ライフサイエンスコーパス: ocean

1 fluencing its success throughout much of the ocean.

2 n and thus enhance its export to the coastal ocean.

3 r skillful climate prediction resides in the ocean.

4 the central role of heterotrophy in the dark ocean.

5 ng lack of reproductive isolation across the ocean.

6 ss the global challenges associated with the ocean.

7 od webs and the flux of carbon into the deep ocean.

8 webs and carbon sequestration in the Arctic Ocean.

9 ntinent, which is surrounded by the Southern Ocean.

10 ges N2 fixation, the dominant N input to the ocean.

11 ousands of kilometres before re-entering the ocean.

12 nsport of mass, heat, and salt in the global ocean.

13 survival strategies for phytoplankton in the ocean.

14 bserved at intermediate depths in the global ocean.

15 he essential role of long time series in the ocean.

16 photolabile DOS formulas not present in the ocean.

17 carbon to higher trophic levels and the deep ocean.

18 ing of carbon between the atmosphere and the ocean.

19 ation in coastal waters compared to the open ocean.

20 underestimate the abundance of SAR11 in the ocean.

21 populations from both sides of the Atlantic Ocean.

22 cial Maximum could have reached the Southern Ocean.

23 filling previously unassigned niches in the ocean.

24 decade in advance based on the state of the ocean.

25 denitrification pathway in the open Atlantic Ocean.

26 tain community structure and function in the ocean.

27 metabolic precursor to methane in the upper ocean.

28 OM) and microbial communities in the surface ocean.

29 y tracer plume through the northeast Pacific Ocean.

30 wood falls in the deep ( 1600 m) NE Pacific Ocean.

31 ay affect Synechococcus distributions in the ocean.

32 y production in the tropical and subtropical ocean.

33 arine ecosystem change develop in the future ocean.

34 rding the oil's fate and effects in the deep ocean.

35 to pelagic ecosystems in the North Atlantic Ocean.

36 sses of iceberg degradation towards the open ocean.

37 across the continental margins of the Arctic Ocean.

38 edators, particularly for fishes of the deep ocean.

39 with active hydrologic cycling involving an ocean.

40 Fin whales) feed in the Arctic and Southern Oceans.

41 by internal variability within the tropical oceans.

42 present in the tropical Indian and Atlantic Oceans.

43 r represent over 50% of the cells in surface oceans.

44 t the dsDNA viral populations dominating the oceans.

45 ea-air exchange and are transported over the oceans.

46 an floor of the Pacific, Atlantic and Indian Oceans.

47 divergence; (1) the opening of the Atlantic Ocean, (2) the breakup of Gondwana, and (3) the closure

48 along a latitudinal transect in the Atlantic Ocean (31 degrees N to 38 degrees S).

49 In the upper ocean, a Pb concentration maxima (64-113 pmol kg(-1)) ex

50 Saturn's moon Enceladus has an ice-covered ocean; a plume of material erupts from cracks in the ice

51 The near-term progression of ocean acidification (OA) is projected to bring about sha

52 r acclimatization or adaptation of corals to ocean acidification and even less about the molecular me

53 Climate change and ocean acidification are altering marine ecosystems and,

54 ications of transgenerational acclimation to ocean acidification during experiments.

55 cting the responses of macroalgal species to ocean acidification is complex, but we demonstrate that

56 Ocean acidification may have far-reaching consequences f

57 We conclude that the effect of ocean acidification on algae (primary producers) can hav

58 ll be a key driver of ecosystem change under ocean acidification.

59 h as a result of increasing temperatures and ocean acidification.

60 ges resulting from global climate change and ocean acidification.

61 Our findings suggest that the Atlantic Ocean acts as a key pacemaker for the western Pacific de

62 terrestrial microbes.The extent to which the ocean acts as a sink and source of airborne particles to

63 e LGT our findings demonstrate that Southern Ocean-AIS feedbacks were controlled by global atmospheri

64 wo song revolutions across the South Pacific Ocean, allowing fine-scale analysis of composition and s

65 atures of water-rock interaction between the ocean and a rocky core.

66 ttern from the Indian landmass to the Indian Ocean and an east-west pattern from the Core Monsoon Zon

67 ylamine N-oxide (TMAO) are widespread in the ocean and are important nitrogen source for bacteria.

68 ia are ubiquitous in oil-rich regions of the ocean and are known for their ability to degrade polycyc

69 This invariant demonstrates that ocean and atmospheric waves share fundamental properties

70 l be reflected in the water contained in the ocean and can manifest as global sea level variations.

71 eruption drove strong responses in both the ocean and cryosphere that were fundamental to driving th

72 the vocal behaviour of penguins in the open ocean and discuss the function of their vocal communicat

73 es of selection on these lineages in today's ocean and have postulated selection as the primary force

74 d from geographic distance across the global ocean and instead, correlated significantly with water t

75 n of anthropogenic atmospheric N on the open ocean and its incorporation into plankton and, in turn,

76 soscale eddies are present everywhere in the ocean and partly determine the mean state of the circula

77 kground of natural variability in 55% of the ocean and propagate rapidly to encompass 86% of the ocea

78 proximately 90% of that of the modern global ocean and relative amplitude varied by approximately 20-

79 Future ocean and sea-ice changes affecting the distribution of

80 Today's Arctic Ocean and surrounding regions are undergoing climatic ch

81 margins mark a transition from continents to oceans and contain in their architecture a record of the

82 a are widespread in subeuphotic areas of the oceans and particularly abundant in oxygen minimum zones

83 er the tropical Atlantic, Pacific and Indian oceans and propose islands as stepping stones for the tr

84 variable, depending on surface type (land or ocean) and surrounding continental configuration.

85 the Mediterranean Sea compared to the global ocean, and demonstrates the essential role of long time

86 the most biologically dynamic regions of the ocean, and they are extensive worldwide, especially in t

87 rian, and were even a feature of Phanerozoic ocean anoxic events.

88 environmental upheaval, like the Cretaceous Ocean-Anoxic-Event-2 (OAE-2).

89 The world's oceans are home to many fantastic creatures, including a

90 ypothesized to decrease in many areas of the ocean as a result of anthropogenically driven climate ch

91 average residence time of carbon in the deep ocean at the LGM.

92 However, a Southern Ocean (Atlantic-sector) iceberg rafted debris event appe

93 Large ocean-atmosphere and hydroclimate changes occurred durin

94 onal predictability results from large-scale ocean-atmosphere interactions.

95 ly and easterly winds is coupled to a simple ocean-atmosphere model that is otherwise deterministic,

96 tently modulated biospheric productivity and ocean-atmosphere oxygen levels over time.

97 Here we use a global array of ocean-atmosphere radiocarbon disequilibrium estimates to

98 lcanism, and associated perturbations in the ocean-atmosphere system, likely had profound implication

99 exchanges over the tropical and subtropical oceans based on the data collected along the Malaspina 2

100 optimal investments to counteract land- and ocean-based stressors: (1) marine restoration should be

101 Subsequent research in the Indian Ocean basin has identified prehistoric tsunamis, but the

102 We use a 60-year ocean basin-wide data set comprising >148,000 samples to

103 ing spatial and behavioral differences on an ocean-basin scale by measuring puffins' among-colony dif

104 ing several enormous igneous plateaus in the ocean basins worldwide.

105 verage is limited in space, as it was in the ocean before the Argo era, these mechanisms may be insuf

106 ries (STEs) are of major importance for land-ocean biogeochemical fluxes.

107 e appeared due to enhanced warming of Arctic Ocean bottom water during the last century.

108 summer when air is mainly arriving from the oceans but low when air is arriving from the continents.

109 (Megalaspis cordyla) over the western Indian Ocean, but also the western Pacific from Japan to Austra

110 en as evidence for the demise of ferruginous oceans, but recent geochemical studies show that ferrugi

111 nd propagate rapidly to encompass 86% of the ocean by 2050 under a 'business-as-usual' scenario.

112 us the observed heaving domination in global oceans cannot mask the extra heat in the ocean during th

113 erived CO2 but is also sensitive to land and ocean carbon cycling and uptake.

114 ion of OMZs is likely to increase biological ocean carbon storage and act as a negative feedback on c

115 r beyond the crest of this ridge, forming an ocean cavity beneath the ice shelf, occurred in 1945 (+/

116 arted and how the supply of nutrients to the oceans changed through time.

117 ses in atmospheric CO2 levels and associated ocean changes are expected to have dramatic impacts on m

118 Washington State in the Northeastern Pacific Ocean, characterized by a species-rich community with lo

119 We propose that the coupling of ocean chemistry and Early Cambrian animal diversificatio

120 st mantle at one location (e.g. under Indian Ocean) circulates down to the core-mantle boundary (CMB)

121 Our results emphasize that the way that ocean circulation affects heat, a dynamic tracer, is con

122 ws that various inferred changes in the deep ocean circulation and stratification between glacial and

123 ciated with major rearrangements in the deep ocean circulation and stratification, which have likely

124 rminates in a rapidly melting ice shelf, and ocean circulation and temperature are implicated in the

125 tion allows improved regional realism of the ocean circulation beyond that of available CMIP5-class m

126 The mechanisms by which the deep ocean circulation changed, however, are still unclear an

127 The large-scale reorganization of deep ocean circulation in the Atlantic involving changes in N

128 use a Lagrangian approach forced by modelled ocean circulation to simulate the circulation pathways t

129 gnetic map, tuned to large-scale features of ocean circulation, facilitates the vast oceanic migratio

130 mpilation of data from the subpolar Atlantic Ocean, clear evidence of a marked pre-bloom silicate dec

131 ep waters to the sea surface in the Southern Ocean closes the global overturning circulation and is f

132 Polar oceans contrast in size, age, isolation, depth, oceanogr

133 consistent with a collapse of the local deep-ocean convection.

134 odels with a database of synthetic storms in Ocean County and estimates a 16% average reduction in an

135 local annual flood losses in Barnegat Bay in Ocean County, New Jersey.

136 ough pH is a fundamental property of Earth's oceans, critical to our understanding of seawater biogeo

137 nding differences between Indian and Pacific Ocean crust.

138 gradient of the Japanese archipelago and its ocean current system.

139 l reef fish larvae is driven by advection in ocean currents and larval swimming.

140 mulations, using pelagic larval duration and ocean currents as proxies, showed a reduced level of con

141 Larval eels are transported by ocean currents associated with the Gulf Stream System fr

142 el is based on settling, biofilm growth, and ocean depth profiles for light, water density, temperatu

143 rient environments, a process referred to as ocean desertification [1].

144 International Ocean Discovery Program Expedition 362 sampled incoming

145 vations to confirm that the tropical Pacific Ocean does play an early and important role in modulatin

146 ered patterns, such as those observed in the ocean due to double-diffusive convection.

147 at breed in North America cross the Atlantic Ocean during autumn migration when travelling to their n

148 bal oceans cannot mask the extra heat in the ocean during the recent "hiatus".

149 onents of climate models without interactive ocean dynamics (i.e., models whose ocean is represented

150 long timescales and exacerbated by shifts in ocean dynamics on shorter timescales.

151 uction in an otherwise iron-limited Southern Ocean Ecosystem.

152 utionarily distinct animals can support both ocean ecosystems and human activities in the future.

153 While amassing data from ocean ecosystems for the Baselines Initiative (6,177 nea

154 croplastics and their devastating effects on ocean ecosystems.

155 s for the use of Adelie penguins in Southern Ocean feedback management, and suggest that aggregating

156 sinks to generate a tropic-ward flow on the ocean floor of the Pacific, Atlantic and Indian Oceans.

157 that the particles either float, sink to the ocean floor, or oscillate vertically, depending on the s

158 me these small particles may never reach the ocean floor.

159 hausia superba) is a key species in Southern Ocean food webs, but there is little understanding of th

160 Our results emphasize the importance of the ocean for ice sheet stability under the current changing

161 rstand the relative roles of contemporaneous ocean-forced change and of ongoing glacier response to a

162 isopycnal mixing experiment in the Southern Ocean found the turbulent diffusivity inferred from the

163 0)Be records, the authors show that Southern Ocean freshwater hosing can trigger global change.

164 on the Juan de Fuca Ridge in the NE Pacific Ocean, from 2013 to 2015 at three different vents: Anemo

165 he southwest Atlantic sector of the Southern Ocean, from net samples and in situ temperature records

166 We demonstrate how recent atmosphere-ocean general circulation model (AOGCM) simulations of t

167 elevant trace gas, and its production in the ocean generally increases under suboxic conditions.

168 al-time measurements of ion-fluxes near deep-ocean geothermal vents.

169 Ocean going vessels (OGVs) operating within emission con

170 chemoautotrophic microorganisms in the dark ocean has a major impact on global carbon cycling and ec

171 surface water distribution across the Arctic Ocean helps to improve our understanding of the large-sc

172 olcano-induced dynamic chemistry of the deep ocean, here we demonstrate the Leidenfrost dynamic chemi

173 (Pb) contamination of the Northwest Pacific Ocean in 2002 and present the first comprehensive Pb iso

174 +/- 5% of the annual N input to the surface ocean in this region, which appears to be at the lower e

175 e Barents and Atlantic sectors of the Arctic Ocean indicate the northbound Atlantic current as a sign

176 Here we present reconstructions of Arctic Ocean intermediate depth water (AIW) temperatures and se

177 South China Sea (SCS-01, SCS-02) and Indian Ocean (IO-01).

178 al has challenged the prevailing view of the ocean iron cycle.

179 ne bacteria and phytoplankton in the surface ocean is a key step in the global carbon cycle, with alm

180 , but one widely distributed species in each ocean is composed of morphotypes previously described as

181 istribution over the central-eastern Pacific Ocean is mainly driven by convective activity related to

182 so regions of striking contrasts: the Arctic Ocean is near surrounded by land compared with the Antar

183 teractive ocean dynamics (i.e., models whose ocean is represented by a 50-m-deep slab ocean mixed lay

184 Overall, the budget of dissolved V in the oceans is remarkably well balanced-with about 40 x 10(9)

185 New tungsten isotope data for modern ocean island basalts (OIB) from Hawaii, Samoa, and Icela

186 e deposits provide invaluable information on ocean island geodynamics they also represent a significa

187 a Markov-chain representation of the surface-ocean Lagrangian dynamics in a region occupied by the Gu

188 decades is significantly smaller than normal ocean-level fluctuations caused by tides, waves, and sto

189 Total ice cover would make an anoxic ocean likely, and would be a formidable barrier to biolo

190 Ocean margin sediments have been considered as important

191 ons in biogeochemical fluxes at and near the ocean margins, with implications for coastal organisms a

192 ests that ice sheets in contact with warming oceans may be vulnerable to catastrophic collapse even w

193 ock data set and then applied it to the Tara Oceans microbiome.

194 ose ocean is represented by a 50-m-deep slab ocean mixed layer with no interactive currents).

195 Using a data assimilative regional ocean model fit to measured conditions, we estimate that

196 Using a high-resolution ocean model, it is shown that the fast vertical spreadin

197 f internal variability in coupled atmosphere-ocean models are remarkably similar to the most predicta

198 In the ocean, most estimates suggesting short-distance dispersa

199 Here we analyze atmosphere and ocean observations and identify evidence that a specific

200 hat were in limited supply compared with the oceans of liquid water.

201 thought to limit primary productivity in the oceans on geological timescales.

202 d as indicator species for the health of the oceans on which they depend.

203 breeze (cold air advection from ice-covered ocean onto adjacent land during the growing season), the

204 Hence, the sensitivity of zooplankton to ocean oxygen concentrations can have direct implications

205 espread nitrate availability associated with ocean oxygenation.

206 r tropical (10-25 degrees N) central Pacific Ocean, particularly during La-Nina conditions.

207 Anthropogenic CO2 is expected to drive ocean pCO2 above 1,000 muatm by 2100 - inducing respirat

208 The evolution of surface ocean pCO2 in key locations can therefore provide import

209 ings of this study provide baseline data for ocean plastic mass balance exercises, and assist in prio

210 r hydrogenetic Fe-Mn crusts from the Pacific Ocean (PO-01), South China Sea (SCS-01, SCS-02) and Indi

211 rometer) and dissolved organic matter in the ocean point to a marine source for the measured OVOCs.

212 interest, since it is widespread in surface oceans, presents ecotypic differentiation and has defied

213 in regulating the magnitude and dynamics of ocean primary productivity, making it an integral compon

214 d delivery of nutrients with implications on ocean productivity at peak glacial conditions.

215 vailable radiation (PAR), but the effects on ocean productivity have received little consideration as

216 whale population of the northeastern Pacific Ocean provides a data-rich case to explore anthropogenic

217 um spp. sampled from geographically isolated ocean provinces (the Atlantic Ocean, the Red Sea and the

218 These findings question the fidelity of ocean reanalysis products in the pre-Argo era.

219 Based on an ocean reanalysis, possible generation mechanism of the l

220 Here we couple records of ocean redox chemistry with nitrogen isotope ((15)N/(14)N

221 (15) N) patterns that differentiate distinct ocean regions to create a 'regional isotope characteriza

222 The Southern Ocean regulates the ocean's biological sequestration of

223 penguins may use vocal communication in the ocean related with group association during foraging tri

224 ctions-protection on land, protection in the ocean, restoration on land, or restoration in the ocean-

225 bon(C)-cycle, and depleted oxygen in Earth's oceans resulting in marine mass extinction.

226 Sulfide mineral precipitation occurs at mid-ocean ridge (MOR) spreading centers, both in the form of

227 mil ( per thousand), than the canonical mid-ocean ridge basalt value of -6.0 per thousand.

228 e lower (3)He/(4)He ratios identified in mid-ocean-ridge basalts that form by melting the upper mantl

229 ced a surge in magma and CO2 fluxes from mid-ocean ridges and oceanic hotspot volcanoes.

230 nected and detectable, the CO2 fluxes at mid-ocean ridges, the depth of the lithosphere-asthenosphere

231 ng, caused primarily by the deepening of the ocean's 26 degrees C isotherm Z 26 .

232 ryotic microorganisms that drive the pelagic ocean's biogeochemical cycles are currently facing an un

233 vity, making it an integral component of the ocean's biogeochemical cycles.

234 The Southern Ocean regulates the ocean's biological sequestration of CO2 and is widely su

235 bility of dominant dsDNA viruses in the open ocean's euphotic zone over daily and seasonal timescales

236 cycling and ecological relationships in the ocean's interior, but the relevant taxa and energy sourc

237 of these findings is that diel cycles in the ocean's photic zone appear to be universal organizing pr

238 rovide important clues for understanding the ocean's role in Pleistocene carbon cycling.

239 , with most land ice-covered and much of the ocean seasonally freezing.

240 om forests, and these were distinct from the ocean sediment isolates.

241 n Oceanic Anoxic Event or T-OAE from an open ocean sedimentary succession from western North America.

242 population dynamics, and tempo of the Indian Ocean slave trade.

243 re is geographically dominated by the Indian Ocean-Southern Pacific region, marking a transition from

244 (delta(18)O) record from the South Atlantic Ocean spanning an interval between 30.1 My and 17.1 My a

245 f flat, normally indistinguishable from open-ocean SST, exceeded 6 degrees C above normal summertime

246 Through modulation of ocean stratification and near-surface winds, global warm

247 rejection leads to a strongly increased deep ocean stratification, consistent with high abyssal salin

248 The ongoing OCEAN study enrolled patients treated with ranibizumab f

249 mble atmospheric simulations with prescribed ocean surface conditions to examine how seasonal-scale N

250 a-a proxy for seawater pH-that show that the ocean surface pH was persistently low during the PETM.

251 Ocean surface warming is resulting in an expansion of st

252 trogen to oligotrophic, tropical/subtropical ocean surface waters.

253 nces of small particles are predicted at the ocean surface, while at the same time these small partic

254 ive conservation outcomes for connected land-ocean systems can proceed without complex modelling.

255 extend to the continental shelf, and include ocean systems with waters up to 50 meters in depth.

256 We conclude that increasing ocean temperature is an important factor facilitating th

257 oximately 1.4 degrees C, while deep Southern Ocean temperature remains largely unchanged.

258 anus glacialis, may respond to both abiotic (ocean temperature) and biotic (phytoplankton prey) drive

259 cross the deglaciation, few studies show how ocean temperatures evolved across the deglaciation.

260 long after, the harmful effects of elevated ocean temperatures take hold and may be the primary driv

261 eather events and their association with the ocean temperatures underscores the potential predictabil

262 ch induces differential heating in the upper ocean that affects vertical mixing and thus SST.

263 were able to precipitate from a contemporary ocean that contained only trace amounts of sulfate remai

264 lgal time series from the northwest Atlantic Ocean that exhibits multidecadal variability extending b

265 nin-Mariana subduction zone forearc (Pacific Ocean) that contain complex organic matter and nanosized

266 ern subtropical and eastern tropical Pacific Ocean, the Arabian Sea, and the Bay of Bengal.

267 cally isolated ocean provinces (the Atlantic Ocean, the Red Sea and the Indian Ocean) were shown to h

268 ere found in the European part of the Arctic Ocean; these distributions likely reflect a combination

269 Anthropogenic noise across the world's oceans threatens the ability of vocalizing marine specie

270 Rogues form in the open ocean through the addition of elemental wave trains or g

271 uranium from the central equatorial Pacific Ocean to identify intervals associated with respiratory

272 d thousands of kilometers across the Pacific Ocean to the shores of North America and Hawai'i.

273 , restoration on land, or restoration in the ocean-to maximise the extent of light-dependent marine b

274 and an opportunity for the Surface Water and Ocean Topography mission.

275 bation experiment results, and retrospective ocean transport simulations, we investigated biological

276 f 2004-2016, we show that the observed upper ocean velocities are comprised of balanced geostrophic f

277 ted with the shortening of lead time between ocean warm water volume (WWV) variability along the equa

278 hic efficiency, which could arise because of ocean warming and DSL shallowing.

279 nt Current Biology paper [1], we describe an ocean warming experiment in which we manipulated the tem

280 ng the distribution of these communities and ocean warming has the potential to cause major distribut

281 edators may be more sensitive to the rate of ocean warming rather than to warming itself.

282 sor global change, the combined influence of ocean warming, acidification, and deoxygenation, poses a

283 at, given potential reductions in PLD due to ocean warming, future marine reserve networks would requ

284 ktonic larval duration (PLD) associated with ocean warming, given current socioeconomic constraints.

285 r are associated with changes in the rate of ocean warming.

286 benthic communities may change under future ocean warming.

287 ciation, possibly triggered by anthropogenic ocean warming.

288 and its metabolites in intermediate and deep ocean water masses.

289 gh heat contained in inflowing warm Atlantic Ocean water to melt all Arctic sea ice within a few year

290 oxies showing the incursion of deep Southern Ocean waters into the tropics and subtropics.

291 ess and geostrophic currents over the global ocean, we confirm that the current-induced surface stres

292 and subtropical Pacific, Atlantic and Indian Oceans were collected during the Malaspina 2010 circumna

293 e Atlantic Ocean, the Red Sea and the Indian Ocean) were shown to harbor highly similar, taxonomicall

294 is a source of methane in the upper, aerobic ocean, where phosphorus-starved microbes catabolize meth

295 cattle of Amsterdam Island, southern Indian Ocean, which dwarfed to about three quarters of its body

296 Yet, Antarctica and the Southern Ocean, which encompass 10% of the planet's surface, are

297 Importantly, these ocean-wide migration patterns can ultimately be linked w

298 of terrestrial microbes transported over the oceans, with abundances declining exponentially with dis

299 Sea and much higher than several other open oceans worldwide.

300 f dissolved organic carbon (DOC) to the deep ocean, yet the contribution from advective settings has