North-Atlantic or East Atlantic-West Russia positive or negative dipoles. In addition, there are winters when the Siberian High induces local maxima in sea-temperatures in the study area. A spectral-coherence analysis of the unfiltered winter sea-temperature and the corresponding teleconnection NAO/EAWR records, shows that common spectral and coherence peaks exist at ~5–6, ~9–10 and ~15–17 years.
650		4	\|a Aegean-Black Sea system \|7 (dpeaa)DE-He213
650		4	\|a Air–sea interaction \|7 (dpeaa)DE-He213
650		4	\|a Multi-decadal variability \|7 (dpeaa)DE-He213
700	1		\|a Papadopoulos, V. \|e verfasserin \|4 aut
700	1		\|a Kazmin, A. \|e verfasserin \|4 aut
700	1		\|a Zatsepin, A. \|e verfasserin \|4 aut
700	1		\|a Georgopoulos, D. \|e verfasserin \|4 aut
773	0	8	\|i Enthalten in \|t Climate dynamics \|d Berlin : Springer, 1986 \|g 39(2012), 6 vom: 01. Mai, Seite 1507-1525 \|w (DE-627)268128561 \|w (DE-600)1471747-5 \|x 1432-0894 \|7 nnns
773	1	8	\|g volume:39 \|g year:2012 \|g number:6 \|g day:01 \|g month:05 \|g pages:1507-1525
856	4	0	\|u https://dx.doi.org/10.1007/s00382-012-1370-8 \|z lizenzpflichtig \|3 Volltext
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936	b	k	\|a 38.80 \|q ASE
951			\|a AR
952			\|d 39 \|j 2012 \|e 6 \|b 01 \|c 05 \|h 1507-1525

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matchkey_str	article:14320894:2012----::lmtcaibltoteusraeetmeaueiteeenlcsaytmnrl
hierarchy_sort_str	2012
bklnumber	38.80
publishDate	2012
allfields	10.1007/s00382-012-1370-8 doi (DE-627)SPR004646398 (SPR)s00382-012-1370-8-e DE-627 ger DE-627 rakwb eng 550 ASE 38.80 bkl Kontoyiannis, H. verfasserin aut Climatic variability of the sub-surface sea temperatures in the Aegean-Black Sea system and relation to meteorological forcing 2012 Text txt rdacontent Computermedien c rdamedia Online-Ressource cr rdacarrier Abstract Non-smoothed yearly temperature records with minimal statistical uncertainties are constructed for winter and summer of the period 1950–2000 in two areas in the Aegean Sea, for the sub-surface layer of 80–120 m, and two areas in the Black Sea, for the sub-surface layer of sigma-theta isopycnals between 14.5 and 15.4. The specific areas are selected mostly because of the dense hydrographic-data coverage they have during the period 1950–2000. Two trend regimes appear in both Seas: a period of decreasing sea temperatures from the early/mid 1960s to the early/mid 1990s and an apparent warming afterwards. Trends in sea temperatures correlate with trends in the North Atlantic Oscillation (NAO) and partly the East Atlantic West Russian (EAWR) indexes, but the signs of NAO and/or EAWR cannot sufficiently justify the winter-to-winter temperature changes in the entire study area. In examining the wind flows in the sea-level-pressure maps for characteristic winters in which local peaks in the sea-temperature records occur, we identify particular sea-level-pressure structures that are not accounted for by the typical North-Atlantic or East Atlantic-West Russia positive or negative dipoles. In addition, there are winters when the Siberian High induces local maxima in sea-temperatures in the study area. A spectral-coherence analysis of the unfiltered winter sea-temperature and the corresponding teleconnection NAO/EAWR records, shows that common spectral and coherence peaks exist at ~5–6, ~9–10 and ~15–17 years. Aegean-Black Sea system (dpeaa)DE-He213 Air–sea interaction (dpeaa)DE-He213 Multi-decadal variability (dpeaa)DE-He213 Papadopoulos, V. verfasserin aut Kazmin, A. verfasserin aut Zatsepin, A. verfasserin aut Georgopoulos, D. verfasserin aut Enthalten in Climate dynamics Berlin : Springer, 1986 39(2012), 6 vom: 01. Mai, Seite 1507-1525 (DE-627)268128561 (DE-600)1471747-5 1432-0894 nnns volume:39 year:2012 number:6 day:01 month:05 pages:1507-1525 https://dx.doi.org/10.1007/s00382-012-1370-8 lizenzpflichtig Volltext GBV_USEFLAG_A SYSFLAG_A GBV_SPRINGER SSG-OPC-GGO SSG-OPC-ASE GBV_ILN_11 GBV_ILN_20 GBV_ILN_22 GBV_ILN_23 GBV_ILN_24 GBV_ILN_31 GBV_ILN_32 GBV_ILN_39 GBV_ILN_40 GBV_ILN_60 GBV_ILN_62 GBV_ILN_63 GBV_ILN_69 GBV_ILN_70 GBV_ILN_73 GBV_ILN_74 GBV_ILN_90 GBV_ILN_95 GBV_ILN_100 GBV_ILN_105 GBV_ILN_110 GBV_ILN_120 GBV_ILN_138 GBV_ILN_150 GBV_ILN_151 GBV_ILN_152 GBV_ILN_161 GBV_ILN_170 GBV_ILN_171 GBV_ILN_187 GBV_ILN_206 GBV_ILN_213 GBV_ILN_224 GBV_ILN_230 GBV_ILN_250 GBV_ILN_281 GBV_ILN_285 GBV_ILN_293 GBV_ILN_370 GBV_ILN_381 GBV_ILN_602 GBV_ILN_612 GBV_ILN_636 GBV_ILN_702 GBV_ILN_2001 GBV_ILN_2003 GBV_ILN_2004 GBV_ILN_2005 GBV_ILN_2006 GBV_ILN_2007 GBV_ILN_2008 GBV_ILN_2009 GBV_ILN_2010 GBV_ILN_2011 GBV_ILN_2014 GBV_ILN_2015 GBV_ILN_2020 GBV_ILN_2021 GBV_ILN_2025 GBV_ILN_2026 GBV_ILN_2027 GBV_ILN_2031 GBV_ILN_2034 GBV_ILN_2037 GBV_ILN_2038 GBV_ILN_2039 GBV_ILN_2044 GBV_ILN_2048 GBV_ILN_2049 GBV_ILN_2050 GBV_ILN_2055 GBV_ILN_2056 GBV_ILN_2057 GBV_ILN_2059 GBV_ILN_2061 GBV_ILN_2064 GBV_ILN_2065 GBV_ILN_2068 GBV_ILN_2070 GBV_ILN_2086 GBV_ILN_2088 GBV_ILN_2093 GBV_ILN_2106 GBV_ILN_2107 GBV_ILN_2108 GBV_ILN_2110 GBV_ILN_2111 GBV_ILN_2112 GBV_ILN_2113 GBV_ILN_2116 GBV_ILN_2118 GBV_ILN_2119 GBV_ILN_2122 GBV_ILN_2129 GBV_ILN_2143 GBV_ILN_2144 GBV_ILN_2147 GBV_ILN_2148 GBV_ILN_2152 GBV_ILN_2153 GBV_ILN_2188 GBV_ILN_2190 GBV_ILN_2232 GBV_ILN_2336 GBV_ILN_2446 GBV_ILN_2470 GBV_ILN_2472 GBV_ILN_2507 GBV_ILN_2522 GBV_ILN_2548 GBV_ILN_4012 GBV_ILN_4035 GBV_ILN_4037 GBV_ILN_4046 GBV_ILN_4112 GBV_ILN_4125 GBV_ILN_4126 GBV_ILN_4242 GBV_ILN_4246 GBV_ILN_4249 GBV_ILN_4251 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_4326 GBV_ILN_4328 GBV_ILN_4333 GBV_ILN_4334 GBV_ILN_4335 GBV_ILN_4336 GBV_ILN_4338 GBV_ILN_4393 GBV_ILN_4700 38.80 ASE AR 39 2012 6 01 05 1507-1525
spelling	10.1007/s00382-012-1370-8 doi (DE-627)SPR004646398 (SPR)s00382-012-1370-8-e DE-627 ger DE-627 rakwb eng 550 ASE 38.80 bkl Kontoyiannis, H. verfasserin aut Climatic variability of the sub-surface sea temperatures in the Aegean-Black Sea system and relation to meteorological forcing 2012 Text txt rdacontent Computermedien c rdamedia Online-Ressource cr rdacarrier Abstract Non-smoothed yearly temperature records with minimal statistical uncertainties are constructed for winter and summer of the period 1950–2000 in two areas in the Aegean Sea, for the sub-surface layer of 80–120 m, and two areas in the Black Sea, for the sub-surface layer of sigma-theta isopycnals between 14.5 and 15.4. The specific areas are selected mostly because of the dense hydrographic-data coverage they have during the period 1950–2000. Two trend regimes appear in both Seas: a period of decreasing sea temperatures from the early/mid 1960s to the early/mid 1990s and an apparent warming afterwards. Trends in sea temperatures correlate with trends in the North Atlantic Oscillation (NAO) and partly the East Atlantic West Russian (EAWR) indexes, but the signs of NAO and/or EAWR cannot sufficiently justify the winter-to-winter temperature changes in the entire study area. In examining the wind flows in the sea-level-pressure maps for characteristic winters in which local peaks in the sea-temperature records occur, we identify particular sea-level-pressure structures that are not accounted for by the typical North-Atlantic or East Atlantic-West Russia positive or negative dipoles. In addition, there are winters when the Siberian High induces local maxima in sea-temperatures in the study area. A spectral-coherence analysis of the unfiltered winter sea-temperature and the corresponding teleconnection NAO/EAWR records, shows that common spectral and coherence peaks exist at ~5–6, ~9–10 and ~15–17 years. Aegean-Black Sea system (dpeaa)DE-He213 Air–sea interaction (dpeaa)DE-He213 Multi-decadal variability (dpeaa)DE-He213 Papadopoulos, V. verfasserin aut Kazmin, A. verfasserin aut Zatsepin, A. verfasserin aut Georgopoulos, D. verfasserin aut Enthalten in Climate dynamics Berlin : Springer, 1986 39(2012), 6 vom: 01. Mai, Seite 1507-1525 (DE-627)268128561 (DE-600)1471747-5 1432-0894 nnns volume:39 year:2012 number:6 day:01 month:05 pages:1507-1525 https://dx.doi.org/10.1007/s00382-012-1370-8 lizenzpflichtig Volltext GBV_USEFLAG_A SYSFLAG_A GBV_SPRINGER SSG-OPC-GGO SSG-OPC-ASE GBV_ILN_11 GBV_ILN_20 GBV_ILN_22 GBV_ILN_23 GBV_ILN_24 GBV_ILN_31 GBV_ILN_32 GBV_ILN_39 GBV_ILN_40 GBV_ILN_60 GBV_ILN_62 GBV_ILN_63 GBV_ILN_69 GBV_ILN_70 GBV_ILN_73 GBV_ILN_74 GBV_ILN_90 GBV_ILN_95 GBV_ILN_100 GBV_ILN_105 GBV_ILN_110 GBV_ILN_120 GBV_ILN_138 GBV_ILN_150 GBV_ILN_151 GBV_ILN_152 GBV_ILN_161 GBV_ILN_170 GBV_ILN_171 GBV_ILN_187 GBV_ILN_206 GBV_ILN_213 GBV_ILN_224 GBV_ILN_230 GBV_ILN_250 GBV_ILN_281 GBV_ILN_285 GBV_ILN_293 GBV_ILN_370 GBV_ILN_381 GBV_ILN_602 GBV_ILN_612 GBV_ILN_636 GBV_ILN_702 GBV_ILN_2001 GBV_ILN_2003 GBV_ILN_2004 GBV_ILN_2005 GBV_ILN_2006 GBV_ILN_2007 GBV_ILN_2008 GBV_ILN_2009 GBV_ILN_2010 GBV_ILN_2011 GBV_ILN_2014 GBV_ILN_2015 GBV_ILN_2020 GBV_ILN_2021 GBV_ILN_2025 GBV_ILN_2026 GBV_ILN_2027 GBV_ILN_2031 GBV_ILN_2034 GBV_ILN_2037 GBV_ILN_2038 GBV_ILN_2039 GBV_ILN_2044 GBV_ILN_2048 GBV_ILN_2049 GBV_ILN_2050 GBV_ILN_2055 GBV_ILN_2056 GBV_ILN_2057 GBV_ILN_2059 GBV_ILN_2061 GBV_ILN_2064 GBV_ILN_2065 GBV_ILN_2068 GBV_ILN_2070 GBV_ILN_2086 GBV_ILN_2088 GBV_ILN_2093 GBV_ILN_2106 GBV_ILN_2107 GBV_ILN_2108 GBV_ILN_2110 GBV_ILN_2111 GBV_ILN_2112 GBV_ILN_2113 GBV_ILN_2116 GBV_ILN_2118 GBV_ILN_2119 GBV_ILN_2122 GBV_ILN_2129 GBV_ILN_2143 GBV_ILN_2144 GBV_ILN_2147 GBV_ILN_2148 GBV_ILN_2152 GBV_ILN_2153 GBV_ILN_2188 GBV_ILN_2190 GBV_ILN_2232 GBV_ILN_2336 GBV_ILN_2446 GBV_ILN_2470 GBV_ILN_2472 GBV_ILN_2507 GBV_ILN_2522 GBV_ILN_2548 GBV_ILN_4012 GBV_ILN_4035 GBV_ILN_4037 GBV_ILN_4046 GBV_ILN_4112 GBV_ILN_4125 GBV_ILN_4126 GBV_ILN_4242 GBV_ILN_4246 GBV_ILN_4249 GBV_ILN_4251 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_4326 GBV_ILN_4328 GBV_ILN_4333 GBV_ILN_4334 GBV_ILN_4335 GBV_ILN_4336 GBV_ILN_4338 GBV_ILN_4393 GBV_ILN_4700 38.80 ASE AR 39 2012 6 01 05 1507-1525
allfields_unstemmed	10.1007/s00382-012-1370-8 doi (DE-627)SPR004646398 (SPR)s00382-012-1370-8-e DE-627 ger DE-627 rakwb eng 550 ASE 38.80 bkl Kontoyiannis, H. verfasserin aut Climatic variability of the sub-surface sea temperatures in the Aegean-Black Sea system and relation to meteorological forcing 2012 Text txt rdacontent Computermedien c rdamedia Online-Ressource cr rdacarrier Abstract Non-smoothed yearly temperature records with minimal statistical uncertainties are constructed for winter and summer of the period 1950–2000 in two areas in the Aegean Sea, for the sub-surface layer of 80–120 m, and two areas in the Black Sea, for the sub-surface layer of sigma-theta isopycnals between 14.5 and 15.4. The specific areas are selected mostly because of the dense hydrographic-data coverage they have during the period 1950–2000. Two trend regimes appear in both Seas: a period of decreasing sea temperatures from the early/mid 1960s to the early/mid 1990s and an apparent warming afterwards. Trends in sea temperatures correlate with trends in the North Atlantic Oscillation (NAO) and partly the East Atlantic West Russian (EAWR) indexes, but the signs of NAO and/or EAWR cannot sufficiently justify the winter-to-winter temperature changes in the entire study area. In examining the wind flows in the sea-level-pressure maps for characteristic winters in which local peaks in the sea-temperature records occur, we identify particular sea-level-pressure structures that are not accounted for by the typical North-Atlantic or East Atlantic-West Russia positive or negative dipoles. In addition, there are winters when the Siberian High induces local maxima in sea-temperatures in the study area. A spectral-coherence analysis of the unfiltered winter sea-temperature and the corresponding teleconnection NAO/EAWR records, shows that common spectral and coherence peaks exist at ~5–6, ~9–10 and ~15–17 years. Aegean-Black Sea system (dpeaa)DE-He213 Air–sea interaction (dpeaa)DE-He213 Multi-decadal variability (dpeaa)DE-He213 Papadopoulos, V. verfasserin aut Kazmin, A. verfasserin aut Zatsepin, A. verfasserin aut Georgopoulos, D. verfasserin aut Enthalten in Climate dynamics Berlin : Springer, 1986 39(2012), 6 vom: 01. Mai, Seite 1507-1525 (DE-627)268128561 (DE-600)1471747-5 1432-0894 nnns volume:39 year:2012 number:6 day:01 month:05 pages:1507-1525 https://dx.doi.org/10.1007/s00382-012-1370-8 lizenzpflichtig Volltext GBV_USEFLAG_A SYSFLAG_A GBV_SPRINGER SSG-OPC-GGO SSG-OPC-ASE GBV_ILN_11 GBV_ILN_20 GBV_ILN_22 GBV_ILN_23 GBV_ILN_24 GBV_ILN_31 GBV_ILN_32 GBV_ILN_39 GBV_ILN_40 GBV_ILN_60 GBV_ILN_62 GBV_ILN_63 GBV_ILN_69 GBV_ILN_70 GBV_ILN_73 GBV_ILN_74 GBV_ILN_90 GBV_ILN_95 GBV_ILN_100 GBV_ILN_105 GBV_ILN_110 GBV_ILN_120 GBV_ILN_138 GBV_ILN_150 GBV_ILN_151 GBV_ILN_152 GBV_ILN_161 GBV_ILN_170 GBV_ILN_171 GBV_ILN_187 GBV_ILN_206 GBV_ILN_213 GBV_ILN_224 GBV_ILN_230 GBV_ILN_250 GBV_ILN_281 GBV_ILN_285 GBV_ILN_293 GBV_ILN_370 GBV_ILN_381 GBV_ILN_602 GBV_ILN_612 GBV_ILN_636 GBV_ILN_702 GBV_ILN_2001 GBV_ILN_2003 GBV_ILN_2004 GBV_ILN_2005 GBV_ILN_2006 GBV_ILN_2007 GBV_ILN_2008 GBV_ILN_2009 GBV_ILN_2010 GBV_ILN_2011 GBV_ILN_2014 GBV_ILN_2015 GBV_ILN_2020 GBV_ILN_2021 GBV_ILN_2025 GBV_ILN_2026 GBV_ILN_2027 GBV_ILN_2031 GBV_ILN_2034 GBV_ILN_2037 GBV_ILN_2038 GBV_ILN_2039 GBV_ILN_2044 GBV_ILN_2048 GBV_ILN_2049 GBV_ILN_2050 GBV_ILN_2055 GBV_ILN_2056 GBV_ILN_2057 GBV_ILN_2059 GBV_ILN_2061 GBV_ILN_2064 GBV_ILN_2065 GBV_ILN_2068 GBV_ILN_2070 GBV_ILN_2086 GBV_ILN_2088 GBV_ILN_2093 GBV_ILN_2106 GBV_ILN_2107 GBV_ILN_2108 GBV_ILN_2110 GBV_ILN_2111 GBV_ILN_2112 GBV_ILN_2113 GBV_ILN_2116 GBV_ILN_2118 GBV_ILN_2119 GBV_ILN_2122 GBV_ILN_2129 GBV_ILN_2143 GBV_ILN_2144 GBV_ILN_2147 GBV_ILN_2148 GBV_ILN_2152 GBV_ILN_2153 GBV_ILN_2188 GBV_ILN_2190 GBV_ILN_2232 GBV_ILN_2336 GBV_ILN_2446 GBV_ILN_2470 GBV_ILN_2472 GBV_ILN_2507 GBV_ILN_2522 GBV_ILN_2548 GBV_ILN_4012 GBV_ILN_4035 GBV_ILN_4037 GBV_ILN_4046 GBV_ILN_4112 GBV_ILN_4125 GBV_ILN_4126 GBV_ILN_4242 GBV_ILN_4246 GBV_ILN_4249 GBV_ILN_4251 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_4326 GBV_ILN_4328 GBV_ILN_4333 GBV_ILN_4334 GBV_ILN_4335 GBV_ILN_4336 GBV_ILN_4338 GBV_ILN_4393 GBV_ILN_4700 38.80 ASE AR 39 2012 6 01 05 1507-1525
allfieldsGer	10.1007/s00382-012-1370-8 doi (DE-627)SPR004646398 (SPR)s00382-012-1370-8-e DE-627 ger DE-627 rakwb eng 550 ASE 38.80 bkl Kontoyiannis, H. verfasserin aut Climatic variability of the sub-surface sea temperatures in the Aegean-Black Sea system and relation to meteorological forcing 2012 Text txt rdacontent Computermedien c rdamedia Online-Ressource cr rdacarrier Abstract Non-smoothed yearly temperature records with minimal statistical uncertainties are constructed for winter and summer of the period 1950–2000 in two areas in the Aegean Sea, for the sub-surface layer of 80–120 m, and two areas in the Black Sea, for the sub-surface layer of sigma-theta isopycnals between 14.5 and 15.4. The specific areas are selected mostly because of the dense hydrographic-data coverage they have during the period 1950–2000. Two trend regimes appear in both Seas: a period of decreasing sea temperatures from the early/mid 1960s to the early/mid 1990s and an apparent warming afterwards. Trends in sea temperatures correlate with trends in the North Atlantic Oscillation (NAO) and partly the East Atlantic West Russian (EAWR) indexes, but the signs of NAO and/or EAWR cannot sufficiently justify the winter-to-winter temperature changes in the entire study area. In examining the wind flows in the sea-level-pressure maps for characteristic winters in which local peaks in the sea-temperature records occur, we identify particular sea-level-pressure structures that are not accounted for by the typical North-Atlantic or East Atlantic-West Russia positive or negative dipoles. In addition, there are winters when the Siberian High induces local maxima in sea-temperatures in the study area. A spectral-coherence analysis of the unfiltered winter sea-temperature and the corresponding teleconnection NAO/EAWR records, shows that common spectral and coherence peaks exist at ~5–6, ~9–10 and ~15–17 years. Aegean-Black Sea system (dpeaa)DE-He213 Air–sea interaction (dpeaa)DE-He213 Multi-decadal variability (dpeaa)DE-He213 Papadopoulos, V. verfasserin aut Kazmin, A. verfasserin aut Zatsepin, A. verfasserin aut Georgopoulos, D. verfasserin aut Enthalten in Climate dynamics Berlin : Springer, 1986 39(2012), 6 vom: 01. Mai, Seite 1507-1525 (DE-627)268128561 (DE-600)1471747-5 1432-0894 nnns volume:39 year:2012 number:6 day:01 month:05 pages:1507-1525 https://dx.doi.org/10.1007/s00382-012-1370-8 lizenzpflichtig Volltext GBV_USEFLAG_A SYSFLAG_A GBV_SPRINGER SSG-OPC-GGO SSG-OPC-ASE GBV_ILN_11 GBV_ILN_20 GBV_ILN_22 GBV_ILN_23 GBV_ILN_24 GBV_ILN_31 GBV_ILN_32 GBV_ILN_39 GBV_ILN_40 GBV_ILN_60 GBV_ILN_62 GBV_ILN_63 GBV_ILN_69 GBV_ILN_70 GBV_ILN_73 GBV_ILN_74 GBV_ILN_90 GBV_ILN_95 GBV_ILN_100 GBV_ILN_105 GBV_ILN_110 GBV_ILN_120 GBV_ILN_138 GBV_ILN_150 GBV_ILN_151 GBV_ILN_152 GBV_ILN_161 GBV_ILN_170 GBV_ILN_171 GBV_ILN_187 GBV_ILN_206 GBV_ILN_213 GBV_ILN_224 GBV_ILN_230 GBV_ILN_250 GBV_ILN_281 GBV_ILN_285 GBV_ILN_293 GBV_ILN_370 GBV_ILN_381 GBV_ILN_602 GBV_ILN_612 GBV_ILN_636 GBV_ILN_702 GBV_ILN_2001 GBV_ILN_2003 GBV_ILN_2004 GBV_ILN_2005 GBV_ILN_2006 GBV_ILN_2007 GBV_ILN_2008 GBV_ILN_2009 GBV_ILN_2010 GBV_ILN_2011 GBV_ILN_2014 GBV_ILN_2015 GBV_ILN_2020 GBV_ILN_2021 GBV_ILN_2025 GBV_ILN_2026 GBV_ILN_2027 GBV_ILN_2031 GBV_ILN_2034 GBV_ILN_2037 GBV_ILN_2038 GBV_ILN_2039 GBV_ILN_2044 GBV_ILN_2048 GBV_ILN_2049 GBV_ILN_2050 GBV_ILN_2055 GBV_ILN_2056 GBV_ILN_2057 GBV_ILN_2059 GBV_ILN_2061 GBV_ILN_2064 GBV_ILN_2065 GBV_ILN_2068 GBV_ILN_2070 GBV_ILN_2086 GBV_ILN_2088 GBV_ILN_2093 GBV_ILN_2106 GBV_ILN_2107 GBV_ILN_2108 GBV_ILN_2110 GBV_ILN_2111 GBV_ILN_2112 GBV_ILN_2113 GBV_ILN_2116 GBV_ILN_2118 GBV_ILN_2119 GBV_ILN_2122 GBV_ILN_2129 GBV_ILN_2143 GBV_ILN_2144 GBV_ILN_2147 GBV_ILN_2148 GBV_ILN_2152 GBV_ILN_2153 GBV_ILN_2188 GBV_ILN_2190 GBV_ILN_2232 GBV_ILN_2336 GBV_ILN_2446 GBV_ILN_2470 GBV_ILN_2472 GBV_ILN_2507 GBV_ILN_2522 GBV_ILN_2548 GBV_ILN_4012 GBV_ILN_4035 GBV_ILN_4037 GBV_ILN_4046 GBV_ILN_4112 GBV_ILN_4125 GBV_ILN_4126 GBV_ILN_4242 GBV_ILN_4246 GBV_ILN_4249 GBV_ILN_4251 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_4326 GBV_ILN_4328 GBV_ILN_4333 GBV_ILN_4334 GBV_ILN_4335 GBV_ILN_4336 GBV_ILN_4338 GBV_ILN_4393 GBV_ILN_4700 38.80 ASE AR 39 2012 6 01 05 1507-1525
allfieldsSound	10.1007/s00382-012-1370-8 doi (DE-627)SPR004646398 (SPR)s00382-012-1370-8-e DE-627 ger DE-627 rakwb eng 550 ASE 38.80 bkl Kontoyiannis, H. verfasserin aut Climatic variability of the sub-surface sea temperatures in the Aegean-Black Sea system and relation to meteorological forcing 2012 Text txt rdacontent Computermedien c rdamedia Online-Ressource cr rdacarrier Abstract Non-smoothed yearly temperature records with minimal statistical uncertainties are constructed for winter and summer of the period 1950–2000 in two areas in the Aegean Sea, for the sub-surface layer of 80–120 m, and two areas in the Black Sea, for the sub-surface layer of sigma-theta isopycnals between 14.5 and 15.4. The specific areas are selected mostly because of the dense hydrographic-data coverage they have during the period 1950–2000. Two trend regimes appear in both Seas: a period of decreasing sea temperatures from the early/mid 1960s to the early/mid 1990s and an apparent warming afterwards. Trends in sea temperatures correlate with trends in the North Atlantic Oscillation (NAO) and partly the East Atlantic West Russian (EAWR) indexes, but the signs of NAO and/or EAWR cannot sufficiently justify the winter-to-winter temperature changes in the entire study area. In examining the wind flows in the sea-level-pressure maps for characteristic winters in which local peaks in the sea-temperature records occur, we identify particular sea-level-pressure structures that are not accounted for by the typical North-Atlantic or East Atlantic-West Russia positive or negative dipoles. In addition, there are winters when the Siberian High induces local maxima in sea-temperatures in the study area. A spectral-coherence analysis of the unfiltered winter sea-temperature and the corresponding teleconnection NAO/EAWR records, shows that common spectral and coherence peaks exist at ~5–6, ~9–10 and ~15–17 years. Aegean-Black Sea system (dpeaa)DE-He213 Air–sea interaction (dpeaa)DE-He213 Multi-decadal variability (dpeaa)DE-He213 Papadopoulos, V. verfasserin aut Kazmin, A. verfasserin aut Zatsepin, A. verfasserin aut Georgopoulos, D. verfasserin aut Enthalten in Climate dynamics Berlin : Springer, 1986 39(2012), 6 vom: 01. Mai, Seite 1507-1525 (DE-627)268128561 (DE-600)1471747-5 1432-0894 nnns volume:39 year:2012 number:6 day:01 month:05 pages:1507-1525 https://dx.doi.org/10.1007/s00382-012-1370-8 lizenzpflichtig Volltext GBV_USEFLAG_A SYSFLAG_A GBV_SPRINGER SSG-OPC-GGO SSG-OPC-ASE GBV_ILN_11 GBV_ILN_20 GBV_ILN_22 GBV_ILN_23 GBV_ILN_24 GBV_ILN_31 GBV_ILN_32 GBV_ILN_39 GBV_ILN_40 GBV_ILN_60 GBV_ILN_62 GBV_ILN_63 GBV_ILN_69 GBV_ILN_70 GBV_ILN_73 GBV_ILN_74 GBV_ILN_90 GBV_ILN_95 GBV_ILN_100 GBV_ILN_105 GBV_ILN_110 GBV_ILN_120 GBV_ILN_138 GBV_ILN_150 GBV_ILN_151 GBV_ILN_152 GBV_ILN_161 GBV_ILN_170 GBV_ILN_171 GBV_ILN_187 GBV_ILN_206 GBV_ILN_213 GBV_ILN_224 GBV_ILN_230 GBV_ILN_250 GBV_ILN_281 GBV_ILN_285 GBV_ILN_293 GBV_ILN_370 GBV_ILN_381 GBV_ILN_602 GBV_ILN_612 GBV_ILN_636 GBV_ILN_702 GBV_ILN_2001 GBV_ILN_2003 GBV_ILN_2004 GBV_ILN_2005 GBV_ILN_2006 GBV_ILN_2007 GBV_ILN_2008 GBV_ILN_2009 GBV_ILN_2010 GBV_ILN_2011 GBV_ILN_2014 GBV_ILN_2015 GBV_ILN_2020 GBV_ILN_2021 GBV_ILN_2025 GBV_ILN_2026 GBV_ILN_2027 GBV_ILN_2031 GBV_ILN_2034 GBV_ILN_2037 GBV_ILN_2038 GBV_ILN_2039 GBV_ILN_2044 GBV_ILN_2048 GBV_ILN_2049 GBV_ILN_2050 GBV_ILN_2055 GBV_ILN_2056 GBV_ILN_2057 GBV_ILN_2059 GBV_ILN_2061 GBV_ILN_2064 GBV_ILN_2065 GBV_ILN_2068 GBV_ILN_2070 GBV_ILN_2086 GBV_ILN_2088 GBV_ILN_2093 GBV_ILN_2106 GBV_ILN_2107 GBV_ILN_2108 GBV_ILN_2110 GBV_ILN_2111 GBV_ILN_2112 GBV_ILN_2113 GBV_ILN_2116 GBV_ILN_2118 GBV_ILN_2119 GBV_ILN_2122 GBV_ILN_2129 GBV_ILN_2143 GBV_ILN_2144 GBV_ILN_2147 GBV_ILN_2148 GBV_ILN_2152 GBV_ILN_2153 GBV_ILN_2188 GBV_ILN_2190 GBV_ILN_2232 GBV_ILN_2336 GBV_ILN_2446 GBV_ILN_2470 GBV_ILN_2472 GBV_ILN_2507 GBV_ILN_2522 GBV_ILN_2548 GBV_ILN_4012 GBV_ILN_4035 GBV_ILN_4037 GBV_ILN_4046 GBV_ILN_4112 GBV_ILN_4125 GBV_ILN_4126 GBV_ILN_4242 GBV_ILN_4246 GBV_ILN_4249 GBV_ILN_4251 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_4326 GBV_ILN_4328 GBV_ILN_4333 GBV_ILN_4334 GBV_ILN_4335 GBV_ILN_4336 GBV_ILN_4338 GBV_ILN_4393 GBV_ILN_4700 38.80 ASE AR 39 2012 6 01 05 1507-1525
language	English
source	Enthalten in Climate dynamics 39(2012), 6 vom: 01. Mai, Seite 1507-1525 volume:39 year:2012 number:6 day:01 month:05 pages:1507-1525
sourceStr	Enthalten in Climate dynamics 39(2012), 6 vom: 01. Mai, Seite 1507-1525 volume:39 year:2012 number:6 day:01 month:05 pages:1507-1525
format_phy_str_mv	Article
institution	findex.gbv.de
topic_facet	Aegean-Black Sea system Air–sea interaction Multi-decadal variability
dewey-raw	550
isfreeaccess_bool	false
container_title	Climate dynamics
authorswithroles_txt_mv	Kontoyiannis, H. @@aut@@ Papadopoulos, V. @@aut@@ Kazmin, A. @@aut@@ Zatsepin, A. @@aut@@ Georgopoulos, D. @@aut@@
publishDateDaySort_date	2012-05-01T00:00:00Z
hierarchy_top_id	268128561
dewey-sort	3550
id	SPR004646398
language_de	englisch
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author	Kontoyiannis, H.
spellingShingle	Kontoyiannis, H. ddc 550 bkl 38.80 misc Aegean-Black Sea system misc Air–sea interaction misc Multi-decadal variability Climatic variability of the sub-surface sea temperatures in the Aegean-Black Sea system and relation to meteorological forcing
authorStr	Kontoyiannis, H.
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topic_title	550 ASE 38.80 bkl Climatic variability of the sub-surface sea temperatures in the Aegean-Black Sea system and relation to meteorological forcing Aegean-Black Sea system (dpeaa)DE-He213 Air–sea interaction (dpeaa)DE-He213 Multi-decadal variability (dpeaa)DE-He213
topic	ddc 550 bkl 38.80 misc Aegean-Black Sea system misc Air–sea interaction misc Multi-decadal variability
topic_unstemmed	ddc 550 bkl 38.80 misc Aegean-Black Sea system misc Air–sea interaction misc Multi-decadal variability
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title	Climatic variability of the sub-surface sea temperatures in the Aegean-Black Sea system and relation to meteorological forcing
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title_full	Climatic variability of the sub-surface sea temperatures in the Aegean-Black Sea system and relation to meteorological forcing
author_sort	Kontoyiannis, H.
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author_browse	Kontoyiannis, H. Papadopoulos, V. Kazmin, A. Zatsepin, A. Georgopoulos, D.
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title_sort	climatic variability of the sub-surface sea temperatures in the aegean-black sea system and relation to meteorological forcing
title_auth	Climatic variability of the sub-surface sea temperatures in the Aegean-Black Sea system and relation to meteorological forcing
abstract	Abstract Non-smoothed yearly temperature records with minimal statistical uncertainties are constructed for winter and summer of the period 1950–2000 in two areas in the Aegean Sea, for the sub-surface layer of 80–120 m, and two areas in the Black Sea, for the sub-surface layer of sigma-theta isopycnals between 14.5 and 15.4. The specific areas are selected mostly because of the dense hydrographic-data coverage they have during the period 1950–2000. Two trend regimes appear in both Seas: a period of decreasing sea temperatures from the early/mid 1960s to the early/mid 1990s and an apparent warming afterwards. Trends in sea temperatures correlate with trends in the North Atlantic Oscillation (NAO) and partly the East Atlantic West Russian (EAWR) indexes, but the signs of NAO and/or EAWR cannot sufficiently justify the winter-to-winter temperature changes in the entire study area. In examining the wind flows in the sea-level-pressure maps for characteristic winters in which local peaks in the sea-temperature records occur, we identify particular sea-level-pressure structures that are not accounted for by the typical North-Atlantic or East Atlantic-West Russia positive or negative dipoles. In addition, there are winters when the Siberian High induces local maxima in sea-temperatures in the study area. A spectral-coherence analysis of the unfiltered winter sea-temperature and the corresponding teleconnection NAO/EAWR records, shows that common spectral and coherence peaks exist at ~5–6, ~9–10 and ~15–17 years.
abstractGer	Abstract Non-smoothed yearly temperature records with minimal statistical uncertainties are constructed for winter and summer of the period 1950–2000 in two areas in the Aegean Sea, for the sub-surface layer of 80–120 m, and two areas in the Black Sea, for the sub-surface layer of sigma-theta isopycnals between 14.5 and 15.4. The specific areas are selected mostly because of the dense hydrographic-data coverage they have during the period 1950–2000. Two trend regimes appear in both Seas: a period of decreasing sea temperatures from the early/mid 1960s to the early/mid 1990s and an apparent warming afterwards. Trends in sea temperatures correlate with trends in the North Atlantic Oscillation (NAO) and partly the East Atlantic West Russian (EAWR) indexes, but the signs of NAO and/or EAWR cannot sufficiently justify the winter-to-winter temperature changes in the entire study area. In examining the wind flows in the sea-level-pressure maps for characteristic winters in which local peaks in the sea-temperature records occur, we identify particular sea-level-pressure structures that are not accounted for by the typical North-Atlantic or East Atlantic-West Russia positive or negative dipoles. In addition, there are winters when the Siberian High induces local maxima in sea-temperatures in the study area. A spectral-coherence analysis of the unfiltered winter sea-temperature and the corresponding teleconnection NAO/EAWR records, shows that common spectral and coherence peaks exist at ~5–6, ~9–10 and ~15–17 years.
abstract_unstemmed	Abstract Non-smoothed yearly temperature records with minimal statistical uncertainties are constructed for winter and summer of the period 1950–2000 in two areas in the Aegean Sea, for the sub-surface layer of 80–120 m, and two areas in the Black Sea, for the sub-surface layer of sigma-theta isopycnals between 14.5 and 15.4. The specific areas are selected mostly because of the dense hydrographic-data coverage they have during the period 1950–2000. Two trend regimes appear in both Seas: a period of decreasing sea temperatures from the early/mid 1960s to the early/mid 1990s and an apparent warming afterwards. Trends in sea temperatures correlate with trends in the North Atlantic Oscillation (NAO) and partly the East Atlantic West Russian (EAWR) indexes, but the signs of NAO and/or EAWR cannot sufficiently justify the winter-to-winter temperature changes in the entire study area. In examining the wind flows in the sea-level-pressure maps for characteristic winters in which local peaks in the sea-temperature records occur, we identify particular sea-level-pressure structures that are not accounted for by the typical North-Atlantic or East Atlantic-West Russia positive or negative dipoles. In addition, there are winters when the Siberian High induces local maxima in sea-temperatures in the study area. A spectral-coherence analysis of the unfiltered winter sea-temperature and the corresponding teleconnection NAO/EAWR records, shows that common spectral and coherence peaks exist at ~5–6, ~9–10 and ~15–17 years.
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container_issue	6
title_short	Climatic variability of the sub-surface sea temperatures in the Aegean-Black Sea system and relation to meteorological forcing
url	https://dx.doi.org/10.1007/s00382-012-1370-8
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author2	Papadopoulos, V. Kazmin, A. Zatsepin, A. Georgopoulos, D.
author2Str	Papadopoulos, V. Kazmin, A. Zatsepin, A. Georgopoulos, D.
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doi_str	10.1007/s00382-012-1370-8
up_date	2024-07-04T02:00:45.512Z
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Climatic variability of the sub-surface sea temperatures in the Aegean-Black Sea system and relation to meteorological forcing

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