ライフサイエンスコーパス: oceanic

1 Although oceanic ammonia and nitrite oxidation are balanced, ammo

2 We then compared those with the National Oceanic and Atmospheric Administration National Weather

3 m the North American portion of the National Oceanic and Atmospheric Administration's Global Greenhou

4 mental Panel on Climate Change, the National Oceanic and Atmospheric Administration, the National Ren

5 Retreat was minimal despite oceanic and climatic conditions during the early-Holocen

6 rbon is the third-largest carbon stock after oceanic and geological pools.

7 , their importance in the sulfur cycle, both oceanic and physiological, has only recently gained atte

8 t toward coherent decadal variability in the oceanic and terrestrial [Formula: see text] sinks, and t

9 es will help to constrain the sensitivity of oceanic and terrestrial [Formula: see text] uptake to cl

10 rrelation and the timing of the responses of oceanic and terrestrial carbon cycle remain poorly const

11 ioeconomic predictors, these slowly evolving oceanic and terrestrial predictors are further identifie

12 Here, we study moisture transport from the oceanic and terrestrial sources to the Indian landmass a

13 l(3) and CH(3)Cl, we found evidence for both oceanic and terrestrial sources.

14 Although the causes of the early Toarcian Oceanic Anoxia Event (OAE) have been fairly well studied

15 This time was characterized by two pulses of oceanic anoxia, named the Lower and Upper Kellwasser eve

16 such as prolonged climatic perturbations and oceanic anoxia, related to the mass extinction.

17 ed by extinctions, climate fluctuations, and oceanic anoxia.

18 The Toarcian Oceanic Anoxic Event (T-OAE) was characterized by a majo

19 spects of the supposed hyperthermal Toarcian Oceanic Anoxic Event (T-OAE, Early Jurassic, c.

20 The Toarcian Oceanic Anoxic Event (TOAE, Early Jurassic, ~182 Ma ago)

21 he source rock represents the later stage of Oceanic Anoxic Event 2.

22 severe climatic warming across the Toarcian Oceanic Anoxic Event or T-OAE from an open ocean sedimen

23 he Triassic-Jurassic transition and Toarcian Oceanic Anoxic Event, are well studied and largely assoc

24 at scales ranging from small ponds to global oceanic anoxic events.The role of microbial communities

25 explain why adaptive radiation is common on oceanic archipelagoes - because colonising species can b

26 Oceanic archipelagos are the ideal setting for investiga

27 ds, based on the terrestrial avifaunas of 41 oceanic archipelagos worldwide (including 596 avian taxa

28 rosol-climate interactions over other remote oceanic areas beyond Pacific.

29 emporal distribution, especially over remote oceanic areas.

30 Understanding the importance of the oceanic background state, local and remote drivers and t

31 copepod zoosphere may influence estimates of oceanic bacterial biomass and in part control bacterial

32 North Male Atoll (Maldives) includes oceanic barrier as well as lagoonal reefs.

33 rt an exhumed mantle basement rather than an oceanic basement below the Vavilov basin.

34 n by ancestral benthic lineages in all major oceanic basins.

35 ean acidification has been documented in all oceanic basins.

36 in, because cyclone effects do differ across oceanic basins.

37 ion (OA) is critical to understanding future oceanic biogeochemical cycles.

38 n and heat, nutrient resupply for sustaining oceanic biological production, and the melt rate of ice

39 The oceanic biological pump is responsible for the important

40 of the ocean forms an important limb of the oceanic biological pump, which impacts the sequestration

41 ern Hemisphere climate anomalies through the oceanic bipolar seesaw.

42 To prevent further introductions, oceanic BW exchange and BW treatment systems are utilize

43 of -10 per mille and a mean increase in the oceanic C inventory of +14,900 petagrams of carbon (PgC)

44 within the distinct evolutionary lineage of Oceanic canids.

45 huxleyi-EhV interactions play a key role in oceanic carbon biogeochemistry.

46 omplex ecosystem dynamics and changes in the oceanic carbon cycle.

47 Despite their importance in oceanic carbon cycling and export, little is known about

48 and biogeochemical function of laminarin in oceanic carbon export and energy flow to higher trophic

49 erwent an ontogenetic habitat shift from the oceanic central North Pacific (CNP) to the neritic east

50 ble-driven ebullitive fluxes, we place total oceanic CH(4) emissions between 6-12TgCH(4)yr(-1), narro

51 to be similar to sea level, temperature and oceanic chemistry at multiple timescales.

52 lationship between interannual variations in oceanic chlorophyll (CHL) and sea surface temperature (S

53 then incorporated into the CESM to represent oceanic chlorophyll -induced climate feedback in the tro

54 persal and persistence driven by patterns of oceanic circulation favouring self-recruitment played a

55 olved to exploit predictable atmospheric and oceanic circulation patterns.

56 likely responds to long-term variability in oceanic circulation ultimately related to climatic indic

57 nd synchronous change in the atmospheric and oceanic circulations was observed in the North Pacific d

58 eceleration periods that typically stem from oceanic climate variability.

59 impact of decadal circulation changes on the oceanic CO2 sink using a carbon cycling model.

60 Recent data show that oceanic CO2 uptake rates have been growing over the past

61 As both models have the same oceanic component, but are with different atmospheric co

62 Oceanic concentrations of the individual monoterpenes ra

63 e species which tolerates higher temperature oceanic conditions than Bathycoccus prasinos (BI).

64 hyll concentrations by up to 56% relative to oceanic conditions, and SICE seamounts have two-fold hig

65 rlie their ecological success in fluctuating oceanic conditions.

66 erature at the serpentinized Atlantis Massif oceanic core complex, Mid-Atlantic Ridge.

67 y reveals that the presence and evolution of oceanic core complexes play a key role in triggering blo

68 When conducting oceanic crossings, migratory birds tend to associate wit

69 and determine the velocities and density of oceanic crust along different mantle geotherms.

70 the Arabian plate from in situ Gulf of Oman oceanic crust and mantle presently subducting northwards

71 and as a constraint on the flux of K between oceanic crust and seawater.

72 us fluids entering the upper mantle or lower oceanic crust are trapped in olivine as secondary fluid

73 wever, the velocity and density of subducted oceanic crust at lower-mantle conditions remain unknown.

74 ths to which carbon in sediments and altered oceanic crust can be subducted and the relative contribu

75 tudy suggests that the presence of subducted oceanic crust could provide good explanations for some l

76 daptations of fungal communities in the deep oceanic crust from ~10 to 780 mbsf by combining metabarc

77 vered a megameter-scale portion of thickened oceanic crust in the uppermost lower mantle west of the

78 n, which recycled increasing volumes of cold oceanic crust into the mantle.

79 The lithified lower oceanic crust is one of Earth's last biological frontier

80 tions between 800 and 400 Ma, which oxidized oceanic crust on the seafloor.

81 rge amounts of low-temperature exchange with oceanic crust or that the weathering flux of continental

82 /(39)K can be used as an effective tracer of oceanic crust recycled into the mantle, as a diagnostic

83 We find that the subducted oceanic crust shows a large negative shear velocity anom

84 the mantle at convergent margins, where the oceanic crust subducts beneath the continental crust.

85 oirs or typical mantle but resembles that of oceanic crust that was initially altered by seawater and

86 r this phase transition in silica, subducted oceanic crust will be visible as high-velocity heterogen

87 apolated, our results suggest that subducted oceanic crust will be visible as low-seismic-velocity an

88 on by which to identify ancient fragments of oceanic crust, and as a constraint on the flux of K betw

89 sistent with moderate enrichment of recycled oceanic crust, and mid-mantle discontinuities can be exp

90 s; those derived from metasediments, altered oceanic crust, and serpentinite have delta(34)S values o

91 The lithified oceanic crust, lower crust gabbros in particular, has re

92 e diamonds, indicate that carbonated igneous oceanic crust, not sediment, is the primary carbon-beari

93 g preferential (26)Mg incorporation into the oceanic crust, on average by epsilon(solid-fluid) ~ 1.6

94 accretion and tectonic dismemberment of the oceanic crust, resulting in an irregular seafloor morpho

95 CO(2) released from the mantle and subducted oceanic crust.

96 ers the chemical and isotopic composition of oceanic crust.

97 of H(2) production and consumption in young oceanic crust.

98 tle were proposed to be related to subducted oceanic crust.

99 ation from melts of carbonate-rich subducted oceanic crust.

100 document the geological processes that form oceanic crust.

101 ctic krill (Euphausia superba) are swarming, oceanic crustaceans, up to two inches long, and best kno

102 t yet been any K-isotope analyses of altered oceanic crustal materials.

103 typus lineages is complex, in which ancient oceanic current systems and (currently unrecognised) spe

104 es into two main groups matching large-scale oceanic current temperatures, and six finer proteotypes

105 early Miocene dispersal to Madagascar, using oceanic currents that favoured eastward dispersal at tha

106 Oceanic cyanobacteria are the most abundant oxygen-gener

107 Thus, we suggest that oceanic DBC does not predominantly originate from rivers

108 rophic upwelling along the light side of the oceanic density front.

109 At oceanic depths >200 m, there is little ambient sunlight,

110 king reasonable assumptions for the pre-PETM oceanic DIC inventory, we provide a fully data-driven es

111 The vast majority of oceanic dimethylsulfoniopropionate (DMSP) is thought to

112 Large seeds were involved in 10 oceanic dispersals.

113 se that the MCO was associated with elevated oceanic dissolved inorganic carbon caused by volcanic de

114 ned model results show that more than 30% of oceanic DMS emitted to the atmosphere forms HPMTF.

115 S holds the key to a better understanding of oceanic DMSP cycles.

116 tter understanding of the feeding ecology of oceanic dolphins and provides new insights into the role

117 n acoustic presence and foraging activity of oceanic dolphins at two seamounts (Condor and Gigante) i

118 both their year-round spatial spread across oceanic domains and the total distance travelled.

119 Comparing porewater and oceanic DOS molecular formulas, solar irradiation increa

120 Oceanic ecosystems are dominated by minute microorganism

121 en that these activities dramatically impact oceanic ecosystems, through overexploitation of fish sto

122 The finding highlights the unique feature of oceanic eddies along the western boundary currents.

123 er Program (GDP) data set, it was found that oceanic eddies are asymmetrically distributed across the

124 From the analysis of oceanic eddies detected in the drifter trajectories of t

125 eries and have been observed in anticyclonic oceanic eddies occasionally.

126 Oceanic emissions of iodine destroy ozone, modify oxidat

127 Oceanic emissions represent a highly uncertain term in t

128 ern as plastics have become prevalent in the oceanic environment, and evidence of their impacts on ma

129 hem to survive and thrive in the challenging oceanic environment.

130 t of 144 US Navy dolphins housed in the same oceanic environment.

131 jority of them weaken due to atmospheric and oceanic environments unfavorable for typhoon intensifica

132 esting different strategies of adaptation to oceanic environments.

133 with convergent evolution to coastal versus oceanic environments.

134 ongly suggests potential contribution of non-oceanic factors (e.g., land cover change and CO2-induced

135 of the BC produced by landscape fires has an oceanic fate.

136 hese observations, we track the evolution of oceanic Fe-concentrations by considering the temporal re

137 olution of the North Pacific atmospheric and oceanic fields.

138 We quantified movements of a demersal oceanic fish species (gray triggerfish Balistes capriscu

139 rate zone and (2) negatively correlated with oceanic fish species richness.

140 l catches reveals a serial depletion of some oceanic fish stocks over time, resulting in fisheries fo

141 rgy from the lateral shear of the background oceanic flow.

142 mate change is of critical importance to the oceanic food web and fish stocks.

143 This suggests that oceanic forcing by subsurface warming may also have cont

144 are three independent methods for estimating oceanic [Formula: see text] uptake and find that the oce

145 cally brief duration of modern anthropogenic oceanic [Formula: see text] uptake is roughly equivalent

146 text]O) is limited by poor knowledge of the oceanic [Formula: see text]O flux to the atmosphere, of

147 ergy and potential vorticity (PV) changes of oceanic geostrophic eddies.

148 arrival of people sharing ancestry with Near Oceanic groups (i.e., Austronesian-speaking and Papuan-s

149 and was then followed by the arrival of non-Oceanic groups during European colonialism.

150 migrations across ocean basins and remain in oceanic habitats for several years.

151 otope ratios between glacial-marine and more oceanic habitats.

152 We further show that a declining northward oceanic heat flux in recent decades, which is linked to

153 Fjord dynamics influence oceanic heat flux to the Greenland ice sheet.

154 The associated enhanced release of oceanic heat has reduced winter sea-ice formation at a r

155 er initial variability, a greater cumulative oceanic heat loss from ENSO thermal damping reduces stra

156 Although oceanic hotspot lavas currently provide the best constra

157 gma and CO2 fluxes from mid-ocean ridges and oceanic hotspot volcanoes.

158 ng-range persistence is a consequence of the oceanic integration of both gradual and abrupt climate f

159 They suggest that the oceanic iron cycle, and therefore oceanic primary produc

160 s to ancient melt extraction) common to most oceanic island basalts, previously called PREMA (prevale

161 esponsible for the rich endemic diversity of oceanic island floras is important for our understanding

162 de of rapid evolutionary radiations found on oceanic islands and mountain ranges across the globe [1-

163 Nutrients from seabirds nesting on oceanic islands enhance the productivity and functioning

164 Evolutionary radiations on oceanic islands have fascinated biologists since Darwin'

165 requently tested on model ecosystems such as oceanic islands that vary in both.

166 s over long timescales, exposing surrounding oceanic islands to plastic contamination, with potential

167 tantially contributes to species endemism on oceanic islands when speciation involves the colonisatio

168 e migration is no longer beneficial, such as oceanic islands, migration-association traits may be sel

169 long distances in the Indian Ocean to small oceanic islands.

170 rculation and enhancing eastward-propagating oceanic Kelvin waves in the tropical Pacific.

171 ematically account for all H(2) within young oceanic lithosphere (<10 Ma) near the Mid-Ocean Ridge (M

172 they would imply the presence of thick young oceanic lithosphere (20-25 km), and extremely heterogene

173 Our results suggest that rifting of oceanic lithosphere alternates between magmatically and

174 Oceanic lithosphere carries volatiles, notably water, in

175 n of the uppermost lower mantle by subducted oceanic lithosphere destabilizes carbon-bearing metals t

176 Crustal properties of young oceanic lithosphere have been examined extensively, but

177 xidation of ultramafic rock, which occurs as oceanic lithosphere is emplaced onto continental margins

178 chanism behind plate tectonics, which allows oceanic lithosphere to be subducted into the mantle as "

179 eoproterozoic - when low-angle subduction of oceanic lithosphere was more prevalent than today - acco

180 ects the physical and chemical properties of oceanic lithosphere, represents one of the major mechani

181 bduction zone sulfur recycling for a typical oceanic lithosphere.

182 wo suites of exhumed fragments of subducted, oceanic lithosphere.

183 ge fluid release from subducting slow-spread oceanic lithosphere.

184 The oceanic magnesium budget is important to our understandi

185 The oceanic magnesium cycle is largely controlled by contine

186 ate on the sources and sinks that define the oceanic magnesium cycle, including new constraints on th

187 th deeper endogenic brines, could also allow oceanic material to reach the surfaces of other large ic

188 ons for air-sea interaction and implies that oceanic mean and mesoscale circulations and their effect

189 By means of synergistic atmospheric and oceanic measurements in the Southern Ocean near Antarcti

190 nisms reliant on surface wind changes, while oceanic mechanisms related to AMOC changes become more i

191 WH requires considering both atmospheric and oceanic mechanisms.

192 identified the incorporation of deeper water oceanic MeHg sources into deeper water sediments prior t

193 baroclinicity and compensates the associated oceanic meridional energy transport.

194 Coherent oceanic mesoscale eddies with unique dynamical structure

195 ine genomics, we explore new applications of oceanic metagenomes for protein structure and function p

196 have at least one member associated with the oceanic metagenomics dataset.

197 ted to be 1.5-2.9 Tmol yr(-1); 40-60% of the oceanic Mg outputs).

198 re hydrothermal circulation remain enigmatic oceanic Mg sinks.

199 s of ocean circulation, facilitates the vast oceanic migrations of the Anguilla genus [7, 13, 14].

200 ntially occur in summer, when climatological oceanic mixed layers are shallow and winds are weak, but

201 and carbon uptake are better represented in oceanic models that include this feedback.

202 e regional scale and an asymmetric supply of oceanic moisture, in which the maximum values are locate

203 Because oceanic N limitation is common and likely to intensify i

204 provide evidence for differentiation across oceanic niches.

205 ariables (ie, rainfall, temperature, and the Oceanic Nino Index).

206 s of the Pacific Decadal Oscillation and the Oceanic Nino Index, an indicator of El Nino events.

207 nt for iron controlling the coupling between oceanic nitrogen and phosphorus cycles.

208 ss therefore has the ability to modulate the oceanic northward heat transport.

209 where they primarily forage on pinnipeds, to oceanic offshore habitats.

210 perative for its representation in models of oceanic overturning.

211 Oceanic oxygen minimum zones (OMZs) play a pivotal role

212 dional Overturning Circulation-the strongest oceanic pacemaker of the Atlantic Ocean and perhaps the

213 and ocean acidification (OA, a reduction in oceanic pH).

214 e show that a combination of atmospheric and oceanic phenomena played primary roles for this decline.

215 y reconstructing it in the globally abundant oceanic phytoplankter Prochlorococcus To understand what

216 l climate change can significantly influence oceanic phytoplankton dynamics, and thus biogeochemical

217 olithophore Emiliania huxleyi is an abundant oceanic phytoplankton, impacting the global cycling of c

218 The biogeographic response of oceanic planktonic communities to climatic change has a

219 orthwest-directed subduction of the Farallon oceanic plate beneath North America since c.

220 Using CSE data for oceanic plateau basalts (OPB), which rarely degas S, we

221 osed that the subaerial phases of Cretaceous oceanic plateau formation spurred the global environment

222 ough the mantle plume hypothesis predicts an oceanic plateau produced by massive decompression meltin

223 s thick crust represents a major part of the oceanic plateau that was created by the Hawaiian plume h

224 Unlike typical tholeiitic basalts of oceanic plateaus, the 1.2 km vertical submarine stratigr

225 al components, probably related to subducted oceanic plates or primordial material associated with Ea

226 work, we characterize the microstructure of oceanic polyethylene debris and compare it to the nonwea

227 is selectively conserved in terrestrial and oceanic pools.

228 his knowledge gap is magnified for dispersed oceanic predators such as endangered blue whales (Balaen

229 t that the oceanic iron cycle, and therefore oceanic primary production and climate, could be more se

230 ) fixation supports a significant portion of oceanic primary production by making N(2) bioavailable t

231 Nutrient limitation of oceanic primary production exerts a fundamental control

232 anticipate future climate change impacts on oceanic primary production.

233 Tuna trophic position and oceanic primary productivity were of weaker importance.

234 ic circulation anomalies and the subtropical oceanic primary productivity.

235 heric processes, while resolving small-scale oceanic processes acts as an unpredictable source of noi

236 tions within a host and enhance the rates of oceanic productivity and carbon export.

237 graphic conditions, being influenced by both oceanic productivity and sea surface temperature.

238 tropical eastern Australia, contrasting with oceanic proxies that suggest El Nino-like conditions pre

239 Subtropical gyres are the oceanic regions where plastic litter accumulates over lo

240 for growth is limited, with three restricted oceanic regions where seasonal conditions permit high gr

241 h into the future may be applicable to other oceanic regions with differing oceanographic modulators.

242 the prevailing view of high gene flow across oceanic regions with evidence of population structure wi

243 d six finer proteotypes that connect distant oceanic regions.

244 The Lofoten Basin is the largest oceanic reservoir of heat in the Nordic Seas, and the si

245 700 y) have been documented, evidence of the oceanic response to these changes is equivocal.

246 We consider the observation and analysis of oceanic rogue waves collected within spatio-temporal (ST

247 1-3 months timescale), which in turn excites oceanic Rossby waves in the central/eastern North Pacifi

248 und strong HIV-1 inhibition in one unrelated oceanic sample closely matching to HIV-1-inhibitory drug

249 co- and nano-sized) protists from a range of oceanic samples.

250 per than the 122 degrees C isotherm in known oceanic serpentinizing regions and an order of magnitude

251 arbonates across a wide range of neritic and oceanic settings, with potentially major implications fo

252 important carbonate producers in neritic and oceanic settings.

253 We quantify the oceanic sink for anthropogenic carbon dioxide (CO(2)) ov

254 ss-based studies are needed to constrain the oceanic sink of PFAS.

255 ood web structure between glacial-marine and oceanic sites.

256 een extensively documented within subducting oceanic slabs, but their mechanics remains enigmatic.

257 We find that the oceanic sources of moisture, namely western and central

258 n leads to the ecological extinction of many oceanic species.

259 ression of hot mantle rock upwelling beneath oceanic spreading centers causes it to exceed the meltin

260 dance and demographic parameters during this oceanic stage is challenging.

261 e patterns indicates that recruitment to the oceanic stage is more dependent on nest abundance at sou

262 factors regulating recruitment to the early oceanic stage.

263 the first estimates of relative abundance of oceanic-stage juvenile sea turtles.

264 r the global overturning circulation and the oceanic storage of atmospheric CO(2).

265 Oceanic submesoscale ageostrophic processes have been pr

266 Large reservoirs of natural gas in the oceanic subsurface sustain complex communities of anaero

267 tal manipulations of laboratory cultures and oceanic surface blooms of Trichodesmium from the South P

268 This work challenges the view that the oceanic surface waters in close proximity to continental

269 quantify and characterize plastic debris in oceanic surface waters of the Antarctic Peninsula.

270 In tropical and subtropical oceanic surface waters phosphate scarcity can limit micr

271 iological alteration of REE distributions in oceanic systems.

272 g results provide the first evidence that an oceanic teleconnection between AMOC strength and subsurf

273 ng which is controlled by largely unobserved oceanic thermodynamic and circulatory processes in the c

274 ure barrier zones that host active swarms on oceanic transform faults and provides candidates for fut

275 Oceanic transform faults display a unique combination of

276 ake sequences and aseismic transient slip on oceanic transform faults.

277 he relative importance of atmospheric versus oceanic transport for poly- and perfluorinated alkyl sub

278 ed in investigating sources, atmospheric and oceanic transport, and forecasting climate change impact

279 t the horizontal transport properties of the oceanic turbulent flow in which they are embedded.

280 lts requires that existing estimates for the oceanic upper mantle potential temperature be adjusted u

281 How H(2)O is distributed in the oceanic upper mantle remains poorly constrained.

282 a significant increase in resolution for the oceanic upper mantle.

283 in the deep ocean, but ultimately may limit oceanic uptake of anthropogenic CO2.

284 The oceanic uptake of atmospheric carbon dioxide (CO(2)) emi

285 rculation and is fundamentally important for oceanic uptake of carbon and heat, nutrient resupply for

286 Ice Shelf (PIIS), that there is considerable oceanic variability at seasonal and interannual timescal

287 therefore plays an important role in driving oceanic variability close to PIIS.

288 ntly than expected to SST evolution and thus oceanic variability during the observation period.

289 erent resolutions, that resolving meso-scale oceanic variability in the Gulf Stream region strongly a

290 In the tropics, long time-scale oceanic variability precludes determination of how much

291 r predicting fishing activity accounting for oceanic variables, climate indices, and vessel flag.

292 sources such as soda lakes and hydrothermal oceanic vents.

293 been widely debated in light of atmospheric/oceanic warming and increases in glacial melt over the p

294 east Australian region is experiencing rapid oceanic warming, predicted to lead to substantial altera

295 he predicted continuation of atmospheric and oceanic warming.

296 ems such as the oxygen-deficient zone in the oceanic water column, sea ice or polar snow.

297 cies with the majority of daily positions in oceanic waters off the continental shelf showed the grea

298 es in Antarctic soils and in the surrounding oceanic waters.

299 a biochemically dependant interplay between oceanic zinc, iron and phosphorus cycles.

300 for understanding the speciation process for oceanic zooplankton.