ライフサイエンスコーパス: ocean

1 ical ocean and winter mixing in the Southern Ocean.

2 ssolved organic matter (DOM) exported to the ocean.

3 ons (RCP8.5 scenario) for the North Atlantic Ocean.

4 from across the Pacific and in the Southern Ocean.

5 a is a French territory in the South Pacific Ocean.

6 y factor in genetic adaptation in a changing ocean.

7 dizers to explain nitrification rates in the ocean.

8 s French territory in the northwest Atlantic Ocean.

9 recalcitrant and may sequester carbon in the ocean.

10 orts numerous ecosystem services in the deep ocean.

11 oorly understood, especially in the Southern Ocean.

12 ent drag at the bottom of the atmosphere and ocean.

13 metabolism, physiology and evolution in the ocean.

14 h as the Faroe Islands in the North Atlantic Ocean.

15 ge and growing anomaly in the South Atlantic Ocean.

16 understanding of how to obtain a sustainable ocean.

17 curred to maintain "just enough" iron in the ocean.

18 feed at ~500-m depth in the central Pacific Ocean.

19 the exchange of water mass between land and ocean.

20 nal and international waters of the Southern Ocean.

21 e temperature profiles in the atmosphere and ocean.

22 fixed nitrogen and carbon production in the ocean.

23 nistic understanding of redox cycling in the ocean.

24 h are U.S. National Monuments in the Pacific Ocean.

25 may not be sufficient to adapt to a changing ocean.

26 the internal iron and sulfur cycling of the ocean.

27 ant determinant of the fate of sulfur in the ocean.

28 rias and squids in the eastern North Pacific Ocean.

29 lastic particle concentration in the surface ocean.

30 e the most abundant primary producers in the ocean.

31 connections we currently see in the Southern Ocean.

32 ssroads between the Arctic and North Pacific Oceans.

33 ly transported to the deepest reaches of the oceans.

34 rtant ecological and biogeochemical roles in oceans.

35 cluding from air, soil, fresh water, and the oceans.

36 contributed by northern land ecosystems and oceans.

37 ata are thus urgently needed for the world's oceans.

38 ibution of the lipid desaturase genes in the oceans.

39 issions are projected to lower the pH of the ocean 0.3 units by 2100.

40 t severely in nations surrounding the Indian Ocean(1-4).

41 liquid at the conditions of the basal magma ocean: 100-140 GPa, and 4000-6000 K.

42 all the observed NPF events from the Arctic Ocean 2018 expedition are driven by iodic acid with litt

43 enically produced trace gas emitted from the ocean, accounts for a large fraction of natural sulfur r

44 n for assessing and predicting the impact of ocean acidification (OA) on marine ecosystems.

45 Ocean acidification (OA) poses a major threat to marine

46 Ocean acidification (OA), a consequence of anthropogenic

47 Here we show that ocean acidification and warming, alone and in combinatio

48 assess how species may survive under future ocean acidification conditions, and help to reveal the t

49 energetic demands of pinto abalone caused by ocean acidification during winter will be exacerbated by

50 egarded as an imminent threat to our oceans, ocean acidification has been documented in all oceanic b

51 of CaCO(3) biominerals but their response to ocean acidification is poorly understood.

52 s (e.g., sediment, low salinity, anoxia, and ocean acidification), offering an alternative approach f

53 ting gradients of temperature, salinity, and ocean acidification, then model growth rate and duration

54 table global change, particularly increasing ocean acidification.

55 ors such as light exposure, temperature, and ocean acidification.

56 Here, we review the work of Tara Oceans, an international, multidisciplinary project to a

57 pelagiphages are globally distributed in the ocean and can be detected throughout the water column.

58 mportant warming impact on the extratropical ocean and climate.

59 PE packaging were collected in the Atlantic Ocean and compared to new PE boxes.

60 of sinking organic carbon out of the surface ocean and its drivers remains poorly understood, especia

61 neighbours by hundreds of kilometres of deep ocean and the Antarctic Circumpolar Current.

62 rm studies of pelagic nekton in the Southern Ocean and their responses to ongoing environmental chang

63 traced to seasonal upwelling in the tropical ocean and winter mixing in the Southern Ocean.

64 icate increasing deoxygenation in the global oceans and an elevated frequency and intensity of hypoxi

65 lus clouds cover large swaths of subtropical oceans and cool Earth by reflecting incident sunlight, t

66 nutrient for phytoplankton in major areas of oceans and deposited wind-blown desert dust is a primary

67 ange the planet including the composition of oceans and the atmosphere and thus the climate, the micr

68 e were travelling to Asia, swimming in a sea/ocean, and not changing the kitchen towel daily.

69 opogenic impacts to the planet's climate and oceans, and informed the creation of fully protected dee

70 rcing likely contributed to the expansion of ocean anoxia and other environmental perturbations assoc

71 nvironmental changes associated with the two ocean anoxia pulses.

72 astal (- 0.03 +/- 1.83 mol C m(-2) year(-1)) ocean are approximately neutral in terms of an annual so

73 iable laminarin concentrations in the sunlit ocean are driven by light availability.

74 The islands of the Western Indian Ocean are identified as a major biodiversity hotspot, wi

75 Estimates of plastic inputs into the ocean are orders of magnitude larger than what is found

76 Up to 80% of the plastics in the oceans are believed to have been transferred from river

77 Oceans are the ultimate sink for many of the over 100 mi

78 offering a pathway to strategically conserve ocean areas while securing seafood for the future.

79 Our results highlight the role of the ocean as a net atmospheric Se sink, with around 7 Gg yr(

80 ing of plankton diversity and ecology in the ocean as a planetary, interconnected ecosystem.

81 gical productivity in the Subarctic Atlantic Ocean as increasing ocean surface buoyancy suppresses tw

82 ce of freshwater and nutrients to the Arctic Ocean as permafrost thaws, yet few studies have quantifi

83 ble quantities of PM(1) eventually enter the oceans as suspended particulates, yet subsequent removal

84 y geobiological processes of the atmosphere, ocean, as well as land.

85 Here we calculate a time history of ocean-atmosphere CO(2) fluxes from 1992 to 2018, correct

86 m too-weak NDH and too-weak linear dynamical ocean-atmosphere coupling.

87 These oscillations resulted from complex ocean-atmosphere interactions in the Nordic seas, caused

88 the emplacement of CAMP using the long-term ocean-atmosphere-sediment carbon cycle reservoir (LOSCAR

89 We use an idealized coupled ocean-atmosphere-wave numerical model to analyze tropica

90 Ocean-atmospheric dynamical processes influence the wave

91 the catalyst for societal shifts in MSEA via ocean-atmospheric teleconnections.

92 alia (F(ST) = 0.377), identifying the Indian Ocean basin as a barrier to dispersal.

93 major conduits of microplastics to lake and ocean basins.

94 e primary influence and the tropical Pacific Ocean being the most dominating larger-scale climate sti

95 pa almost certainly hides a global saltwater ocean beneath its icy surface.

96 les use a true navigation system in the open ocean, but their map sense is coarse scale.

97 and generates sulfate that is carried to the ocean by rivers.

98 ical [Formula: see text]O emissions from the ocean by training a supervised learning algorithm with o

99 the algae and is a critical parameter in the ocean carbon cycle.

100 y used to estimate large-scale variations in ocean carbon export, but the relationship between export

101 ese experiments provide evidence that global ocean change can affect the resilience of corals to envi

102 Changing ocean chemistries will alter the iron bioavailability wh

103 results show future implications of changing ocean chemistry as well as of the resulting abilities of

104 with a large spread in their projections of ocean circulation and ocean heat uptake(8,11).

105 Changes in ocean circulation and the biological carbon pump have be

106 Additionally, assessing the influence of ocean circulation changes (specifically, the redistribut

107 a model of adaptation and an eddy-resolving ocean circulation climate model.

108 volcanic eruptions or multidecadal cycles in ocean circulation occur infrequently and are therefore p

109 and mixing of water masses within the global ocean circulation system.

110 Increased ocean CO(2) can enhance seagrass productivity and therma

111 estimates of this flux, derived from surface ocean CO(2) concentrations, have not corrected the data

112 Using an ocean color algorithm parameterized for the Arctic Ocean

113 ies suggest that acclimatization to changing ocean conditions may vary, even among related species th

114 ral skeletons as mainly passive recorders of ocean conditions, it has become increasingly clear that

115 , leading to winners and losers under future ocean conditions.

116 us species was indirect and related to river-ocean connectivity.

117 ess anthropogenic disturbance than any other ocean continental shelf environment.

118 A network to protect an additional 5% of the ocean could increase future catch by at least 20% via sp

119 one, through a feedback involving decreasing ocean coverage and increased dust loading.

120 lying chemosynthetic activity within igneous ocean crust.

121 n (including atmosphere loss to space, magma ocean crystallization, and volcanic outgassing).

122 During early magma ocean crystallization, high-molecular-weight species usu

123 Despite much stronger horizontal ocean currents, vertical swimming of simulated larvae ca

124 pe (delta(13)C) megasplice, documenting deep-ocean delta(13)C evolution since 35 million years ago (M

125 energetic Snowball ocean due to the reduced ocean depth, the supercontinent palaeogeography predicts

126 The Indian Ocean Dipole (IOD) affects climate and rainfall across t

127 ciated with the positive phase of the Indian Ocean Dipole, although the positive PMM phase and El Nin

128 The removal mechanism of refractory deep-ocean dissolved organic carbon (deep-DOC) is poorly unde

129 6 degrees S) and western equatorial Atlantic Ocean Drilling Project Site 929 (paleolatitude ~0 degree

130 sheets predicts a tidally energetic Snowball ocean due to the reduced ocean depth, the supercontinent

131 Because Southern Ocean dynamics are influenced by the Southern Hemisphere

132 different ocean uses to optimize the overall ocean economy.

133 Southern Ocean ecosystems are under pressure from resource exploi

134 a host of ecological parameters in Southern Ocean ecosystems.

135 obula mobular species in the eastern Pacific Ocean (EPO).

136 The Southern Ocean exerts a major influence on the mass balance of th

137 Expedition (1872-1876) with the recent Tara Oceans expedition material (2009-2016).

138 metagenomic analysis of stations of the Tara Oceans expedition to describe the latitudinal distributi

139 findings reveal that in the glacial Southern Ocean, Fe fertilization critically relies on the dynamic

140 odesmium growth onto inferred global surface ocean fields of pCO(2) , temperature, light and Fe.

141 ay have composed ~10% of the Mesoproterozoic ocean focused along continental margins.

142 ry means of sensing and communication in the ocean for humans and many marine animals.

143 ummer towards autumn, possibly linked to the ocean freeze-up and a seasonal rise in ozone.

144 tic pollution in Antarctica and the Southern Ocean has been recorded in scientific literature since t

145 sources and sinks of molecular oxygen in the oceans has greatly impacted the composition of Earth's a

146 The environmental conditions in the ocean have long been considered relatively more stable t

147 Studies of warming events in the ocean have typically focused on the events' maximum temp

148 escales are steric changes due to changes in ocean heat content and barystatic changes due to the exc

149 n their projections of ocean circulation and ocean heat uptake(8,11).

150 a-level change from thermal expansion of the ocean, ice-mass loss and changes in terrestrial water st

151 wever, as our methods for exploring the deep ocean improve, common assumptions about dispersal, repro

152 ip between the heat and carbon uptake of the ocean in response to anthropogenic emissions.

153 he efficiency of iron retention in the upper ocean in the eastern equatorial Pacific across different

154 s been reported in many regions of the world oceans in the past decade.

155 limited by iron (Fe) in ~40% of the world's oceans including high-nutrient low-chlorophyll (HNLC) re

156 and clear evidence of plastics loss into the oceans, including a substantial standing stock, previous

157 e developed a novel, server-based tool (ICBM-OCEAN, Institute for Chemistry and Biology of the Marine

158 C (particulate organic carbon) flux into the ocean interior at a fixed reference depth.

159 However, here we show that the ocean interior conceals high loads of small-sized plasti

160 rbon supply, consumption, and storage in the oceans' interior.

161 radient in oxygen fugacity with deeper magma oceans invoking more oxidizing surface conditions.

162 chemically feasible molecular mechanism from ocean iodine emissions to atmospheric particles that is

163 Emitted from the oceans, iodine-bearing molecules are ubiquitous in the a

164 oncentration threshold that buffers the deep ocean iron inventory.

165 The Southern Ocean is a key region for the overturning and mixing of

166 The ocean is a sink for ~25% of the atmospheric CO(2) emitte

167 ed ligand source/sink ratios where the model ocean is driven to global-scale colimitation by micronut

168 The mean state of the atmosphere and ocean is set through a balance between external forcing

169 wind strength over the south tropical Indian Ocean is the main driver of year-to-year variability.

170 predicts weak tides because the surrounding ocean is too large to host tidal resonances.

171 Anthropogenic Hg added to the surface ocean is, therefore, expected to be rapidly transported

172 Rare high-(3)He/(4)He signatures in ocean island basalts (OIB) erupted at volcanic hotspots

173 Long-lived ocean island volcanoes are crosscut by thousands of dyke

174 nd evolutionarily relevant timescales in the ocean, leading to a growing recognition of the dynamism

175 ratification of the upper equatorial Pacific Ocean, leading to a smaller increase in ENSO variability

176 ng with warmer northern Pacific and Atlantic oceans, leading mostly to global supply shortages.

177 ction with the development of (at least) two ocean levels.

178 iplinary project to assess the complexity of ocean life across comprehensive taxonomic and spatial sc

179 ssing during the final stages of lunar magma ocean (LMO) or later melt crystallization.

180 onged high-temperature extreme events in the ocean, marine heatwaves, can have severe and long-lastin

181 50% of the Mesoproterozoic ocean may have been suboxic, promoting nitrification and

182 Fe, Ti) far exceed global riverine and open ocean mean values and highlight the importance of subgla

183 tarctic outlet glaciers (dynamic response to ocean melting) was partially compensated by mass gains o

184 face melt), Antarctic ice shelves (increased ocean melting), and Greenland and Antarctic outlet glaci

185 for setting the horizontal structure of the ocean mixed layer.

186 correlation between eastern tropical Pacific Ocean mixed-layer thickness and both El Nino amplitude a

187 es evaporative cooling and wind-driven upper ocean mixing.

188 bservational platforms and an eddy-resolving ocean model to identify an unrecognized deep flow toward

189 We modify an ocean model to simulate submarine iceberg melting in Ser

190 ded within the currents of a high-resolution ocean model.

191 While Ocean modeling has made significant advances over the la

192 eveloped a 2D implementation of the Regional Ocean Modeling System (ROMS) to downscale global climate

193 rophytes, organisms particularly abundant in ocean N(2)O-producing hot spots.

194 oproterozoic and ~40% of the Mesoproterozoic ocean, nitrogen cycling dominated.

195 ing past inter-annual variations in regional ocean NPP, largely due to limited change in the historic

196 Widely regarded as an imminent threat to our oceans, ocean acidification has been documented in all o

197 the microscope, and you will likely find an ocean of extraordinary and diverse single-celled organis

198 That pipefishes survive in an ocean of microbes without one arm of the adaptive immune

199 h thermodynamic modeling, we show that magma oceans of Earth, Mars, and the Moon are likely character

200 techniques to uncover new insights from the "ocean" of known bioactive peptides.

201 altered delivery of iron and sulfate to the ocean, or major shifts in marine productivity.

202 unities, such as those found in animal guts, oceans, or soils, it is still unclear whether there are

203 icular locations by marine habitat features, ocean physical processes, and invertebrate bioconcentrat

204 Nano CT-scans of selected equatorial Pacific Ocean planktonic foraminifera, have revealed that all mo

205 cessary to model the degradation behavior of ocean plastics or understand if degradation is possible?

206 iotic era, radiolytic transformations in the oceans played a key role in purifying water from toxic i

207 y in the water column of the Canadian Arctic Ocean points to the need for international regulatory me

208 erial dsyB mutants are less tolerant of deep ocean pressures than wild-type strains.

209 ound state, local and remote drivers and the ocean productivity response from past events are critica

210 an increase of P input would elevate surface ocean productivity, which in turn enhances marine iron r

211 llation, triggering processes and impacts on ocean productivity.

212 h), the export of nutrients from the surface ocean provides a crucial but seasonally variable energy

213 ively anoxic and showed occasional shifts in ocean redox chemistry between iron-buffered and sulfide-

214 erns of fragile gelatinous fauna in the open ocean remain scarcely documented.

215 how much methane is being released into the ocean remains a major challenge and a critical gap in as

216 owledge of how ammonia oxidation (AO) in the ocean responds to warming is crucial to predicting futur

217 ing an offshore branch in the western Indian Ocean, resulting in remobilization of sediment in the fo

218 Xe isotopes in Yellowstone compared with mid-ocean ridge basalt (MORB) samples, this confirms that th

219 the displacement process of the Pacific mid-ocean ridge basalt (MORB)-type mantle by the Indian MORB

220 old subsurface sediments from the Arctic Mid-Ocean Ridge.

221 es for the convective mantle provided by mid-ocean-ridge basalts(11), consistent with subducted nitro

222 -temperature hydrothermal circulation at mid-ocean ridges.

223 Furthermore, our results imply that such ocean rose in elevation (ca. 1000 m) between ca. 3.6 Ga

224 xchange was somehow weakened in the Southern Ocean's Antarctic Zone, which reduced the leakage of dee

225 Our findings highlight the South Indian Ocean's capacity to influence atmospheric CO(2) levels a

226 1) further obstruct our understanding of the ocean's influence on weather and climate.

227 For most of Earth's history, the ocean's interior was pervasively anoxic and showed occas

228 picture of the last 120 My of change in the ocean's largest oxidant reservoir.

229 with less river runoff, rainfall and higher ocean salinities.

230 We used the same chronology to synchronize ocean sediments from the North Atlantic to correlate maj

231 Ocean Sentinel was also able to provide unpreceded infor

232 nian, and highlight that simulations of past oceans should include explicit tidally driven mixing pro

233 exceed the estimated plastic inputs into the ocean since 1950.

234 Comparison to a distant eastern Indian Ocean site (Western Australia, n = 15) revealed strong g

235 dapt to existing pressures and shift towards ocean stewardship through incorporation of niche innovat

236 rococcus isolate from the equatorial Pacific Ocean (strain MIT9215) through a series of growth experi

237 Absolute geostrophic current at the ocean surface (S) contains three components: (1) absolut

238 n the Subarctic Atlantic Ocean as increasing ocean surface buoyancy suppresses two physical drivers o

239 We produce estimates of ocean surface chlorophyll trends, by using Coupled Model

240 Search and detection of objects on the ocean surface is a challenging task due to the complexit

241 meters depth, or for the effect of the cool ocean surface skin.

242 tion of Ekman pumping due to reduced sea ice-ocean surface stress.

243 irectly related to latitudinal variations in ocean surface temperature.

244 tainties of the drifting search areas on the ocean surface.

245 cal fluxes, and deposition velocities to the ocean surface.

246 In particular, modeling organisms in the ocean system must integrate parameters to fit both physi

247 roduce a method that infers basin-scale deep-ocean temperature changes from the travel times of sound

248 sea-surface temperature thresholds or inter-ocean temperature gradients.

249 Ocean temperature was identified as a likely driver of p

250 are shaped by more nuanced Fe niches in the oceans than previously implied from mostly binary compar

251 This suggests a future Arctic Ocean that can support higher trophic-level production a

252 pes in diatoms and sponges from the Southern Ocean that together show increased Si supply from deep m

253 e major subtropical WBC of the South Pacific Ocean, the East Australian Current (EAC), transports mic

254 ght levels-a pervasive condition in the deep ocean, the largest inhabitable space on the planet.

255 In the open Southern Ocean, the spring bloom magnitude is found to be greates

256 la: see text]O measurements from the surface ocean-the largest synthesis to date.

257 A first implementation of this seismic ocean thermometry constrains temperature anomalies avera

258 face 0.02-0.2 mum samples from the San Pedro Ocean Time-series(3) that were sampled monthly over 5 ye

259 carbon cycle changes would have allowed the ocean to absorb massive amounts of carbon dioxide, thus

260 rage theoretical sensitivity of the Southern Ocean to potential changes in seasonal nutrient and ligh

261 ydas) migrating long distances in the Indian Ocean to small oceanic islands.

262 y a shift in moisture source from the Indian Ocean to the South China Sea.

263 land (Mascarene Islands, southwestern Indian Ocean), to determine any potential unique characters.

264 shear due to horizontal gradient of dynamic ocean topography) was found by the statistical character

265 and N) due to horizontal gradient of dynamic ocean topography, and (3) geostrophic shear (between S a

266 ertainties in soil weathering rates and land-ocean transfer of weathered products.

267 pressures equivalent to those in the deepest ocean trenches.

268 ms while integrating and balancing different ocean uses to optimize the overall ocean economy.

269 ntic overturning conditions favoured abyssal ocean ventilation at the YD and marked an interval of Si

270 , single-virus vSAG 37-F6 and several Global Ocean Viromes (GOV) viral populations, are now further c

271 We investigated how predicted ocean warming (OW) and acidification (OA) affect key eco

272 effect would gradually vanish as the Indian Ocean warming acts to strengthen the Atlantic meridional

273 er the past decade, the number of reports of ocean warming impacts on kelp forests has risen sharply.

274 the strong links with temperature, continued ocean warming in the northeast Atlantic may reduce prima

275 Ocean warming is causing the symbioses between cnidarian

276 ction) on patterns of observed and simulated ocean warming remains a challenge.

277 Monitoring the resulting ocean warming remains a challenging sampling problem.

278 , July 2007-April 2013, a time of both rapid ocean warming throughout the Gulf of Maine and apparent

279 nisms [2], it may therefore be expected that ocean warming would lead to abundance increases at polew

280 to abandon their traditional habitats due to ocean warming, and consequently either migrate further N

281 ecline in fish production with anthropogenic ocean warming, but how fish production equilibrates to w

282 Anthropogenic upper-ocean warming, increased dissolved carbon dioxide, and a

283 accurately capture the observed patterns of ocean warming, with a large spread in their projections

284 expected on Red Sea coral reefs with future ocean warming.

285 acteria to assess the retention time of deep-ocean water by a seamount.

286 concentrations of aerosol components across ocean waters next to the Antarctic Peninsula, South Orkn

287 results support the hypothesis that warming ocean waters will restrict the habitat range of the narw

288 and retreating where ice is exposed to warm ocean waters.

289 color algorithm parameterized for the Arctic Ocean, we show that primary production increased by 57%

290 ith the particulate organic carbon export to oceans, we demonstrated that a large fraction of the car

291 We also found that the area of the ocean where sea surface temperatures (SST) are within Tr

292 We relied on a major published dataset (Tara Oceans) where samples from the mesopelagic zone were ava

293 y restructuring is especially evident in the ocean, whereas climatic debt may be accumulating on land

294 ertainly affect terrestrial P input into the ocean, which in turn might have impacted the marine prim

295 r-long section in the equatorial East Indian Ocean with a standard error of 0.0060 kelvin.

296 stal ecosystems are rich areas of the global ocean with elevated rates of organic matter production s

297 on of serpentinites is a source of Si to the ocean with extremely high fluid delta(30)Si values, whic

298 ian hydrosphere capable of supporting a vast ocean, with an active hydrological cycle stretching into

299 ound in the temperate western North Atlantic Ocean, with limited information existing on the distribu

300 repeated today, such rapid mass loss to the ocean would have clear implications for increasing the r