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This is the first benthic δ\u003Cjats:sup>18\u003C\u002Fjats:sup>O stack composed of more than three records to extend beyond 850 ka, and we use its improved signal quality to identify 24 new marine isotope stages in the early Pliocene. We also present a new LR04 age model for the Pliocene‐Pleistocene derived from tuning the δ\u003Cjats:sup>18\u003C\u002Fjats:sup>O stack to a simple ice model based on 21 June insolation at 65°N. Stacked sedimentation rates provide additional age model constraints to prevent overtuning. Despite a conservative tuning strategy, the LR04 benthic stack exhibits significant coherency with insolation in the obliquity band throughout the entire 5.3 Myr and in the precession band for more than half of the record. The LR04 stack contains significantly more variance in benthic δ\u003Cjats:sup>18\u003C\u002Fjats:sup>O than previously published stacks of the late Pleistocene as the result of higher‐resolution records, a better alignment technique, and a greater percentage of records from the Atlantic. Finally, the relative phases of the stack's 41‐ and 23‐kyr components suggest that the precession component of δ\u003Cjats:sup>18\u003C\u002Fjats:sup>O from 2.7–1.6 Ma is primarily a deep‐water temperature signal and that the phase of δ\u003Cjats:sup>18\u003C\u002Fjats:sup>O precession response changed suddenly at 1.6 Ma.\u003C\u002Fjats:p>",{"EN":41,"VI":42},"A Pliocene‐Pleistocene stack of 57 globally distributed benthic δ\u003Csup>18\u003C\u002Fsup>O records","Chuỗi xếp chồng Pliocen–Pleistocen từ 57 bản ghi δ18O sinh vật đáy phân bố toàn cầu",{"VOID":44},"10.1029\u002F2004pa001071","PUBLICATION","VERIFIED","Auto Verify",[49],"EN",[51],"VI","https:\u002F\u002Fagupubs.onlinelibrary.wiley.com\u002Fdoi\u002F10.1029\u002F2004PA001071",[54,73],{"id":55,"sortIndex":18,"researcher":17,"roles":56,"affiliations":57,"properties":66,"displayName":70,"givenName":17,"familyName":17},"87ff27dd-cc36-4d18-9968-cd450f17902a",[],[58],{"id":59,"sortIndex":18,"affiliation":60,"properties":17},"b0ca18c1-37d5-4524-a216-c12998d0c139",{"id":59,"createTime":17,"updateTime":17,"relativeEntities":61,"slug":17,"properties":62,"entityType":17,"verifyStatus":17,"verifyTime":17,"verifyNote":17,"languages":17,"translateLanguages":17,"viewCount":17,"url":17,"parentIds":65,"statistic":17},[],{"title":63},{"VI":64},"Department of Geological Sciences, Brown University, Providence, Rhode Island, USA",[],{"orcid":67,"title":69,"openalex":71},{"VOID":68},"https:\u002F\u002Forcid.org\u002F0000-0001-7859-0096",{"EN":70},"L. 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C., 1995, Benthic foraminiferal stable isotope stratigraphy from Site 846: 0–1.8 Ma, Proc. Ocean Drill. Program Sci. Results, 138, 839",{},{"id":17,"text":267,"url":17,"identifiers":268},"Mix A. C., 1995, Benthic foraminifer stable isotope record from Site 849 (0–5 Ma): Local and global climate changes, Proc. Ocean Drill. Program Sci. Results, 138, 371",{},{"id":17,"text":270,"url":17,"identifiers":271},"10.1029\u002F1999PA000457",{"doi":270},{"id":17,"text":273,"url":17,"identifiers":274},"10.1016\u002F0012-821X(75)90156-9",{"doi":273},{"id":17,"text":276,"url":17,"identifiers":277},"10.1029\u002FPA005i001p00043",{"doi":276},{"id":17,"text":279,"url":17,"identifiers":280},"10.1126\u002Fscience.279.5355.1335",{"doi":279},{"id":17,"text":282,"url":17,"identifiers":283},"Pierre C., 2001, Stable isotope record of the last 500 k.y. at Site 1087 (Southern Cape Basin), Proc. Ocean Drill. Program Sci. 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Project, 81, 599",{},{"id":17,"text":327,"url":17,"identifiers":328},"10.1029\u002FGM032p0303",{"doi":327},{"id":17,"text":330,"url":17,"identifiers":331},"10.1017\u002FS0263593300020782",{"doi":330},{"id":17,"text":333,"url":17,"identifiers":334},"Shackleton N. J., 1995, Pliocene stable isotope stratigraphy of ODP Site 846, Proc. Ocean Drill. Program Sci. Results, 138, 337",{},{"id":17,"text":336,"url":17,"identifiers":337},"Shackleton N. J., 1995, A new late Neogene time scale: Application to Leg 138 sites, Proc. Ocean Drill. Program Sci. Results, 138, 73",{},{"id":17,"text":339,"url":17,"identifiers":340},"10.1029\u002F2000PA000513",{"doi":339},{"id":17,"text":342,"url":17,"identifiers":343},"10.1016\u002FS0025-3227(03)00127-0",{"doi":342},{"id":17,"text":345,"url":17,"identifiers":346},"10.1016\u002F0016-7037(93)90416-T",{"doi":345},{"id":17,"text":348,"url":17,"identifiers":349},"10.1016\u002FS0012-821X(02)00923-8",{"doi":348},{"id":17,"text":351,"url":17,"identifiers":352},"Tiedemann R.(1991) Acht Millionen Jahre Klimageschichte von Nordwest Afrika und Paläo‐Ozeanographie des angrenzenden Atlantiks Ber. Rep. 46 190 pp. Geol.‐Paläontol. Inst. und Mus. Christian‐Albrechts‐Univ. Kiel Germany.",{},{"id":17,"text":354,"url":17,"identifiers":355},"Tiedemann R., 1997, Deep‐water cicurlation, chemistry, and terrigenous sediment supply in the equatorial Atlantic during the Pliocene, 3.3–2.6 Ma and 5–4.5 Ma, Proc. Ocean Drill. Program Sci. 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The timing of increased grain size is coincident with the onset of strong summer monsoon winds and dust storm activity over the Arabian Peninsula and Middle East. Data spanning a full annual cycle show that eolian grain size is highly correlated with barometric pressure (\u003Cjats:italic>r\u003C\u002Fjats:italic>=−0.91) and wind speed (\u003Cjats:italic>r\u003C\u002Fjats:italic>=0.84), enabling calibration of the downcore record in terms of these primary meteorological variables. Eolian flux is highly correlated with organic carbon flux (\u003Cjats:italic>r\u003C\u002Fjats:italic>=0.80); both increase 6–8 weeks after the grain size increase and summer monsoon onset. This lag, and the low correlation between eolian grain size and eolian flux (\u003Cjats:italic>r\u003C\u002Fjats:italic>=0.36), likely result from the differential sinking rates of large and small dust particles in the surface waters as well as biological scavenging associated with monsoon‐induced productivity.\u003C\u002Fjats:p>",{"EN":388},"Dust response to seasonal atmospheric forcing: Proxy evaluation and calibration",{"VOID":390},"10.1029\u002F98pa02131","Author affiliation is blank",[49],"https:\u002F\u002Fagupubs.onlinelibrary.wiley.com\u002Fdoi\u002F10.1029\u002F98PA02131",[395],{"id":396,"sortIndex":18,"researcher":17,"roles":397,"affiliations":398,"properties":399,"displayName":403,"givenName":17,"familyName":17},"d8f82de5-03bd-4593-8eba-0bf317998bbb",[],[],{"orcid":400,"title":402,"openalex":404},{"VOID":401},"https:\u002F\u002Forcid.org\u002F0000-0002-1136-7815",{"EN":403},"Steven C. 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All three sites show an increase in marine organic carbon (OC) accumulation rates during the C\u002FT Oceanic Anoxic Event (OAE). The occurrence of molecular fossils of anoxygenic photosynthetic green sulfur bacteria, lack of bioturbation, and high abundance of redox sensitive trace metals indicate sulfidic conditions, periodically reaching up into the photic zone before as well as during the C\u002FT OAE. During the C\u002FT OAE, there was a significant rise of the chemocline as indicated by the increase in concentrations of molecular fossils of green sulfur bacteria and Mo\u002FAl ratios. The presence of molecular fossils of the green strain of green sulfur bacteria indicates that euxinic conditions periodically even occurred at very shallow water depths of 15 m or less during the C\u002FT OAE. However, bottom water conditions did not dramatically change as indicated by more or less constant V\u002FAl and Zn\u002FAl ratios at site 367. 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The mid‐Cretaceous ocean circulation and its impact on Greenhouse Climate dynamics Ph.D. thesis Pa. State Univ. University Park 1999.",{},{"id":17,"text":981,"url":17,"identifiers":982},"10.1038\u002F341516a0",{"doi":981},{"id":17,"text":984,"url":17,"identifiers":985},"10.1016\u002F0016-7037(93)90334-S",{"doi":984},{"id":17,"text":987,"url":17,"identifiers":988},"Ricken W., 1993, Sedimentation as a three‐component system, Lect. Notes Earth Sci., 51, 1",{},{"id":17,"text":990,"url":17,"identifiers":991},"10.1029\u002FGB002i004p00427",{"doi":990},{"id":17,"text":993,"url":17,"identifiers":994},"Schlanger S. O., 1976, Cretaceous oceanoc anoxic events: Causes and consequences, Geol. Mijnbouw, 55, 179",{},{"id":17,"text":996,"url":17,"identifiers":997},"Scholle P. 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The \u003Cjats:italic>δ\u003C\u002Fjats:italic>\u003Cjats:sup>13\u003C\u002Fjats:sup>C\u003Cjats:sub>carb\u003C\u002Fjats:sub>, \u003Cjats:italic>δ\u003C\u002Fjats:italic>\u003Cjats:sup>13\u003C\u002Fjats:sup>C\u003Cjats:sub>org\u003C\u002Fjats:sub>, and \u003Cjats:italic>δ\u003C\u002Fjats:italic>\u003Cjats:sup>18\u003C\u002Fjats:sup>O chemostratigraphy of a black shale–bearing CTB succession in the Vocontian Basin of France is described and correlated at high resolution to the European CTB reference section at Eastbourne, England, and to successions in Germany, the equatorial and midlatitude proto‐North Atlantic, and the U.S. Western Interior Seaway (WIS). Δ\u003Cjats:sup>13\u003C\u002Fjats:sup>C (offset between \u003Cjats:italic>δ\u003C\u002Fjats:italic>\u003Cjats:sup>13\u003C\u002Fjats:sup>C\u003Cjats:sub>carb\u003C\u002Fjats:sub> and \u003Cjats:italic>δ\u003C\u002Fjats:italic>\u003Cjats:sup>13\u003C\u002Fjats:sup>C\u003Cjats:sub>org\u003C\u002Fjats:sub>) is shown to be a good \u003Cjats:italic>p\u003C\u002Fjats:italic>CO\u003Cjats:sub>2\u003C\u002Fjats:sub> proxy that is consistent with \u003Cjats:italic>p\u003C\u002Fjats:italic>CO\u003Cjats:sub>2\u003C\u002Fjats:sub> records obtained using biomarker \u003Cjats:italic>δ\u003C\u002Fjats:italic>\u003Cjats:sup>13\u003C\u002Fjats:sup>C data from Atlantic black shales and leaf stomata data from WIS sections. Boreal chalk \u003Cjats:italic>δ\u003C\u002Fjats:italic>\u003Cjats:sup>18\u003C\u002Fjats:sup>O records show sea surface temperature (SST) changes that closely follow the Δ\u003Cjats:sup>13\u003C\u002Fjats:sup>C \u003Cjats:italic>p\u003C\u002Fjats:italic>CO\u003Cjats:sub>2\u003C\u002Fjats:sub> proxy and confirm TEX\u003Cjats:sub>86\u003C\u002Fjats:sub> results from deep ocean sites. Rising \u003Cjats:italic>p\u003C\u002Fjats:italic>CO\u003Cjats:sub>2\u003C\u002Fjats:sub> and SST during the Late Cenomanian is attributed to volcanic degassing; \u003Cjats:italic>p\u003C\u002Fjats:italic>CO\u003Cjats:sub>2\u003C\u002Fjats:sub> and SST maxima occurred at the onset of black shale deposition, followed by falling \u003Cjats:italic>p\u003C\u002Fjats:italic>CO\u003Cjats:sub>2\u003C\u002Fjats:sub> and cooling due to carbon sequestration by marine organic productivity and preservation, and increased silicate weathering. A marked \u003Cjats:italic>p\u003C\u002Fjats:italic>CO\u003Cjats:sub>2\u003C\u002Fjats:sub> minimum (∼25% fall) occurred with a SST minimum (Plenus Cold Event) showing >4°C of cooling in ∼40 kyr. Renewed increases in \u003Cjats:italic>p\u003C\u002Fjats:italic>CO\u003Cjats:sub>2\u003C\u002Fjats:sub>, SST, and \u003Cjats:italic>δ\u003C\u002Fjats:italic>\u003Cjats:sup>13\u003C\u002Fjats:sup>C during latest Cenomanian black shale deposition suggest that a continuing volcanogenic CO\u003Cjats:sub>2\u003C\u002Fjats:sub> flux overrode further drawdown effects. Maximum \u003Cjats:italic>p\u003C\u002Fjats:italic>CO\u003Cjats:sub>2\u003C\u002Fjats:sub> and SST followed the end of OAE2, associated with a falling nutrient supply during the Early Turonian eustatic highstand.\u003C\u002Fjats:p>",{"EN":1068},"Black shale deposition, atmospheric CO\u003Csub>2\u003C\u002Fsub> drawdown, and cooling during the Cenomanian‐Turonian Oceanic Anoxic Event",{"VOID":1070},"10.1029\u002F2010pa002081",[49],"https:\u002F\u002Fagupubs.onlinelibrary.wiley.com\u002Fdoi\u002F10.1029\u002F2010PA002081",[1074,1093,1116,1135,1154],{"id":1075,"sortIndex":18,"researcher":17,"roles":1076,"affiliations":1077,"properties":1086,"displayName":1090,"givenName":17,"familyName":17},"18bdb89c-58c2-4047-8c05-fba39711ea12",[],[1078],{"id":1079,"sortIndex":18,"affiliation":1080,"properties":17},"855f1ef8-7265-4ddb-8589-4f85cf610925",{"id":1079,"createTime":17,"updateTime":17,"relativeEntities":1081,"slug":17,"properties":1082,"entityType":17,"verifyStatus":17,"verifyTime":17,"verifyNote":17,"languages":17,"translateLanguages":17,"viewCount":17,"url":17,"parentIds":1085,"statistic":17},[],{"title":1083},{"EN":1084},"Centre for Earth and Environmental Science Research, School of Geography, Geology and the Environment, Kingston University London, Kingston upon Thames, UK",[],{"orcid":1087,"title":1089,"openalex":1091},{"VOID":1088},"https:\u002F\u002Forcid.org\u002F0000-0003-3184-3097",{"EN":1090},"Ian Jarvis",{"VOID":1092},"A5047448597",{"id":1094,"sortIndex":75,"researcher":17,"roles":1095,"affiliations":1096,"properties":1111,"displayName":1113,"givenName":17,"familyName":17},"bff8328d-fc7b-40c2-8212-be86324b1d36",[],[1097,1103],{"id":1079,"sortIndex":18,"affiliation":1098,"properties":17},{"id":1079,"createTime":17,"updateTime":17,"relativeEntities":1099,"slug":17,"properties":1100,"entityType":17,"verifyStatus":17,"verifyTime":17,"verifyNote":17,"languages":17,"translateLanguages":17,"viewCount":17,"url":17,"parentIds":1102,"statistic":17},[],{"title":1101},{"EN":1084},[],{"id":1104,"sortIndex":75,"affiliation":1105,"properties":17},"28fbe5fb-b5cd-42cc-b640-e5f67586e30d",{"id":1104,"createTime":17,"updateTime":17,"relativeEntities":1106,"slug":17,"properties":1107,"entityType":17,"verifyStatus":17,"verifyTime":17,"verifyNote":17,"languages":17,"translateLanguages":17,"viewCount":17,"url":17,"parentIds":1110,"statistic":17},[],{"title":1108},{"EN":1109},"Ichron Limited, Northwich, UK",[],{"title":1112,"openalex":1114},{"EN":1113},"John Lignum",{"VOID":1115},"A5048986636",{"id":1117,"sortIndex":426,"researcher":17,"roles":1118,"affiliations":1119,"properties":1128,"displayName":1132,"givenName":17,"familyName":17},"9991bc7d-24c7-4953-a3ee-f7849f6a11b6",[],[1120],{"id":1121,"sortIndex":18,"affiliation":1122,"properties":17},"0c0c828c-85b8-402a-abcb-cb7a99816c8e",{"id":1121,"createTime":17,"updateTime":17,"relativeEntities":1123,"slug":17,"properties":1124,"entityType":17,"verifyStatus":17,"verifyTime":17,"verifyNote":17,"languages":17,"translateLanguages":17,"viewCount":17,"url":17,"parentIds":1127,"statistic":17},[],{"title":1125},{"VI":1126}," Department of Earth Sciences, Durham University, Durham, UK",[],{"orcid":1129,"title":1131,"openalex":1133},{"VOID":1130},"https:\u002F\u002Forcid.org\u002F0000-0003-2296-7530",{"EN":1132},"Darren R. 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The cores range in water depth from 1451 to 2658 m. In one core, we generated estimates of sea surface temperature (SST) and of ice‐rafted detritus (IRD) delivery for all of stage 5. We reconstruct bathymeric profiles of δ\u003Cjats:sup>13\u003C\u002Fjats:sup>C for stage 6, Termination II, and three time slices of substage 5e. The δ\u003Cjats:sup>13\u003C\u002Fjats:sup>C profiles indicate that local deep water geometry during stage 6 was similar to that of the last glaciation, with glacial North Atlantic Intermediate Water (GNAIW) overlying deeper waters partially of southern origin. An anomalously large peak in IRD, coupled with planktonic δ\u003Cjats:sup>18\u003C\u002Fjats:sup>O evidence for iceberg melting immediately precedes Termination II and is otherwise similar to stage 2 and 3 Heinrich events. During the termination, low δ\u003Cjats:sup>13\u003C\u002Fjats:sup>C values are observed in cores near and above 2 km, providing evidence of reduced GNAIW production in association with deglacial melting. In the shallowest cores, low δ\u003Cjats:sup>13\u003C\u002Fjats:sup>C values persist into early substage 5e, indicating that the southward retreat of southern‐source waters was not completed until well after the beginning of the substage. In contrast to Termination I, SSTs remained cold until the end of the deglaciation; this may be why there is little evidence from marine and terrestrial sequences for a pronounced climate reversal on Termination II despite what is now clear evidence of a significant reduction in ocean ventilation. The faunal data suggest that SSTs during early 5e were about 7°C warmer than during the glaciation. SST rose several degrees from early to middle substage 5e, peaked in middle substage 5e at about 10°C above glacial values, and then gradually declined by about 5°C. These changes were linked to variations in water mass configuration, as interpreted from benthic δ\u003Cjats:sup>13\u003C\u002Fjats:sup>C evidence. Most of the evidence suggests that oscillations superimposed on the gradual SST trend were 1°–2°C, in contrast to the larger SST changes (3°–4°C) documented for substage 5d.\u003C\u002Fjats:p>",{"EN":2207},"Marine core evidence for reduced deep water production during Termination II followed by a relatively stable substage 5e (Eemian)",{"VOID":2209},"10.1029\u002F96pa03133",[49],"https:\u002F\u002Fagupubs.onlinelibrary.wiley.com\u002Fdoi\u002F10.1029\u002F96PA03133",[2213,2224,2233],{"id":2214,"sortIndex":18,"researcher":17,"roles":2215,"affiliations":2216,"properties":2217,"displayName":2221,"givenName":17,"familyName":17},"167d68a4-ef54-44e2-a39d-1a948c0b5066",[],[],{"orcid":2218,"title":2220,"openalex":2222},{"VOID":2219},"https:\u002F\u002Forcid.org\u002F0000-0003-2946-5904",{"EN":2221},"Delia W Oppo",{"VOID":2223},"A5001481194",{"id":2225,"sortIndex":75,"researcher":17,"roles":2226,"affiliations":2227,"properties":2228,"displayName":2230,"givenName":17,"familyName":17},"de4bbffe-dc67-499d-93b7-239c5c348f26",[],[],{"title":2229,"openalex":2231},{"EN":2230},"Michael Horowitz",{"VOID":2232},"A5107842929",{"id":2234,"sortIndex":426,"researcher":17,"roles":2235,"affiliations":2236,"properties":2237,"displayName":2241,"givenName":17,"familyName":17},"9c7ea6d9-be2f-426c-a173-11cb13b0f7ab",[],[],{"orcid":2238,"title":2240,"openalex":2242},{"VOID":2239},"https:\u002F\u002Forcid.org\u002F0000-0002-8865-9584",{"EN":2241},"Scott J. 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K. E.Platon M. S.Hackworth andP.Aharon Historical record of benthic foraminiferal species at a methane‐hydrate dissociation site Green Canyon Gulf of Mexico paper presented atGSA Annual Meeting Geol. Soc. of Am. Boulder Colo. 5 – 8 Nov.2001.",{},{"id":17,"text":2695,"url":17,"identifiers":2696},"10.1029\u002F2001GC000196",{"doi":2695},{"id":17,"text":2698,"url":17,"identifiers":2699},"10.1016\u002F0031-0182(89)90033-3",{"doi":2698},{"id":17,"text":2701,"url":17,"identifiers":2702},"10.1016\u002FS0012-821X(99)00092-8",{"doi":2701},{"id":17,"text":2704,"url":17,"identifiers":2705},"10.1029\u002FGM124p0087",{"doi":2704},{"id":17,"text":2707,"url":17,"identifiers":2708},"Thomas E., 1998, The Paleocene\u002FEocene Boundary (IGCP Project 308), 214",{},{"id":17,"text":2710,"url":17,"identifiers":2711},"Torres M. E. G.Bohrmann K.Brown M. A.de Angelis D.Hammond G.Klinkhammer J.McManus E.Suess andA.Trehu Geochemical observations on Hydrate Ridge Cascadia Margin during R\u002FV‐ATLANTIS‐cruise aT3‐35b July 1999 COAS Data Rep. 174 Ref. 99‐3 Oreg. St. Univ. Corvallis Oreg. 1999.",{},{"id":17,"text":2713,"url":17,"identifiers":2714},"10.1016\u002FS0012-821X(02)00733-1",{"doi":2713},{"id":17,"text":2716,"url":17,"identifiers":2717},"10.1130\u002F0091-7613(1999)027\u003C0939:TASEOA>2.3.CO;2",{"doi":2716},{"id":17,"text":2719,"url":17,"identifiers":2720},"A. M. Trehu N. L. Bangs M. A. Arsenault G. Bohrmann C. Goldfinger J. E. Johnson Y. Nakamura M. E. 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P., 1987, An underwater gas source in the Sea of Okhotsk West of Paramushir Island, Oceanology, 27, 598",{},{"id":2734,"createTime":2735,"updateTime":2735,"relativeEntities":2736,"slug":2737,"properties":2738,"entityType":45,"verifyStatus":46,"verifyTime":2749,"verifyNote":47,"languages":2750,"translateLanguages":17,"viewCount":18,"primaryUrl":2751,"fullTextUrl":17,"authors":2752,"publicationType":93,"publisherRelationship":2899,"citationCount":2913,"citationInfo":2914,"publishDate":2917,"publishYear":2915,"citationAnalyzeStatus":16,"lastCitationAnalyze":17,"indexDatabases":2918,"openAccess":17,"references":2919,"isForceReanalyzing":374},"8aeea121-c00f-4300-b640-0556764c08f1","2024-11-26T14:56:54.046+00:00",[],"Experimental-determination-of-salinity-temperature-growth-and-metabolic-effects-on-shell-isotope-chemistry-of-i-Mytilus-edulis-i-collected-from-Maine-and-Greenland",{"openalex":2739,"mag":2741,"abstract":2743,"title":2745,"doi":2747},{"VOID":2740},"W1949620474",{"VOID":2742},"1949620474",{"EN":2744},"\u003Cjats:p>To study the effects of temperature, salinity, and life processes (growth rates, size, metabolic effects, and physiological\u002Fgenetic effects) on newly precipitated bivalve carbonate, we quantified shell isotopic chemistry of adult and juvenile animals of the intertidal bivalve\u003Cjats:italic>Mytilus edulis\u003C\u002Fjats:italic>(Blue mussel) collected alive from western Greenland and the central Gulf of Maine and cultured them under controlled conditions. Data for juvenile and adult\u003Cjats:italic>M. edulis\u003C\u002Fjats:italic>bivalves cultured in this study, and previously by Wanamaker et al. (2006), yielded statistically identical paleotemperature relationships. On the basis of these experiments we have developed a species‐specific paleotemperature equation for the bivalve\u003Cjats:italic>M. edulis\u003C\u002Fjats:italic>[T °C = 16.28 (±0.10) − 4.57 (±0.15) {\u003Cjats:italic>δ\u003C\u002Fjats:italic>\u003Cjats:sup>18\u003C\u002Fjats:sup>O\u003Cjats:sub>c\u003C\u002Fjats:sub>VPBD −\u003Cjats:italic>δ\u003C\u002Fjats:italic>\u003Cjats:sup>18\u003C\u002Fjats:sup>O\u003Cjats:sub>w\u003C\u002Fjats:sub>VSMOW} + 0.06 (±0.06) {\u003Cjats:italic>δ\u003C\u002Fjats:italic>\u003Cjats:sup>18\u003C\u002Fjats:sup>O\u003Cjats:sub>c\u003C\u002Fjats:sub>VPBD −\u003Cjats:italic>δ\u003C\u002Fjats:italic>\u003Cjats:sup>18\u003C\u002Fjats:sup>O\u003Cjats:sub>w\u003C\u002Fjats:sub>VSMOW}\u003Cjats:sup>2\u003C\u002Fjats:sup>; r\u003Cjats:sup>2\u003C\u002Fjats:sup>= 0.99; N = 323; p < 0.0001]. Compared to the Kim and O'Neil (1997) inorganic calcite equation,\u003Cjats:italic>M. edulis\u003C\u002Fjats:italic>deposits its shell in isotope equilibrium (\u003Cjats:italic>δ\u003C\u002Fjats:italic>\u003Cjats:sup>18\u003C\u002Fjats:sup>O\u003Cjats:sub>calcite\u003C\u002Fjats:sub>) with ambient water. Carbon isotopes (\u003Cjats:italic>δ\u003C\u002Fjats:italic>\u003Cjats:sup>13\u003C\u002Fjats:sup>C\u003Cjats:sub>calcite\u003C\u002Fjats:sub>) from sampled shells were substantially more negative than predicted values, indicating an uptake of metabolic carbon into shell carbonate, and\u003Cjats:italic>δ\u003C\u002Fjats:italic>\u003Cjats:sup>13\u003C\u002Fjats:sup>C\u003Cjats:sub>calcite\u003C\u002Fjats:sub>disequilibrium increased with increasing salinity. Sampled shells of\u003Cjats:italic>M. edulis\u003C\u002Fjats:italic>showed no significant trends in\u003Cjats:italic>δ\u003C\u002Fjats:italic>\u003Cjats:sup>18\u003C\u002Fjats:sup>O\u003Cjats:sub>calcite\u003C\u002Fjats:sub>based on size, cultured growth rates, or geographic collection location, suggesting that vital effects do not affect\u003Cjats:italic>δ\u003C\u002Fjats:italic>\u003Cjats:sup>18\u003C\u002Fjats:sup>O\u003Cjats:sub>calcite\u003C\u002Fjats:sub>in\u003Cjats:italic>M. edulis\u003C\u002Fjats:italic>. The broad modern and paleogeographic distribution of this bivalve, its abundance during the Holocene, and the lack of an intraspecies physiologic isotope effect demonstrated here make it an ideal nearshore paleoceanographic proxy throughout much of the North Atlantic Ocean.\u003C\u002Fjats:p>",{"EN":2746},"Experimental determination of salinity, temperature, growth, and metabolic effects on shell isotope chemistry of\u003Ci>Mytilus edulis\u003C\u002Fi>collected from Maine and Greenland",{"VOID":2748},"10.1029\u002F2006pa001352","2024-11-26T14:56:54.045+00:00",[49],"https:\u002F\u002Fagupubs.onlinelibrary.wiley.com\u002Fdoi\u002F10.1029\u002F2006PA001352",[2753,2772,2789,2804,2821,2838,2857,2876],{"id":2754,"sortIndex":18,"researcher":17,"roles":2755,"affiliations":2756,"properties":2765,"displayName":2769,"givenName":17,"familyName":17},"fb6b2f2a-8518-454f-be0e-91ed61a65b4a",[],[2757],{"id":2758,"sortIndex":18,"affiliation":2759,"properties":17},"a445c90c-b2f0-46b5-8d2f-b0b087e638a0",{"id":2758,"createTime":17,"updateTime":17,"relativeEntities":2760,"slug":17,"properties":2761,"entityType":17,"verifyStatus":17,"verifyTime":17,"verifyNote":17,"languages":17,"translateLanguages":17,"viewCount":17,"url":17,"parentIds":2764,"statistic":17},[],{"title":2762},{"VI":2763},"Climate Change Institute and Department of Earth Sciences, University of Maine, Orono Maine, USA",[],{"orcid":2766,"title":2768,"openalex":2770},{"VOID":2767},"https:\u002F\u002Forcid.org\u002F0000-0002-6560-6420",{"EN":2769},"Alan D. 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Using data from Deep Sea Drilling Project (DSDP) site 576 in the Western Pacific, this method yields a glacial to interglacial change in δ\u003Cjats:sup>18\u003C\u002Fjats:sup>O\u003Cjats:sub>sw\u003C\u002Fjats:sub> of 1.0±0.25‰. This value for Δδ\u003Cjats:sup>18\u003C\u002Fjats:sup>O\u003Cjats:sub>sw\u003C\u002Fjats:sub> is the first direct measurement of deep ocean δ\u003Cjats:sup>18\u003C\u002Fjats:sup>O for the last glacial maximum and avoids the problems of spatial and temporal variability of the δ\u003Cjats:sup>18\u003C\u002Fjats:sup>O of surface water implicit in previous determinations. More precise, higher‐resolution pore fluid measurements are required to improve this determination.\u003C\u002Fjats:p>",{"EN":3150},"Determination of δ\u003Csup>18\u003C\u002Fsup>O of Seawater in the Deep Ocean during the Last Glacial Maximum",{"VOID":3152},"10.1029\u002F92pa02796","2024-11-26T14:56:34.747+00:00",[49],"https:\u002F\u002Fagupubs.onlinelibrary.wiley.com\u002Fdoi\u002F10.1029\u002F92PA02796",[3157,3166],{"id":3158,"sortIndex":18,"researcher":17,"roles":3159,"affiliations":3160,"properties":3161,"displayName":3163,"givenName":17,"familyName":17},"38e43e4c-fba6-4193-9305-09cfc5447e5b",[],[],{"title":3162,"openalex":3164},{"EN":3163},"D. P. 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