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NARROW
GeoRef Subject
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all geography including DSDP/ODP Sites and Legs
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oxygen
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fossils
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Invertebrata
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Protista
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Osculosida
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orthosilicates
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Primary terms
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Antarctica
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Arctic Ocean
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Asia
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Far East
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continental shelf (2)
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crust (9)
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data processing (1)
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Deep Sea Drilling Project
-
IPOD
-
Leg 62
-
DSDP Site 463 (1)
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-
Leg 71
-
DSDP Site 511 (1)
-
-
Leg 72
-
DSDP Site 516 (1)
-
-
Leg 74
-
DSDP Site 526 (1)
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-
Leg 80
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DSDP Site 549 (1)
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Leg 90
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DSDP Site 590 (2)
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DSDP Site 593 (2)
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Leg 94
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DSDP Site 607 (1)
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DSDP Site 610 (1)
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Leg 14
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DSDP Site 138 (1)
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Leg 21
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DSDP Site 206 (1)
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DSDP Site 207 (5)
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DSDP Site 208 (5)
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DSDP Site 209 (1)
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Leg 26
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DSDP Site 253 (1)
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DSDP Site 254 (1)
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DSDP Site 258 (1)
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Leg 28
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DSDP Site 264 (1)
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Leg 29
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DSDP Site 277 (1)
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DSDP Site 280 (1)
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DSDP Site 281 (1)
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DSDP Site 284 (2)
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Leg 33
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DSDP Site 318 (1)
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Leg 36
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DSDP Site 327 (1)
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Leg 39
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DSDP Site 357 (1)
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inclusions
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-
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Maestrichtian (2)
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Jurassic
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Kimmeridge Clay (1)
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metals
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alkaline earth metals
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rare earths
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samarium
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metamorphic rocks
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metamorphism (1)
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-
Leg 104 (1)
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Leg 113
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ODP Site 690 (1)
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Leg 119
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ODP Site 744 (1)
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Leg 120
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ODP Site 748 (1)
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Leg 121
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ODP Site 758 (1)
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Leg 159
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ODP Site 959 (1)
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Leg 165
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ODP Site 998 (1)
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Leg 166
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ODP Site 1007 (1)
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Leg 174AX (1)
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Leg 181
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ODP Site 1123 (1)
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Leg 184
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ODP Site 1146 (1)
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Leg 189
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ODP Site 1171 (3)
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Leg 202
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ocean floors (3)
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New Caledonia Basin (2)
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South Pacific
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West Pacific
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Ontong Java Plateau (1)
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Tasman Sea
Middle Miocene climate–carbon cycle dynamics: Keys for understanding future trends on a warmer Earth?
ABSTRACT The late early to middle Miocene period (18–12.7 Ma) was marked by profound environmental change, as Earth entered into the warmest climate phase of the Neogene (Miocene climate optimum) and then transitioned to a much colder mode with development of permanent ice sheets on Antarctica. Integration of high-resolution benthic foraminiferal isotope records in well-preserved sedimentary successions from the Pacific, Southern, and Indian Oceans provides a long-term perspective with which to assess relationships among climate change, ocean circulation, and carbon cycle dynamics during these successive climate reversals. Fundamentally different modes of ocean circulation and carbon cycling prevailed on an almost ice-free Earth during the Miocene climate optimum (ca. 16.9–14.7 Ma). Comparison of δ 13 C profiles revealed a marked decrease in ocean stratification and in the strength of the meridional overturning circulation during the Miocene climate optimum. We speculate that labile polar ice sheets, weaker Southern Hemisphere westerlies, higher sea level, and more acidic, oxygen-depleted oceans promoted shelf-basin partitioning of carbonate deposition and a weaker meridional overturning circulation, reducing the sequestration efficiency of the biological pump. X-ray fluorescence scanning data additionally revealed that 100 k.y. eccentricity-paced transient hyperthermal events coincided with intense episodes of deep-water acidification and deoxygenation. The in-phase coherence of δ 18 O and δ 13 C at the eccentricity band further suggests that orbitally paced processes such as remineralization of organic carbon from the deep-ocean dissolved organic carbon pool and/or weathering-induced carbon and nutrient fluxes from tropical monsoonal regions to the ocean contributed to the high amplitude variability of the marine carbon cycle. Stepwise global cooling and ice-sheet expansion during the middle Miocene climate transition (ca. 14.7–13.8 Ma) were associated with dampening of astronomically driven climate cycles and progressive steepening of the δ 13 C gradient between intermediate and deep waters, indicating intensification and vertical expansion of ocean meridional overturning circulation following the end of the Miocene climate optimum. Together, these results underline the crucial role of the marine carbon cycle and low-latitude processes in driving climate dynamics on an almost ice-free Earth.
Stratigraphic and sedimentological aspects of the worldwide distribution of Apectodinium in Paleocene/Eocene Thermal Maximum deposits
Abstract The Paleocene/Eocene Thermal Maximum (PETM) is characterized by pronounced global warming and associated environmental changes. In the more-or-less two decades since prior regional syntheses of Apectodinium distribution at the PETM, extensive biological and geochemical datasets have elucidated the effect of rising world temperatures on climate and the biome. A Carbon Isotope Excursion (CIE) that marks the Paleocene/Eocene Boundary is associated with an acme of marine dinocysts of the genus Apectodinium in many locations. Distinctive foraminiferal and calcareous nannofossil populations may also be present. For this updated, dinocyst-oriented view of the PETM, data from worldwide locations have been evaluated with an emphasis on stratigraphic and sedimentological context. What has emerged is that a change in lithology is common, often to a distinctive siltstone or claystone unit, which contrasts with underlying and overlying lithotypes. This change, present in shallow marine/coastal settings and in deep-water turbidite deposits, is attributed to radical modifications of precipitation and erosional processes. An abrupt boundary carries the implication that some time (of unknowable duration) is potentially missing, which then requires caution in the interpretation of the pacing of events in relation to that boundary. In most instances an ‘abrupt’ or ‘rapid’ CIE onset can be attributed to a data gap at a hiatus, particularly in shallow shelf settings where transgression resulted from sea-level rise associated with the PETM. Truly gradational lower boundaries of the PETM interval are quite unusual and, if present, are poorly known so far. Gradational upper boundaries are more common, but erosional upper boundaries have been reported. Taxonomic changes have been made to clarify identification issues that have adversely impacted some biostratigraphic interpretations. Apectodinium hyperacanthum has been retained in Wetzeliella , its original genus. The majority of specimens previously assigned to Apectodinium hyperacanthum or Wetzeliella ( Apectodinium ) hyperacanthum have been reassigned to an informal species, Apectodinium sp. 1. Dracodinium astra has been retained in its original genus as Wetzeliella astra and is emended.
Continental-scale geographic change across Zealandia during Paleogene subduction initiation
Multispectral coherence: Which decomposition should we use?
Multiattribute analysis for channel element discrimination in the Taranaki Basin, offshore New Zealand
A benthic flux from calcareous sediments results in non-conservative neodymium behavior during lateral transport: A study from the Tasman Sea
Globoconella Pseudospinosa , N. Sp.: a New Early Pliocene Planktonic Foraminifera from the Southwest Pacific
3-D seismic imaging of the plumbing system of the Kora Volcano, Taranaki Basin, New Zealand: The influence of syn-rift structure on shallow igneous intrusion architecture
Erosion of the Southern Alps of New Zealand during the last deglaciation
Regional volcanism of northern Zealandia: post-Gondwana break-up magmatism on an extended, submerged continent
Abstract: Volcanism of Late Cretaceous–Miocene age is more widespread across the Zealandia continent than previously recognized. New age and geochemical information from widely spaced northern Zealandia seafloor samples can be related to three volcanotectonic regimes: (1) age-progressive, hotspot-style, low-K, alkali-basalt-dominated volcanism in the Lord Howe Seamount Chain. The northern end of the chain ( c. 28 Ma) is spatially and temporally linked to the 40–28 Ma South Rennell Trough spreading centre. (2) Subalkaline, intermediate to silicic, medium-K to shoshonitic lavas of >78–42 Ma age within and near to the New Caledonia Basin. These lavas indicate that the basin and the adjacent Fairway Ridge are underlain by continental rather than oceanic crust, and are a record of Late Cretaceous–Eocene intracontinental rifting or, in some cases, speculatively subduction. (3) Spatially scattered, non-hotspot, alkali basalts of 30–18 Ma age from Loyalty Ridge, Lord Howe Rise, Aotea Basin and Reinga Basin. These lavas are part of a more extensive suite of Zealandia-wide, 97–0 Ma intraplate volcanics. Ages of northern Zealandia alkali basalts confirm that a late Cenozoic pulse of intraplate volcanism erupted across both northern and southern Zealandia. Collectively, the three groups of volcanic rocks emphasize the important role of magmatism in the geology of northern Zealandia, both during and after Gondwana break-up. There is no compelling evidence in our dataset for Late Cretaceous–Paleocene subduction beneath northern Zealandia. Supplementary material: Trace element compositions of zircons and whole-rock chemical compositions obtained by previous studies are available at: https://doi.org/10.6084/m9.figshare.c.3850975
Two-phase Cretaceous–Paleocene rifting in the Taranaki Basin region, New Zealand; implications for Gondwana break-up
Widespread compression associated with Eocene Tonga-Kermadec subduction initiation
Animated reconstructions of the Late Cretaceous to Cenozoic northward migration of Australia, and implications for the generation of east Australian mafic magmatism
Structural analysis of extended Australian continental crust: Capel and Faust basins, Lord Howe Rise
Abstract The Capel and Faust basins (northern Lord Howe Rise) are located in the SW Pacific between Australia, New Zealand and New Caledonia. New seismic, gravity, magnetic and bathymetry data and rock samples have enabled the construction of a three-dimensional geological model providing insights into the crustal architecture and basin stratigraphy. Multiple large depocentres up to 150 km long and 40 km wide, containing over 6 km of sediment, have been identified. These basins probably evolved through two major Early Cretaceous rifting episodes leading to the final break-up of the eastern Gondwanan margin. Pre-break-up plate restorations and potential field data suggest that pre-rift basement is a collage of several discrete terranes, including a Palaeozoic orogen, pre-rift sedimentary basins and rift-precursor igneous rocks. It is likely that a pre-existing NW-trending basement fabric, inherited from the New England Orogen (onshore eastern Australia), had a strong influence on the evolution of basin architecture. This basement fabric was subjected to oblique rifting along an east–west vector in the ?Early Cretaceous to Cenomanian and NE–SW-oriented orthogonal rifting in the ?Cenomanian to Campanian. This has resulted in three structural provinces in the study area: Eastern Flank, Central Belt and Western Flank.
Two-stage development of the Paparoa Metamorphic Core Complex, West Coast, South Island, New Zealand: Hot continental extension precedes sea-floor spreading by ∼25 m.y.
Near-tropical Early Eocene terrestrial temperatures at the Australo-Antarctic margin, western Tasmania
Mantle dynamics of continentwide Cenozoic subsidence and tilting of Australia
Three time lines through the neritic stratigraphic record distributed around the northern margin of the Australo-Antarctic Gulf (AAG) mark three fundamental shifts in global environments collectively comprising the Auversian facies shift. The three lines are: (1) the beginning: the Khirthar transgression and the onset of neritic carbonate accumulation in the Bartonian Age (preceding onset of the Middle Eocene climatic optimum [MECO]); (2) the midlife change (Bartonian-Priabonian transition): the shift from carbonate-rich to carbonate-poor, higher-nutrient environments under estuarine circulation, causing widespread dysaerobia culminating in opaline silicas; and (3) the Eocene-Oligocene = Priabonian-Rupelian boundary and glaciation during oxygen isotope event Oi-1, with return of improved ventilation in neritic environments and resumption of carbonate accumulation. Meanwhile, it was warm and very wet at ~60°S. In developing a scenario for the death of the AAG, the birth of the Southern Ocean, and the transition from Paleogene greenhouse Earth to Neogene icehouse Earth, the neritic record of the northern margin is more in accord with the “Dinocyst biogeographic hypothesis” than with the “Tasman gateway hypothesis.”