ライフサイエンスコーパス: deep ocean

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

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

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

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

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

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

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

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

9 production and carbon sequestration into the deep ocean.

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

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

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

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

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

15 have directly enhanced carbon export to the deep ocean.

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

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

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

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

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

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

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

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

24 o sustained and widespread freshening of the deep ocean.

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

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

27 ion in POC export from surface waters to the deep ocean.

28 re exploration of microbial diversity in the deep ocean.

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

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

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

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

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

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

35 pollutants between the coastal ocean and the deep ocean.

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

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

38 ly efficient at sequestering carbon into the deep ocean.

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

40 r enhance export of picophytoplankton to the deep ocean.

41 enzymes that underpin chemosynthesis in the deep oceans.

42 k of environmental regulatory policy for the deep oceans.

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

59 ately 55.5 million years ago to a warming of deep-ocean and high-latitude surface waters, a large per

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

90 Our data show that the deep ocean changed on decadal-centennial time scales dur

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

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

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

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

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

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

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

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

99 Coherent deep ocean circulation changes were associated with glac

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

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

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

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

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

105 The deep-ocean circulation is responsible for a significant

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

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

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

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

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

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

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

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

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

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

116 down atmospheric CO2 and transport it to the deep ocean could diminish dramatically if predicted incr

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

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

119 for the vertical transport of water into the deep ocean--deep water formation at high latitudes--and

120 Deep-ocean density stratification has been proposed as a

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

142 -30% of the total dissipation--occurs in the deep ocean, generally near areas of rough topography.

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

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

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

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

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

148 1 year, but stabilization of subsurface and deep ocean Hg levels requires aggressive controls.

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

150 The migration and evolution of a deep ocean hydrothermal event plume were tracked with a

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

198 ~38 to 28 million years ago), accompanied by deep-ocean reorganization attributed to gradual Antarcti

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

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

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

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

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

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

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

206 the sedimentary organic carbon (SOC) at two deep ocean sites, and it is 2400 to 13,900 carbon-14 yea

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

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

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

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

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

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

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

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

215 2 million years ago for both the surface and deep ocean that are consistent with an approximately 200

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

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

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

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

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

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

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

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

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

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

226 Deep ocean ventilation and oxygenation around 750 Ma bro

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

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

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

230 predominantly the result of abrupt shifts in deep ocean ventilation.

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

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

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

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

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

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

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

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

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

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

241 t the last glacial cycle, reorganizations of deep ocean water masses were coincident with rapid mille

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

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

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

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

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

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

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

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

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

251 overall cooling of about 12 degrees C in the deep oceans with four main cooling periods.

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