ライフサイエンスコーパス: deep ocean

1 ng particles, and finally sequestered in the deep ocean.

2 aditional beliefs that POPs do not reach the deep ocean.

3 pollutants between the coastal ocean and the deep ocean.

4 persistent organic pollutants (POPs) in the deep ocean.

5 rticulate organic carbon (POC) fluxes to the deep ocean.

6 onments, including lakes, rather than in the deep ocean.

7 ly efficient at sequestering carbon into the deep ocean.

8 r enhance export of picophytoplankton to the deep ocean.

9 export of carbon and other nutrients to the deep ocean.

10 of which 5 to 15 per cent is exported to the deep ocean.

11 presents 4-31% of the oil sequestered in the deep ocean.

12 e a precursor of micro-blebs observed in the deep ocean.

13 ce of ash/pumice deposit distribution in the deep ocean.

14 the near-inertial energy penetrates into the deep ocean.

15 rtance of H(2) as a key energy source in the deep ocean.

16 arbon northward, and from the surface to the deep ocean.

17 n or uptake, sequestration and export to the deep ocean.

18 production and carbon sequestration into the deep ocean.

19 pable of delta(13)C(CH4) measurements in the deep ocean.

20 e marine habitats, from the surf zone to the deep ocean.

21 c was home to a globally sulphidic (euxinic) deep ocean.

22 on is transferred from the atmosphere to the deep ocean.

23 soon enough to avoid transfer of heat to the deep ocean.

24 have directly enhanced carbon export to the deep ocean.

25 sults in enhanced organic carbon flux to the deep ocean.

26 d subtle slope breaks located far out in the deep ocean.

27 the globe and regulates their storage in the deep ocean.

28 it serves as a lid to a larger volume of the deep ocean.

29 ates, and may have led to oxygenation of the deep ocean.

30 ent iron can alter the flux of carbon to the deep ocean.

31 it occurs on long unknown time scales in the deep ocean.

32 rn Ocean contained the saltiest water in the deep ocean.

33 o sustained and widespread freshening of the deep ocean.

34 ion concentration existed in the glacial-age deep ocean.

35 e will have inhibited transport of O2 to the deep ocean.

36 ents acting as a source of old carbon to the deep ocean.

37 organic material from surface waters to the deep ocean.

38 ontribution of different water masses to the deep ocean.

39 y and distribution of nektonic carbon in the deep ocean.

40 look its relevance as a carbon source to the deep ocean.

41 between benthic and pelagic habitats in the deep ocean.

42 retching from high montane lakes down to the deep ocean.

43 of sinking particulate organic matter in the deep ocean.

44 regarding the oil's fate and effects in the deep ocean.

45 om predators, particularly for fishes of the deep ocean.

46 ne food webs and the flux of carbon into the deep ocean.

47 supports numerous ecosystem services in the deep ocean.

48 r of carbon to higher trophic levels and the deep ocean.

49 ochthonous FDOM, which may accumulate in the deep ocean.

50 e of aquatic habitats from shallow rivers to deep oceans.

51 ccessible to humans, from distant planets to deep oceans.

52 s key step of the global carbon cycle in the deep oceans.

53 enzymes that underpin chemosynthesis in the deep oceans.

54 ources and transformations of mercury in the deep oceans.

55 k of environmental regulatory policy for the deep oceans.

56 s and man-made structures in the shallow and deep oceans.

57 variables among five scientific areas of the deep ocean: (1) biodiversity; (2) ecosystem functions; (

58 f the euphotic zone into the mesopelagic and deep ocean(3-5).

59 ency of the biological pump of carbon to the deep ocean [7-9].

60 of alternative eruption sources, including a deep ocean, a freshwater reservoir, or ice.

61 The deep ocean absorbs vast amounts of heat and carbon dioxi

62 the carbon cycle and solar forcing modulates deep ocean acidity as well as the production and burial

63 city intensity and enhance the mixing in the deep ocean, also have potential implication for deep-sea

64 penetration of near-inertial energy into the deep ocean and a hotspot for the diapycnal mixing in win

65 -3) Wm(-2) radiates into the thermocline and deep ocean and accounts for 42%-58% of the energy requir

66 gin of sulfur-depleted organic matter in the deep ocean and cannot adequately reproduce our observed

67 oceanic reservoir due to oxygenation of the deep ocean and corresponding decrease in sulphidic condi

68 arbon and what allows its persistence in the deep ocean and in sediment is unresolved.

69 biological pump drives carbon storage in the deep ocean and is thought to function via gravitational

70 organic carbon from the ocean surface to the deep ocean and its subsequent burial through biogeochemi

71 e of the most abundant microorganisms in the deep ocean and responsible for much of the ammonia oxida

72 mparatively little carbon, in the underlying deep ocean and sediments.

73 tion of a substantial fraction of DOC in the deep ocean and that this dilution acts as an alternative

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

75 conditions proposed previously for Ediacaran deep oceans and helps to explain the patchy temporal rec

76 obiological studies and energy flow in dark, deep-ocean and subseafloor rock habitats.

77 gene and its transcription is greater in the deep ocean, and is highest in the sediment.s DMSP catabo

78 biomass exists in the deep biosphere, in the deep ocean, and within the Earth's crust.

79 an is the principal means of ventilating the deep oceans, and is therefore a key element of the globa

80 The amplitude of the deep ocean anomalies is up to six times the amplitude of

81 t radiocarbon variations in the intermediate/deep ocean are associated with roughly synchronous chang

82 cale releases of methane from hydrate in the deep ocean are likely to be met by a similarly rapid met

83 Estimates of carbon flux to the deep oceans are essential for our understanding of globa

84 ed carbon is transferred from the surface to deep ocean as sinking particles or dissolved organic car

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

86 sess the impact of mixing processes on these deep ocean bacterial communities and their capacity for

87 Deep ocean bacterial isolates show enhanced DMSP product

88 n the deep-ocean water for 1.8 years for the deep-ocean bacterioplankton to grow to the 2.4x higher c

89 present observations from the Scotia Sea, a deep ocean basin between the Antarctic peninsula and the

90 pping tectonic structures, especially in the deep ocean basins where the topography remains unmapped

91 In the deep ocean bed of the SCS, source-related signatures of

92 The deep ocean bed of the South China Sea (SCS) is considere

93 f hydrothermal vent microbial communities in deep ocean biogeochemical cycles.

94 Deep-sea coral communities are hotspots of deep ocean biomass and biodiversity, providing critical

95 The photochemical reaction cycle of Hawaiian deep ocean BPR in cells is 10-fold slower than that of G

96 hermal heating of young rift sediments alter deep-ocean budgets of bioavailable DOM, creating organic

97 s is among the highest found anywhere in the deep ocean, but constraints on microbial growth and meta

98 e near future by trapping natural CO2 in the deep ocean, but ultimately may limit oceanic uptake of a

99 observed estimates of vertical mixing in the deep ocean by presenting a revised view of the thermohal

100 that this signal will be transferred to the deep ocean by the two overflows.

101 rect quantification of the contribution from deep ocean carbon sources to community production in the

102 supports the view that the ventilation of a deep-ocean carbon reservoir in the Southern Ocean had a

103 t, during deglaciations, an isolated glacial deep-ocean carbon reservoir is reconnected with the atmo

104 eglacial injection of very old waters from a deep-ocean carbon reservoir that was previously well iso

105 ump almost doubles the previous estimates of deep-ocean carbon sequestration by biological processes

106 atmospheric CO2 variations invoke changes in deep-ocean carbon storage, probably modulated by process

107 e, match the shape of the CIE and pattern of deep ocean carbonate dissolution as recorded in sediment

108 Deep-ocean carbonate ion concentrations ([CO(3)(2-)]) an

109 ermine the population structure of a cryptic deep ocean cetacean, the Gray's beaked whale (Mesoplodon

110 ngly suggests that the sequenced surface and deep ocean changes were forced by pulsed meltwater outbu

111 etal enrichment record implies a Proterozoic deep ocean characterized by pervasive anoxia relative to

112 iously unexplored texture and variability in deep ocean chemistry during Earth's early history.

113 This suggests that on millennial timescales deep ocean circulation and iron fertilization in the Sou

114 y shows that various inferred changes in the deep ocean circulation and stratification between glacia

115 associated with major rearrangements in the deep ocean circulation and stratification, which have li

116 nt interglacial, but evidence for concurrent deep ocean circulation change is ambiguous.

117 The mechanisms by which the deep ocean circulation changed, however, are still uncle

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

119 strong polar halocline fundamentally altered deep ocean circulation, which enhanced interhemispheric

120 he atmosphere--probably linked to changes in deep ocean circulation--occurred during the last deglaci

121 ever, understanding the relationship between deep-ocean circulation and ancient climate is complicate

122 eenhouse conditions can thus initiate abrupt deep-ocean circulation changes in less than a few thousa

123 The deep-ocean circulation is responsible for a significant

124 These records indicate that deep-ocean circulation patterns changed from Southern He

125 e we present evidence for an abrupt shift in deep-ocean circulation using carbon isotope records from

126 ate climate model inferences that a shift in deep-ocean circulation would deliver relatively warmer w

127 Explicit recognition of deep-ocean climate mitigation and inclusion in adaptatio

128 In contrast, deep ocean communities differed less between poles and l

129 stions persist about how such changes impact deep ocean communities.

130 selection mechanisms controlling surface and deep ocean community structure and diversity.

131 may be related to iron-rich and sulfate-poor deep-ocean conditions facilitated by an increase in the

132 ing, consistent with a collapse of the local deep-ocean convection.

133 ains Southern Ocean surface water and global deep ocean cooling in the apparent absence of (sub-) equ

134 The deep ocean, covering a vast expanse of the globe, relies

135 at suitable habitats as larvae dispersed by deep-ocean currents.

136 isotope (delta(13)C) megasplice, documenting deep-ocean delta(13)C evolution since 35 million years a

137 Deep-ocean density stratification has been proposed as a

138 n, which indirectly points to an increase in deep-ocean density stratification.

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

140 chanism to promote the storage of CO2 in the deep ocean during glacial times.

141 reconstruct salinity and temperature of the deep ocean during the Last Glacial Maximum (LGM).

142 enomena suggests that the overturn of anoxic deep oceans during the Late Permian introduced high conc

143 An enigmatic mass extinction occurred in the deep oceans during the Mid Pleistocene, with a loss of o

144 ffective management of increasing use of the deep ocean (e.g., for bottom fishing, oil and gas extrac

145 s and virtually no in situ productivity, the deep oceans, Earth's largest ecosystem, are especially e

146 limate change will affect carbon cycling and deep-ocean ecosystem function.

147 ed food supply), is projected to affect most deep-ocean ecosystems concomitantly with increasing dire

148 have revealed unexpectedly large changes in deep-ocean ecosystems significantly correlated to climat

149 nd to protect the integrity and functions of deep-ocean ecosystems.

150 ts into organic matter transformation in the deep ocean emerged.

151 .5-year record of photographic data from the Deep-ocean Environmental Long-term Observatory Systems s

152 mixing processes in the microbial ecology of deep ocean environments.

153 Reduced surface-deep ocean exchange and enhanced nutrient consumption by

154 with shallow tropical seas; however, recent deep-ocean exploration using advanced acoustics and subm

155 oto-degradation behaviour when compared with deep-ocean FDOM, further strengthening the similarity be

156 ling reveal that marine red beds formed when deep-ocean Fe-concentrations were > 4 nM.

157 r petroleum hydrocarbons that settled to the deep ocean floor following release from the damaged Maco

158 en comprise >50% of eukaryote biomass on the deep-ocean floor.

159 describe a footprint of oil deposited on the deep-ocean floor.

160 rease occurred in the amplitude of change of deep-ocean foraminiferal oxygen isotopic ratios, traditi

161 cal dissolved inorganic carbon fluxes to the deep ocean from the organic-poor, metalliferous sediment

162 tu real-time measurements of ion-fluxes near deep-ocean geothermal vents.

163 here on glacial-interglacial timescales, the deep ocean has been implicated as the likely location of

164 A build-up of carbon in the deep ocean has been shown to have occurred during the La

165 As a result, the great volume of the deep ocean has easiest access to the atmosphere through

166 t to be maintained by a rapid ventilation of deep-ocean heat through convective mixing.

167 the volcano-induced dynamic chemistry of the deep ocean, here we demonstrate the Leidenfrost dynamic

168 1 year, but stabilization of subsurface and deep ocean Hg levels requires aggressive controls.

169 t patterns of microbial succession following deep ocean hydrocarbon blowouts are predictable and prim

170 However, as our methods for exploring the deep ocean improve, common assumptions about dispersal,

171 heric pCO2 invoke a significant role for the deep ocean in the storage of CO2.

172 here convection exports surface water to the deep ocean in winter as part of the thermohaline circula

173 reservoir of organic carbon suspended in the deep ocean, indicating that this event may have had a ke

174 Our observations indicate that the deep ocean influenced dramatic Northern Hemisphere warmi

175 hydrothermal chemical and heat flux into the deep-ocean interior and for dispersing propagules hundre

176 The pattern of contamination points to deep-ocean intrusion layers as the source and is most co

177 ubmerged oil thought to have been trapped in deep-ocean intrusion layers at depths of approximately 1

178 escales are dominated by slow changes in the deep ocean inventory of biologically sequestered carbon

179 e a concentration threshold that buffers the deep ocean iron inventory.

180 cline suggest that P remineralization in the deep ocean is a byproduct of microbial carbon and energy

181 es through the mesopelagic zone and into the deep ocean is a critical determinant of the atmosphere-o

182 Field evidence from the deep ocean is consistent with these laboratory conclusio

183 The deep ocean is frequently assumed to be a homogeneous sys

184 ogeochemical methane cycling dynamics in the deep ocean is hampered by a number of challenges, especi

185 The deep ocean is home to a group of broad-collared hemichor

186 The deep ocean is most likely the primary source of the radi

187 The deep ocean is the largest and least-explored ecosystem o

188 Ventilation of carbon stored in the deep ocean is thought to play an important role in atmos

189 the diapycnal mixing in the thermocline and deep ocean is tightly related to the shear variance of w

190 constraint the organic carbon export to the deep ocean is unable to compensate for the outgassing of

191 ses in the Southern Ocean, where much of the deep ocean is ventilated.

192 otope composition ((187)Os/(188)Os ratio) of deep oceans is 1.05, reflecting a balance between inputs

193 Consequently, oxygenation of the deep oceans may have lagged that of the atmosphere by ov

194 no-Southern Oscillation and for interpreting deep ocean measurements made from ships.

195 d and slowly sinking matter, stimulating the deep-ocean microbial loop.

196 of the global ocean is critically shaped by deep-ocean mixing, which transforms cold waters sinking

197 ers and their associated separation from the deep ocean nutrient reservoir.

198 ropose this elevation is due to increases in deep-ocean O(2) and marine sulfate concentrations betwee

199 age maximum at mid-depths and depriving the deep ocean of a fast escape route for accumulating respi

200 ation as rising atmospheric pO(2) sweeps the deep ocean of the ferrous iron substrate for photoferrot

201 of deglaciation include ice albedo feedback, deep-ocean out-gassing during post-glacial oceanic overt

202 eased because of progressive atmospheric and deep-ocean oxidation.

203 tional foraminiferal samples and multi-proxy deep-ocean oxygen estimates.

204 bal ice volume proxy(3) (as derived from the deep-ocean oxygen isotope record) and sea-level cycles a

205 models linking drastic isotope excursions to deep ocean oxygenation and the opening of environments c

206 ide a reconstruction of transient changes in deep ocean oxygenation and, by inference, respired carbo

207 an between these two steps and the timing of deep-ocean oxygenation have important implications for t

208 rmations and marine red beds, which indicate deep-ocean oxygenation occurred in the middle Ediacaran,

209 of marine red beds constrains the timing of deep-ocean oxygenation.The evolution of oceanic redox st

210 Here we reconstruct deep ocean particle fluxes by diagnosing the rate of nut

211 on periods consistent with a tsunami typical deep ocean period.

212 organic carbon (POC) from the surface to the deep ocean, plays an important role in regulating atmosp

213 bacterial dsyB mutants are less tolerant of deep ocean pressures than wild-type strains.

214 loss, indicating that biodegradation in the deep ocean progresses similarly to other environments.

215 from these two widely separated areas of the deep ocean provide compelling evidence that changes in c

216 nued international interest in exploring the deep ocean provides impetus to increase our understandin

217 in the Southern Ocean, we show that existing deep-ocean radiocarbon records from the glacial period a

218 rease in the residence time of carbon in the deep ocean, rather than an increase in biological carbon

219 The deep-ocean record supports the notion of a bipolar seesa

220 Here we show, using new 2.4-Myr-long Eocene deep ocean records, that the comparatively modest hypert

221 ytoplankton and hence the N : P ratio of the deep ocean remain incompletely understood.

222 l connections between surface waters and the deep ocean remain poorly studied despite the high biomas

223 consistent with previous estimates that the deep ocean remained anoxic throughout the GOE.

224 ic marine basins suggests, however, that the deep ocean remained anoxic until much later.

225 r of particulate organic matter (POM) to the deep ocean remains disputed.

226 ermore, adaptation of archaeal lipids in the deep ocean remains poorly constrained.

227 ~38 to 28 million years ago), accompanied by deep-ocean reorganization attributed to gradual Antarcti

228 Climate Change (UNFCCC) could help to expand deep-ocean research and observation and to protect the i

229 as no upwelling of Se oxyanions from an oxic deep-ocean reservoir, which is consistent with previous

230 Trends suggest that deep-ocean Se oxyanion concentrations increased because

231 are present around hydrothermal vents in the deep ocean seafloor, this process might be relevant, at

232 ctinomycete strain CNQ-418, retrieved from a deep ocean sediment sample off the coast of La Jolla, CA

233 The microbial ecology of oligotrophic deep ocean sediments is understudied relative to their s

234 deglaciation, and the relative importance of deep ocean sequestration in regulating millennial-timesc

235 The implied heat loss in the deep ocean since 1750 CE offsets one-fourth of the globa

236 This deep ocean sink of energy input from the wind is potenti

237 in the Chicxulub crater sediments and at two deep ocean sites indicate a fossil carbon source that ex

238 s, we hypothesize, initial conditions of the deep ocean state that are consistent with observations o

239 rine rejection leads to a strongly increased deep ocean stratification, consistent with high abyssal

240 However, achieving deep-ocean sustainability under the UN Sustainable Devel

241 ant decline in high-latitude sea surface and deep ocean temperature and enhanced seasonality in middl

242 e we present an orbitally resolved record of deep ocean temperature derived from benthic foraminifera

243 We present evidence that their record of deep ocean temperature is not reliable, thus raising dou

244 ghtly lead) global changes in ice volume and deep ocean temperature over the past 3.5 million years.

245 heric carbon dioxide, Antarctic temperature, deep ocean temperature, and global ice volume correlated

246 urface anomalies are associated with ongoing deep-ocean temperature adjustments.

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

248 present a detailed record of North Atlantic deep-ocean temperature, global sea-level, and ice-volume

249 hough containing large effects of changes in deep-ocean temperature.

250 example, saltmarsh ponds, estuaries and the deep ocean than in the overlying seawater.

251 l plume, implying a greater longevity in the deep ocean than previously assumed.

252 d tidal energy needs to be dissipated in the deep ocean than was originally thought.

253 2 million years ago for both the surface and deep ocean that are consistent with an approximately 200

254 uations of species diversity in the tropical deep ocean that are correlated with orbital-scale oscill

255 ight their versatile metabolic strategies in deep oceans that might play a critical role in global ca

256 In the deep ocean, the conversion of methane into derived carbo

257 ow light levels-a pervasive condition in the deep ocean, the largest inhabitable space on the planet.

258 In the deep ocean, the permanent absence of light precludes cur

259 Along with recent measurements of Hg in the deep ocean, these archives indicate that atmospheric Hg

260 In the deep ocean, tides supply much of the mechanical energy r

261 traces the redistribution of carbon from the deep ocean to the atmosphere during deglaciation.

262 pwelling and associated carbon flux from the deep ocean to the atmosphere, a positive feedback loop n

263 f very 'old' ((14)C-depleted) CO(2) from the deep ocean to the atmosphere.

264 Mixing of water masses from the deep ocean to the layers above can be estimated from con

265 sistent with the transfer of carbon from the deep ocean to the surface ocean and atmosphere via a Sou

266 Geochemical evidence invokes anoxic deep oceans until the terminal Neoproterozoic ~0.55 Ma,

267 and 400 Ma is thought to have oxygenated the deep oceans, ushered in modern biogeochemical cycles, an

268 ous records have hinted at a partitioning of deep ocean ventilation across the two major intervals of

269 Deep ocean ventilation and oxygenation around 750 Ma bro

270 These results have implications for deep ocean ventilation and suggest that the interior sub

271 Changes in deep ocean ventilation are commonly invoked as the prima

272 ecosystem were facilitated by restoration of deep ocean ventilation linked mechanistically to a chang

273 ling iron fertilization by dust and enhanced deep ocean ventilation.

274 ir age reconstructions required for accurate deep-ocean ventilation age estimates.

275 e variability, and thus provide estimates of deep-ocean ventilation ages.

276 tion rate together with plausible changes in deep-ocean ventilation and the global carbon cycle durin

277 biological export of carbon and increases in deep-ocean ventilation via southern-sourced water masses

278 make unlikely suggestions that a slowdown in deep-ocean ventilation was responsible for a sizable fra

279 he Earth's albedo, ongoing changes in global deep-ocean ventilation, and the evolution of Southern Oc

280 nteractions in the Earth's subsurface and at deep ocean vents.

281 rge genomic fragments from both surface- and deep-ocean viruses sampled during the Tara Oceans and Ma

282 efore the Bolling-Allerod interstadial), the deep ocean was about three degrees Celsius warmer than s

283 strial-scale dumping of organic waste to the deep ocean was once common practice, leaving a legacy of

284 DDT) and its metabolites in intermediate and deep ocean water masses.

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

286 Therefore, the seamount should retain the deep-ocean water for 1.8 years for the deep-ocean bacter

287 cale ventilation of Southern Ocean CO2-rich, deep-ocean water masses is thought to have been fundamen

288 eamount-associated or 'sheath'-water than in deep-ocean water unaffected by seamounts.

289 e surrounding seafloor, obstruct the flow of deep-ocean water.

290 sants stimulate microbial oil degradation in deep ocean waters and instead highlights that dispersant

291 Hg is primarily recalcitrant soil pools and deep ocean waters and sediments.

292 scale dynamical instabilities by the flow of deep-ocean waters along a steep topographic boundary.

293 usly undocumented mixing mechanism, by which deep-ocean waters are efficiently laundered through inte

294 Redox proxy data indicate the deep oceans were oxygenated during 435-392 Ma, and the a

295 rface ocean conditions are translated to the deep ocean, where decadal peaks in supply, remineralizat

296 le in furnishing the diapycnal mixing in the deep ocean which affects the uptake of heat and carbon b

297 ents 20% of total organic carbon flux to the deep ocean, which constitutes a primary control on atmos

298 ace, sinking in the tropics, and filling the deep ocean with warm water.

299 eparates the productive upper ocean from the deep ocean, yet little is known of its long-term dynamic

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