supplement

supplement_百度翻译supplement [英]ˈsʌplɪmənt[美]ˈsʌpləməntvt. 增补，补充n. 增补，补充;补充物;增刊，副刊[例句]Powdered formula is the most convenient to supplement breastfeeding.奶粉配方用于补充母乳喂养是最方便的。您好，答题不易如有帮助请采纳，谢谢！

supplement[英][ˈsʌplɪmənt][美][ˈsʌpləmənt]vt.增补，补充; n.增补，补充; 补充物; 增刊，副刊; 第三人称单数：supplements复数：supplements现在进行时：supplementing过去式：supplemented例句:1.Then there"s cocoa as a dietary supplement. 此外，可可还被用作一种膳食补充成分。

　　supplement英 [ˈsʌplɪmənt] 美 [ˈsʌpləmənt]　　vt.增补，补充;　　n.增补，补充; 补充物; 增刊，副刊;　　[例句]Specifically, the US trade representative should supplement the annual survey of foreign country trade barriers to include market distortions of any sort.　　具体而言，美国贸易代表应该将任何形式的市场扭曲，都增补进对外国贸易壁垒的年度调查报告。　　[其他]第三人称单数：supplements 复数：supplements 现在分词：supplementing 过去式：supplemented 形近词： implement antiplement complement

In the Late Proterozoic，profound changes occurred that included the break-up of the supercontinent Rodinia，geographically extensive glaciations，dramatic isotope excursions of，for example，strontium and carbon Jacobsen and Kaufman，this volume on a scale unprecedented in the Phanerozoic，intervals with high abundance of acritarchs suggesting alternating periods of low and high organic productivity，and the emergence of trace，body and skeletonized fossils. Close to the Precambrian-Cambrian boundary， other dramatic biotic events continue that have been described as the Cambrian Explosion. Extensive biomineralization of soft tissue in many major groups of organisms resulted in diverse skeletonized faunas being preserved in the fossil record. Some new biochemical evidence suggests that the initial radiation of major clades of metazoans began about 1200 Ma rather than about 600 Ma ago. If so，what processes or threshold conditions existed to suppress the abundance，size，and diversity radiation for about 600 Ma from 1200 to 600 Ma? Answers may lie in the chemical nature of these oceans. Martin has argued for superoligotrophic oceans for most of the Early Paleozoic. He considered that the oceans were predominantly stratified and only sluggishly circulating; as a consequence there was limited mixing and transfer of nutrients from the deep ocean to surface waters for utilization by organisms ( Fig. 1) . If the oxygen and CO2levels of about 0. 2，2 and 20 times the present atmospheric levels，respectively，for the Cambrian are correct，as interpreted by Berner，then a critical threshold factor for respiration and for ecological expansion would have been the O2levels in the surface and deeper part of the oceans. The interplay of anoxic waters with surface waters somewhat enriched in oxygen is likely to have been a critical factor in the waves of extinctions evident in Cambrian and early Ordovician rocks. Such encroachment of anoxic waters onto carbonate platforms was considered by Zhuravlev and Wood to cause the mid-Early Cambrian Botomian extinction and later the periods of eutrophication to be characterized by phytoplankton blooms. Using Sr and C isotopes data from the Upper Cambrian，Saltzman et al. argued that catastrophic ocean overturning produced similar periodic，widespread，anoxic conditions. Such pulses may well explain the pattern of trilobite extinctions that were used to define biomere boundaries by Palmer.Progressive ventilation of the deeper oceans appears to have occurred through the Ordovician and Silurian. Attempts to deduce the pattern of oceanic circulation for intervals throughout these two periods have been made by Wilde and Wilde et al. ，respectively，using the paleogeographic reconstructions of Scotese and McKerrow. The superoligotrophic conditions of these oceans and the warm greenhouse climate state throughout the Early Paleozoic were only interrupted in the Ashgill and early Llandovery ( Late Ordovician—Early Silurian) when a continental glaciation developed across North Africa that was then located near the southern pole. The onset of aggressive thermohaline circulation both chilled and ventilated the deep ocean with several glacial phases occurring over about a 10 Ma interval，but with the main Hirnantian phase perhaps lasting only for a few hundred thousand years. The cause of this short-lived icehouse state within such a long 200 Ma period of greenhouse conditions is still speculative and some authors have related it to the passage of part of Gondwana over the south polar region or to the brief drawdown of atmospheric CO2. Even as greenhouse states prevailed through much of the Silurian，detailed analysis on conodont microfossil distributions and related microfacies changes have suggested to Jeppsson and Aldridge et al. that the Silurian ocean state and associated climate was characterized by alternating primo and secundo states with periodic，but rapid turnover intervals. The principal differences being a warm humid phase vs. a drier cooler phase that resulted in significantly different lithologies and reef tracts across the low latitude carbonate platforms. Fig. 1 Indices of ancient nutrient fluxes and productivity through the last 650 MaAnother seemingly important factor in paleoceanography is the changing pattern of eustasy. Sensitive records are preserved on the carbonate platforms and examination of several cratons allows a global pattern to emerge for the Ordovician and Silurian. Major transgressions produced as epicontinental seas that generated important sites of warm，dense hypersaline waters and the periodic development and then closure of this system with transgressive and then regressive events has not yet been fully accommodated into paleoceanographic models. Such oscillations certainly produced major global bio-events. For the Late Ordovician，the Caradoc transgression was the largest of the Phanerozoic and may have been generated by much higher rates of sea-floor spreading and / or the occurrence of a mantle superplume.There is a marked contrast in the studies of paleoceanography of the Early Paleozoic with those of the Mesozoic and Cenozoic as noted initially. The application of a wide range of isotope proxy data with DSDP and ODP core samples and detailed analysis of abundant cores and outcrop studies in well preserved sedimentary basins，such as the Western Interior Seaway of North America，have allowed increasingly sophisticated interpretations of paleoceanography. Periods of anoxia，of less than 1 Ma duration have been recognized in all major oceans for the Late Barremian to Late Aptian of the Early Cretaceous. Peak oxygen deficiency corresponded to highly eutrophic conditions whereas less intense dysoxic / anoxic intervals were characteristic of oligotrophic conditions. The Albian and part of the Cenomanian were the warmest parts of the Cretaceous at a time when there appears to have been four times the present atmospheric level of CO2. Some authors have argued that ready transfer of heat from the equator to the polar regions reduced the latitudinal gradient and fostered a warm green-house state. Larson advocated the presence of a mid-Cretaceous mantle superplume in the western Pacific that produced the Ontong Java Plateau and this model was elaborated upon by Caldeira and Rampino to explain the widespread black shales，high organic productivity and oil accumulation ( Fig. 2) . Even within the Cretaceous there are considerable changes in oceanic temperature gradients. Huber et al. showed that during the Coniacian—Santonian the difference between low and high latitude surface- water paleotemperatures was in the range of 0—4℃ . As cooling increased towards the end of the period，the temperature difference increased to about 14℃ . Detailed investigations of the Cretaceous biotas have revealed complex patterns of marine biogeography that primarily mirror the changing major water masses and current systems along with the modifications to the Tethys Seaway and the Western Interior Seaway of North America. The open equatorial circulation around much of the globe via the Tethyan Seaway and the presence of wide shallow shelves on which warm saline waters were generated seem to be critical components to maintain the ultra warm greenhouse state at this time.Fig. 2 Inferred mid-Cretaceous mantle superplume showing increased ocean crust generation， sea level，black shales and related increases in ocean temperature and oil generation. These changes correspond to an interval free of magnetic reversals.In addition to the Cretaceous deep oceans，particularly Tethys，Pacific and opening Atlantic， large shelf seas developed as in Europe and the Western. Interior Sea of North America. The latter has received considerable attention because of the large stratigraphic database developed through oil exploration. In the Western Canada Sedimentary Basin，over 150，000 wells have been drilled in Alberta alone，with many aimed at the Cretaceous or passing to Devonian targets. The Cretaceous Seaway initially spread north from the Gulf of Mexico and south from the Beaufort Sea， meeting in Albian time. The sea was constrained on the west by emerging tectonic forelands tied to major Cordilleran orogenic phases and terrane accretion on the Pacific margin; on the east it lapped progressively eastwards on a largely peneplained Canadian Shield. Tectonic deformation generated an asymmetrically subsiding foreland basin and an eastward migrating peripheral bulge. From sedimentological and paleontological studies the seaway is estimated to have been up to 1000 m deep in the west-central corridor. The western margin was subjected to much clastic fill from the deforming foreland，transported by complex river systems. Volcanoes contributed extensive， eastwardly transported ash falls with over 200 bentonites in the Cretaceous sequence，which，with detailed biostratigraphy，have provided a remarkably detailed chemostratigraphy to unravel the changes to the seaway through time.Within this overall framework，there have been several recent attempts to understand and model the paleoceanography of this north-south seaway. Kaufmann initially tried to discriminate the inflowing north and south waters from surface freshwater caps derived from rivers mainly flowing from the emerging Cordilleran foreland. More recent attempts have modelled current flows within the sea-way. Jewell noted that salinity stratification in the seaway could have been established rapidly. Slingerland et al. proposed that river flux was important and likely controlled the strong counterclockwise gyre occupying the entire north-south extent of the seaway.In the Cenozoic，an early phase of global warming ( Paleocene—Eocene) was followed by a progressive but variable decline in mean annual temperature ( Oligocene—Recent) . The onset of glaciation occurred first in Antarctica close to the Eocene—Oligocene boundary ( ca. 34 Ma) . Major Arctic glaciation appears to have been initiated in the late Pliocene ( ca. 2. 8 Ma) . The Cenozoic provides an opportunity to investigate the processes of changeover from a greenhouse to icehouse state. Fundamental questions remain unresolved about the initiation and maintenance of these two states and of the complex feedback loops in the climate system. Of particular interest are the processes of heat transfer to the high latitudes during a greenhouse state and their collapse during the icehouse state. Two possible principal causes have been advanced， possibly interrelated. Firstly，decreased atmospheric CO2partly derived from the weathering of uplifted crustal rocks during the late phases of alpine orogeny ( e. g. ， Himalayan， Alps， Andes， Cordillera) . Secondly，there was substantially altered ocean circulation，particularly the onset of the deep ocean conveyor belt with thermohaline circulation derived from sinking of cold water in the North Atlantic. In this latter case，the pattern of ocean circulation is strongly affected by paleogeographic barriers such as the opening of the Drake Passage or closing of the Panama Isthmus.For the early Cenozoic greenhouse state，O"Connell et al. modelled atmospheric circulation conditions. In one experiment，they showed that under extreme zonal conditions evaporation may have substantially exceeded precipitation leading to the generation of very saline water. Zachos et al. discussed early Cenozoic temperatures from the oceanographic view，and Hovan and Rea used ODP data to examine the particular changes at the Paleocene / Eocene boundary. Here，they noted the dramatic changes that occur over a period of about 1. 2 Ma including: extinction of some benthic foraminifera and changes in calcareous plankton assemblages，oceanic warming，decrease in carbon isotope ratios，reduction in wind strength，an increase in hydrothermal activity. This same change is found in the continental record and is marked by the first appearance of several important modern mammalian orders. The Paleocene and early Eocene climates were controlled primarily by large scale meridional energy transport through the oceans rather than the atmosphere and in part influenced by tectonic events. Hovan and Rea showed that a strong reduction in Paleocene / Eocene wind stress occurs in both hemispheres at the boundary，related to decreased latitudinal thermal gradients produced by a more effective poleward heat transport via the deep ocean.There were dramatic changes to these greenhouse conditions at the Eocene / Oligocene boundary，including: fall in oceanic bottom water temperatures; 1 km drop in the calcium compensation depth in the Pacific; increase in deep sea unconformities; extinctions of planktonic foraminifera. These were apparently related to sudden high latitude cooling and enhanced oceanic thermohaline circulation. The onset of Antarctic glaciation occurred at about 34. 5 Ma seemingly closely related to the opening of the Drake Passage ( between South America and Antarctica) : surface and intermediate water circulation is documented by paleontology at this time，with other geologic evidence suggesting complete opening and deepwater circulation by about 30 Ma. These circulation changes induced a new position for the polar front and strongly influenced the pattern of upwelling and productivity.The late Neogene marks the onset of Arctic glaciation and enhanced global cooling. A significant oceanographic circulation event during this time was the full closure，evaporation and then reflooding of the Mediterranean Sea; the Messinian Event ( ca. 8—5 Ma ) in the late Miocene. The more recent work based on defined sequence stratigraphy and chronostratigraphy has shown that there were two distinct phases of evaporite accumulation，each associated with a sea-level drop that were in turn likely to be of glacio-eustatic origin. Salt a

In the Late Proterozoic，profound changes occurred that included the break-up of the supercontinent Rodinia，geographically extensive glaciations，dramatic isotope excursions of，for example，strontium and carbon Jacobsen and Kaufman，this volume on a scale unprecedented in the Phanerozoic，intervals with high abundance of acritarchs suggesting alternating periods of low and high organic productivity，and the emergence of trace，body and skeletonized fossils. Close to the Precambrian-Cambrian boundary， other dramatic biotic events continue that have been described as the Cambrian Explosion. Extensive biomineralization of soft tissue in many major groups of organisms resulted in diverse skeletonized faunas being preserved in the fossil record. Some new biochemical evidence suggests that the initial radiation of major clades of metazoans began about 1200 Ma rather than about 600 Ma ago. If so，what processes or threshold conditions existed to suppress the abundance，size，and diversity radiation for about 600 Ma from 1200 to 600 Ma? Answers may lie in the chemical nature of these oceans. Martin has argued for superoligotrophic oceans for most of the Early Paleozoic. He considered that the oceans were predominantly stratified and only sluggishly circulating; as a consequence there was limited mixing and transfer of nutrients from the deep ocean to surface waters for utilization by organisms ( Fig. 1) . If the oxygen and CO2levels of about 0. 2，2 and 20 times the present atmospheric levels，respectively，for the Cambrian are correct，as interpreted by Berner，then a critical threshold factor for respiration and for ecological expansion would have been the O2levels in the surface and deeper part of the oceans. The interplay of anoxic waters with surface waters somewhat enriched in oxygen is likely to have been a critical factor in the waves of extinctions evident in Cambrian and early Ordovician rocks. Such encroachment of anoxic waters onto carbonate platforms was considered by Zhuravlev and Wood to cause the mid-Early Cambrian Botomian extinction and later the periods of eutrophication to be characterized by phytoplankton blooms. Using Sr and C isotopes data from the Upper Cambrian，Saltzman et al. argued that catastrophic ocean overturning produced similar periodic，widespread，anoxic conditions. Such pulses may well explain the pattern of trilobite extinctions that were used to define biomere boundaries by Palmer.Progressive ventilation of the deeper oceans appears to have occurred through the Ordovician and Silurian. Attempts to deduce the pattern of oceanic circulation for intervals throughout these two periods have been made by Wilde and Wilde et al. ，respectively，using the paleogeographic reconstructions of Scotese and McKerrow. The superoligotrophic conditions of these oceans and the warm greenhouse climate state throughout the Early Paleozoic were only interrupted in the Ashgill and early Llandovery ( Late Ordovician—Early Silurian) when a continental glaciation developed across North Africa that was then located near the southern pole. The onset of aggressive thermohaline circulation both chilled and ventilated the deep ocean with several glacial phases occurring over about a 10 Ma interval，but with the main Hirnantian phase perhaps lasting only for a few hundred thousand years. The cause of this short-lived icehouse state within such a long 200 Ma period of greenhouse conditions is still speculative and some authors have related it to the passage of part of Gondwana over the south polar region or to the brief drawdown of atmospheric CO2. Even as greenhouse states prevailed through much of the Silurian，detailed analysis on conodont microfossil distributions and related microfacies changes have suggested to Jeppsson and Aldridge et al. that the Silurian ocean state and associated climate was characterized by alternating primo and secundo states with periodic，but rapid turnover intervals. The principal differences being a warm humid phase vs. a drier cooler phase that resulted in significantly different lithologies and reef tracts across the low latitude carbonate platforms. Fig. 1 Indices of ancient nutrient fluxes and productivity through the last 650 MaAnother seemingly important factor in paleoceanography is the changing pattern of eustasy. Sensitive records are preserved on the carbonate platforms and examination of several cratons allows a global pattern to emerge for the Ordovician and Silurian. Major transgressions produced as epicontinental seas that generated important sites of warm，dense hypersaline waters and the periodic development and then closure of this system with transgressive and then regressive events has not yet been fully accommodated into paleoceanographic models. Such oscillations certainly produced major global bio-events. For the Late Ordovician，the Caradoc transgression was the largest of the Phanerozoic and may have been generated by much higher rates of sea-floor spreading and / or the occurrence of a mantle superplume.There is a marked contrast in the studies of paleoceanography of the Early Paleozoic with those of the Mesozoic and Cenozoic as noted initially. The application of a wide range of isotope proxy data with DSDP and ODP core samples and detailed analysis of abundant cores and outcrop studies in well preserved sedimentary basins，such as the Western Interior Seaway of North America，have allowed increasingly sophisticated interpretations of paleoceanography. Periods of anoxia，of less than 1 Ma duration have been recognized in all major oceans for the Late Barremian to Late Aptian of the Early Cretaceous. Peak oxygen deficiency corresponded to highly eutrophic conditions whereas less intense dysoxic / anoxic intervals were characteristic of oligotrophic conditions. The Albian and part of the Cenomanian were the warmest parts of the Cretaceous at a time when there appears to have been four times the present atmospheric level of CO2. Some authors have argued that ready transfer of heat from the equator to the polar regions reduced the latitudinal gradient and fostered a warm green-house state. Larson advocated the presence of a mid-Cretaceous mantle superplume in the western Pacific that produced the Ontong Java Plateau and this model was elaborated upon by Caldeira and Rampino to explain the widespread black shales，high organic productivity and oil accumulation ( Fig. 2) . Even within the Cretaceous there are considerable changes in oceanic temperature gradients. Huber et al. showed that during the Coniacian—Santonian the difference between low and high latitude surface- water paleotemperatures was in the range of 0—4℃ . As cooling increased towards the end of the period，the temperature difference increased to about 14℃ . Detailed investigations of the Cretaceous biotas have revealed complex patterns of marine biogeography that primarily mirror the changing major water masses and current systems along with the modifications to the Tethys Seaway and the Western Interior Seaway of North America. The open equatorial circulation around much of the globe via the Tethyan Seaway and the presence of wide shallow shelves on which warm saline waters were generated seem to be critical components to maintain the ultra warm greenhouse state at this time.Fig. 2 Inferred mid-Cretaceous mantle superplume showing increased ocean crust generation， sea level，black shales and related increases in ocean temperature and oil generation. These changes correspond to an interval free of magnetic reversals.In addition to the Cretaceous deep oceans，particularly Tethys，Pacific and opening Atlantic， large shelf seas developed as in Europe and the Western. Interior Sea of North America. The latter has received considerable attention because of the large stratigraphic database developed through oil exploration. In the Western Canada Sedimentary Basin，over 150，000 wells have been drilled in Alberta alone，with many aimed at the Cretaceous or passing to Devonian targets. The Cretaceous Seaway initially spread north from the Gulf of Mexico and south from the Beaufort Sea， meeting in Albian time. The sea was constrained on the west by emerging tectonic forelands tied to major Cordilleran orogenic phases and terrane accretion on the Pacific margin; on the east it lapped progressively eastwards on a largely peneplained Canadian Shield. Tectonic deformation generated an asymmetrically subsiding foreland basin and an eastward migrating peripheral bulge. From sedimentological and paleontological studies the seaway is estimated to have been up to 1000 m deep in the west-central corridor. The western margin was subjected to much clastic fill from the deforming foreland，transported by complex river systems. Volcanoes contributed extensive， eastwardly transported ash falls with over 200 bentonites in the Cretaceous sequence，which，with detailed biostratigraphy，have provided a remarkably detailed chemostratigraphy to unravel the changes to the seaway through time.Within this overall framework，there have been several recent attempts to understand and model the paleoceanography of this north-south seaway. Kaufmann initially tried to discriminate the inflowing north and south waters from surface freshwater caps derived from rivers mainly flowing from the emerging Cordilleran foreland. More recent attempts have modelled current flows within the sea-way. Jewell noted that salinity stratification in the seaway could have been established rapidly. Slingerland et al. proposed that river flux was important and likely controlled the strong counterclockwise gyre occupying the entire north-south extent of the seaway.In the Cenozoic，an early phase of global warming ( Paleocene—Eocene) was followed by a progressive but variable decline in mean annual temperature ( Oligocene—Recent) . The onset of glaciation occurred first in Antarctica close to the Eocene—Oligocene boundary ( ca. 34 Ma) . Major Arctic glaciation appears to have been initiated in the late Pliocene ( ca. 2. 8 Ma) . The Cenozoic provides an opportunity to investigate the processes of changeover from a greenhouse to icehouse state. Fundamental questions remain unresolved about the initiation and maintenance of these two states and of the complex feedback loops in the climate system. Of particular interest are the processes of heat transfer to the high latitudes during a greenhouse state and their collapse during the icehouse state. Two possible principal causes have been advanced， possibly interrelated. Firstly，decreased atmospheric CO2partly derived from the weathering of uplifted crustal rocks during the late phases of alpine orogeny ( e. g. ， Himalayan， Alps， Andes， Cordillera) . Secondly，there was substantially altered ocean circulation，particularly the onset of the deep ocean conveyor belt with thermohaline circulation derived from sinking of cold water in the North Atlantic. In this latter case，the pattern of ocean circulation is strongly affected by paleogeographic barriers such as the opening of the Drake Passage or closing of the Panama Isthmus.For the early Cenozoic greenhouse state，O"Connell et al. modelled atmospheric circulation conditions. In one experiment，they showed that under extreme zonal conditions evaporation may have substantially exceeded precipitation leading to the generation of very saline water. Zachos et al. discussed early Cenozoic temperatures from the oceanographic view，and Hovan and Rea used ODP data to examine the particular changes at the Paleocene / Eocene boundary. Here，they noted the dramatic changes that occur over a period of about 1. 2 Ma including: extinction of some benthic foraminifera and changes in calcareous plankton assemblages，oceanic warming，decrease in carbon isotope ratios，reduction in wind strength，an increase in hydrothermal activity. This same change is found in the continental record and is marked by the first appearance of several important modern mammalian orders. The Paleocene and early Eocene climates were controlled primarily by large scale meridional energy transport through the oceans rather than the atmosphere and in part influenced by tectonic events. Hovan and Rea showed that a strong reduction in Paleocene / Eocene wind stress occurs in both hemispheres at the boundary，related to decreased latitudinal thermal gradients produced by a more effective poleward heat transport via the deep ocean.There were dramatic changes to these greenhouse conditions at the Eocene / Oligocene boundary，including: fall in oceanic bottom water temperatures; 1 km drop in the calcium compensation depth in the Pacific; increase in deep sea unconformities; extinctions of planktonic foraminifera. These were apparently related to sudden high latitude cooling and enhanced oceanic thermohaline circulation. The onset of Antarctic glaciation occurred at about 34. 5 Ma seemingly closely related to the opening of the Drake Passage ( between South America and Antarctica) : surface and intermediate water circulation is documented by paleontology at this time，with other geologic evidence suggesting complete opening and deepwater circulation by about 30 Ma. These circulation changes induced a new position for the polar front and strongly influenced the pattern of upwelling and productivity.The late Neogene marks the onset of Arctic glaciation and enhanced global cooling. A significant oceanographic circulation event during this time was the full closure，evaporation and then reflooding of the Mediterranean Sea; the Messinian Event ( ca. 8—5 Ma ) in the late Miocene. The more recent work based on defined sequence stratigraphy and chronostratigraphy has shown that there were two distinct phases of evaporite accumulation，each associated with a sea-level drop that were in turn likely to be of glacio-eustatic origin. Salt a