ライフサイエンスコーパス: deep water

1 layers while trees have exclusive access to deep water.

2 hort-term natural release from hydrates into deep water.

3 ; and (4) the case of shallow phosphorus and deep water.

4 tent high-SigmaCO2 state for eastern Pacific deep water.

5 ced mass fractionation within North Atlantic Deep Water.

6 ndently, like linear waves on the surface of deep water.

7 of multicellularity, and typically found in deep water.

8 Seaway and intensification of North Atlantic Deep Water.

9 rasting with heavier isotopic composition in deep waters.

10 arge amounts of methane accumulate in anoxic deep waters.

11 DOM pool, have persisted for 2 years in the deep waters.

12 Es was defined by globally pervasive euxinic deep waters.

13 dwiched within ferruginous [Fe(II)-enriched] deep waters.

14 bon dioxide that occurs through upwelling of deep waters.

15 awater has lower (187)Os/(188)Os values than deep waters.

16 hese metals after the oxygenation of oceanic deep waters.

17 rs and exports them into the thermocline and deep waters.

18 l-oxygenated surface waters and fully anoxic deep waters.

19 make an important contribution to the DOC in deep waters.

20 c matter (DOM), with high optical yields, in deep waters 15 months after the Deepwater Horizon (DWH)

21 probable Fe-sulphide that likely formed in a deep water (500-1,500 m) hydrothermal setting.

22 ating a mixing event by adding nutrient-rich deep water abruptly triggered dense phytoplankton blooms

23 DOM) components could still be identified in deep waters after 2 years of degradation, which is furth

24 ral imply that the nutrient content of these deep waters also increased.

25 d of significantly diminished North Atlantic Deep Water and are able to quantitatively match paleocli

26 owing to reduced upwelling of nutrient-rich deep water and gradual depletion of upper ocean nutrient

27 d carbon export from P. antarctica blooms to deep water and sediments in the Ross Sea.

28 Here we reconstruct changes in deep water and thermocline radiocarbon content over the

29 ffered less between poles and lower latitude deep waters and displayed different diversity patterns c

30 The dramatic mercury loss from deep waters and methylmercury loss from underlying sedim

31 ir-sea heat exchange drives the formation of deep waters and the surface circulation of warm waters a

32 eepwater production at high latitudes, moves deep waters and their attendant properties continuously

33 are physically demanding, require travel to deep waters, and are considered more sustainable.

34 hallow phosphorus; (3) the case of localized deep water; and (4) the case of shallow phosphorus and d

35 he hypolimnia of freshwater lakes leading to deep-water anoxia are still not well understood, thereby

36 00 and 1,400 million years ago, which record deep-water anoxia beneath oxidized surface water.

37 r classes of plankton, including potentially deep-water archaea, were also involved.

38 imum Atlantic are more SigmaCO2-depleted and deep waters are SigmaCO2-enriched compared with the wate

39 floor because they focus on a limited mostly deep-water area of the Gulf, include a conservative esti

40 1) was associated with reduced upwelling of deep waters around Antarctica, thereby allowing CO2 outg

41 e, rather than reduce, the upwelling rate of deep waters around Antarctica.

42 ep decrease in both the upper North Atlantic Deep Water assemblage and species diversity at 13.1 ka a

43 r amounts of these oil-derived components in deep waters, assuming microbial activity on DOM in the c

44 2000 from fixed locations in waist- and knee-deep waters at Chicago 63rd Street Beach, an embayed, ti

45 distinguish shallow-water zooxanthellate and deep-water azooxanthellate fossil corals.

46 ethylthio) nucleoside, was isolated from the deep-water Bahaman tunicate Didemnum sp.

47 era was positioned to look down into a 10-cm-deep water bath that filled its field of view (FOV).

48 and probably fresher than the North Atlantic Deep Water before the intensification of NHG.

49 Deep water below the Western Subarctic Gyre (WSAG) conta

50 change in Pb isotope ratios of North Pacific deep water below the WSAG versus the NPSG.

51 Deep-water benthic communities in the ocean are almost w

52 leocene global events eliminated much of the deep-water benthos.

53 southward transport of lower North Atlantic Deep Water between 3,000 and 5,000 m in depth.

54 More than 80% of potential deep-water biodiversity hotspots known around the world,

55 r-soluble compounds into biologically sparse deep water by 55%, while decreasing the flows of several

56 glacial, reflecting decreased oxygenation of deep water by Antarctic Bottom Water (AABW).

57 tling processes and particles transferred to deep waters by dense shelf water cascading (DSWC).

58 to trace the main nutrient return path from deep waters by upwelling in the Southern Ocean and subse

59 After the spring ascent from deep waters, C. hyperboreus approach equilibrium partiti

60 Plio-Pleistocene transition, as Circumpolar Deep Water (CDW) became the common source.

61 numerical models show that warm Circumpolar Deep Water (CDW) incursions onto the West Antarctic cont

62 e areas of seafloor dominated by Circumpolar Deep Water (CDW).

63 ean and the separation of the North Atlantic Deep Water cell from the Antarctic Bottom Water cell.

64 ation have been inferred from records of the deep water chemical composition derived from sedimentary

65 Atlantic deep water chemical properties are seen to change in as

66 s than to the remainder of the monophyletic, deep-water chrysogorgiid genera.

67 We show that during the last glacial period, deep water circulating around Antarctica was more than t

68 regime, and conclude that the initiation of deep-water circulation from the Norwegian Sea into the N

69 several Holocene Bond events when changes in deep-water circulation occurred.

70 e records indicates that changes in Cenozoic deep-water circulation patterns were the consequence, no

71 s estimates of the date marking the onset of deep-water circulation through this basin-on the basis o

72 of the early Pliocene CAS shoaling phase on deep-water circulation.

73 insic bioremediation of the oil plume in the deep-water column without substantial oxygen drawdown.

74 rine particles (called micro-blebs) from the deep-water column.

75 tage of taller eukaryotic osmotrophs in this deep-water community context has not been addressed.

76 es to the very rare data on OCPs in the vast deep-water compartments and combined with surface water

77 indings represent the first PBDE data in the deep-water compartments of an ocean.

78 Modeled deep water concentrations below 200 m (5-15 pg/L) were s

79 years, there has been a marked shift towards deep-water continental margins (500-2,500 m below sea le

80 We also show that most known deep-water coral communities in the Gulf of Mexico do no

81 ill on offshore ecosystems, 11 sites hosting deep-water coral communities were examined 3 to 4 mo aft

82 ury species and the resettlement of the oxic deep waters, could lead to the enhanced transfer of accu

83 tely 81% and methylmercury concentrations in deep waters decreased by roughly 86% due to destratifica

84 The deep-water deficit in NO(3)(-) was in near-stoichiometri

85 However, species that require deep water did not reach northern regions because of wea

86 ype, as opposed to rock properties, controls deep water drainage for the vegetation transition zone.

87 veals a similar proportion of North Atlantic Deep Water during the 'lukewarm interglacials' and the m

88 olwellia, which also bloomed in situ in Gulf deep waters during the discharge.

89 lution reveals that a water molecule, termed deep water, Dw, and bound in a hydrophobic pocket of the

90 ryotes may have been aerotolerant anaerobes, deep-water dysoxic environments are likely settings for

91 es compelling evidence that the oil impacted deep-water ecosystems.

92 s magnitude, release at depth, and impact to deep-water ecosystems.

93 del predictions, we discovered extensive new deep-water Eisenia galapagensis populations in the Galap

94 ould indicate that a previously unrecognized deep water end member originated along the western margi

95 e analysis reveals that the northern-sourced deep waters enter the Antarctic Circumpolar Current via

96 and recent descriptions of large epibenthic deep-water enteropneusts, Torquaratoridae.

97 adicting the hypothesis that La Voulte was a deep-water environment.

98 but also spatially from the shallow shelf to deep-water environments in tandem with progressive oxyge

99 nshore, diversify offshore, and retreat into deep-water environments.

100 the deep Arctic and may indicate continuous deep-water exchange between the Arctic and Atlantic ocea

101 ound in the Arctic, our records suggest that deep-water exchange through the Fram strait may export (

102 a during the times of reduced North Atlantic Deep Water export.

103 ystem architectures that might contribute to deep-water extraction or to water-saving strategies.

104 t for the jewelry trade and damage caused by deep-water fishing practices.

105 ygen exchange between water and Pi along the deep water flow path.

106 Dating the onset of deep-water flow between the Arctic and North Atlantic oc

107 nces in oceanic gateways, which affect where deep waters form and how they circulate.

108 In the present mode of circulation, deep waters form in the North Atlantic and Southern ocea

109 reduction in the strength of North Atlantic Deep Water formation and attendant cooling of the North

110 the Bering Strait, disrupting North Atlantic Deep Water formation and enhancing sea ice formation.

111 cycle through oscillations in North Atlantic Deep Water formation and northward oceanic heat flux.

112 he catalyst for a decrease in North Atlantic Deep Water formation and subsequent cooling around the N

113 ical transport of water into the deep ocean--deep water formation at high latitudes--and horizontal t

114 Thus, alternation of deep water formation between the Antarctic and the North

115 Lawrence Valley inhibited deep water formation in the subpolar North Atlantic and

116 multicentennial weakening of North Atlantic Deep Water formation occurred only during Heinrich stadi

117 l gyre ~3,000 km south of the North Atlantic deep water formation regions and weakens the AMOC by <15

118 ltwater from the two drainage outlets to the deep water formation regions in the North Atlantic.

119 r meltwater from the Mackenzie Valley to the deep water formation regions of the subpolar North Atlan

120 Deep water formation that connects the two limbs of the

121 s the impact of a slowdown of North Atlantic Deep Water formation, and the geographical extent of the

122 antic Ocean and a slowdown of North Atlantic Deep Water formation--this anomaly provides an opportuni

123 (14)C data sets, implying limited changes in deep water formation.

124 ovarying with the strength of North Atlantic Deep Water formation.

125 hey may have recurrently produced favourable deep-water formation conditions, both increasing salinit

126 at transport in the South Pacific, driven by deep-water formation in the Ross Sea, was largely respon

127 ipolar seesaw with increased Northern-source deep-water formation linked to Northern Hemisphere warmi

128 This shift in the location of deep-water formation persisted for at least 40,000 years

129 ogical pump and circulation in the Antarctic deep-water formation region, whereas global export produ

130 a substantial surface inflow to a region of deep-water formation throughout the Holocene.

131 ation of warming in high-latitude regions of deep-water formation under ice-free conditions.

132 The deep water formed in the Irminger Sea has the characteri

133 of hydrocarbons in laboratory incubations of deep waters from the Gulf of Mexico stimulated Colwellia

134 We attribute the ECR to upwelling of cold deep waters from the Southern Ocean.

135 ates of gravitational particle export near a deep-water front (305 mg Cm(-2)d(-1)) compared with adja

136 kelp habitat and the discovery of expansive deep-water Galapagos kelp forests validate the extent of

137 Shallow-water genera, and two of eight deep-water genera, appear more closely related to other

138 in of Tolypocladium that was obtained from a deep-water Great Lakes sediment sample.

139 In contrast, the deep water (>1000 m) Pb concentrations were lower (6-37

140 fs may share many characteristics with their deep-water (>30 m) mesophotic equivalents and may have s

141 low through to higher trophic levels even in deep water habitats.

142 ing birds forage in a gradient from shelf to deep-water habitats.

143 Thaumarchaeota from Arctic deep waters had a higher abundance of urease genes than

144 apparently had no effect on central Pacific deep-water hafnium.

145 ium isotopic compositions of central Pacific deep water has been obtained from two ferromanganese cru

146 e iron isotope composition in North Atlantic Deep Water has changed substantially over the past 6 mil

147 Where deep water has direct access to grounding lines, glacier

148 glaciers that terminate in warm Circumpolar Deep Water have undergone considerable retreat, whereas

149 is a primary factor driving the expansion of deep-water hypoxia in lakes during the Anthropocene.

150 observation suggests that the provenance of deep water in the Atlantic Ocean can be decoupled from v

151 a "chemical divide" between intermediate and deep water in the glacial Atlantic Ocean, which indirect

152 waters produced in the northern Atlantic and deep water in the Pacific appears to have been larger th

153 n of marine biological production sinking to deep water in the postextinction ocean.

154 ular weight fraction of DON from surface and deep water in three ocean basins show substantial enrich

155 red between ~15 and 14 Ma in intermediate to deep waters in each basin.

156 gesting a century-scale replacement time for deep waters in the Arctic Ocean since the most recent gl

157 ents is consistent with a residence time for deep waters in the Atlantic only slightly greater than t

158 was characterized by pronounced formation of deep waters in the NW Atlantic.

159 The production of cold, deep waters in the Southern Ocean is an important factor

160 was due to the resumption of North Atlantic Deep Water influence in the Southern Ocean.

161 um fluid mass became channeled into a stable deep-water intrusion at 900- to 1,300-m depth, as aqueou

162 10(6) cubic meters per second of ventilated deep water is currently being produced.

163 Recovery from disturbance in deep water is poorly understood, but as anthropogenic im

164 The predictability of deep-water kelp habitat and the discovery of expansive d

165 mediate Atlantic Water Layer, and the Arctic Deep Water Layer) are 158 +/- 77 kg, 6320 +/- 235 kg and

166 Oxygen consumption in its deep waters leads to the buildup of sulfide from sulfate

167 sibly a result of their low growth rates and deep-water lifestyle - has allowed frameshift insertions

168 sulting in adaptations that enable vision in deep water light environments.

169 pecies richness was highly variable for both deep water macro- and meio- fauna along latitudinal and

170 by 1-5-m-thick 'cap carbonates' (particulate deep-water marine carbonate rocks) associated with a pro

171 ical adaptations to contrasting shallow- and deep-water marine environments and might be considered i

172 emical investigation of a new species of the deep-water marine sponge Leiodermatium, collected by man

173 otentially explain the convergence of global deep water mass properties at the Plio-Pleistocene trans

174 significant change, with the convergence of deep water mass properties in the North Pacific and Nort

175 turning strength proxies shows that both the deep water mass source and the overturning rate shifted

176 tracer protactinium/thorium (Pa/Th) with the deep water-mass tracer, epibenthic delta(13)C.

177 (144 +/- 40 t), intermediate (5 +/- 1 t) and deep water masses (30 +/- 2 t) storing 98% of the PCBs i

178 his study we show that this rearrangement of deep water masses is dynamically linked to the expansion

179 ategy, we show that bacterial communities of deep water masses of the North Atlantic and diffuse flow

180 igher concentrations in the intermediate and deep water masses than in surface waters.

181 partments, with no reports yet for the large deep-water masses of the Arctic Ocean.

182 In deep-water masses, summation operator14PBDE concentratio

183 ration of light into the sulphide-containing deep water may result in a zone of anaerobic primary pro

184 Propane and ethane trapped in the deep water may therefore promote rapid hydrocarbon respi

185 Atlantic involving changes in North Atlantic Deep Water (NADW) and Antarctic Bottom Water (AABW) play

186 for the predicted increase in North Atlantic Deep Water (NADW) formation exists in the Caribbean and

187 tion coincided with increased North Atlantic Deep Water (NADW) formation, and the subsequent reinvigo

188 ided with strong increases in North Atlantic Deep Water (NADW) production and inferred warming (inter

189 ing and the loss of the modern North Pacific Deep Water (NPDW) mass in climate models of the warmest

190 Deep-water nutrient injection in the North Pacific Subtr

191 as contributed to reduced mixing, decreasing deep-water nutrient upwelling and entrainment into surfa

192 rate that ventilation of EEP thermocline and deep waters occurred synchronously during the last degla

193 ea level changes enhances the instability of deep-water oceanic sediments, and thus human activities

194 degrees S to the mixed layer is 60-90 years.Deep waters of the Atlantic, Pacific and Indian Oceans u

195 rth Sea temporally re-establish oxic life in deep waters of the Baltic Sea.

196 covery of four new Xenoturbella species from deep waters of the eastern Pacific Ocean is reported her

197 bution of carbonate ion concentration in the deep waters of the equatorial ocean on the basis of diff

198 SUP05 populations in hydrothermal plumes and deep waters of the Gulf of California enabled detailed p

199 The diversity, ubiquity and prevalence in deep waters of the octocoral family Chrysogorgiidae Verr

200 Total mercury concentrations in the deep waters of the south arm decreased by approximately

201 malously enriched in mercury relative to the deep waters of the South Atlantic, Southern and Pacific

202 ed from Conus pergrandis, a species found in deep waters of the Western Pacific.

203 ep convection, one of the processes by which deep waters of the world's oceans are formed, is restric

204 y widespread and diverse coral ecosystems in deep waters on continental shelves, slopes, seamounts, a

205 A simple theory further suggests that these deep waters only came to the surface under sea ice, whic

206 he delivery of oxygen-poor and nutrient-rich deep water onto continental shelves.

207 cks amplified by the delivery of Circumpolar Deep Water onto the continental shelf.

208 arger, expandable detectors in, for example, deep water or ice.

209 years), large (>100 km(2)), and isolated by deep water or sand.

210 lastics are already becoming integrated into deep-water organisms.

211 sil records indicate neogastropods to have a deep-water origin, suggesting shallow-water species may

212 As a consequence of this climate shift, new deep waters outflowing through Gibraltar will impact the

213 by methanotrophic bacteria in Gulf of Mexico deep waters over a 4-month period.

214 numbers and relative species abundance, and deep-water oxygen declines) in areas of restricted water

215 These findings support the view that deep-water pathways along and across density surfaces in

216 Mapped accessibility data revealed deep water penetration through hHv1, suggesting a highly

217 The observed near equilibration of deep water Pi likely calls for continued slow rates of m

218 tion of this old and presumably CO2-enriched deep water played an important role in the pulsed rise o

219 In deep water plumes, these communities were initially domi

220 y have affected production of North Atlantic Deep Water, potentially providing an additional mechanis

221 t between the carbonate ion concentration in deep waters produced in the northern Atlantic and deep w

222 entide Lakes, which disrupted North Atlantic Deep Water production and subsequently altered monsoonal

223 If this is true, a seesawing of deep water production between the northern Atlantic and

224 A major reduction in Southern Ocean deep water production during the 20th century (from high

225 cial weakening or shutdown of North Atlantic Deep Water production, whereas other proxies, such as Cd

226 gional ocean hindcast links SCFR to enhanced deep-water production and in turn to strengthened Medite

227 re, and influences vertical ocean structure, deep-water production and the global distribution of nut

228 n the Pacific Ocean that indicate a shift in deep-water production from the Southern Ocean to the Nor

229 Net deep-water production rates amount to (15 +/- 12) x 10(6

230 deep western boundary current to reconstruct deep-water properties and speed changes during the Pleis

231 tracers supports a different distribution of deep-water properties, including density, which is dynam

232 Newly applied radiocarbon age dates from the deep water proteinaceous corals Gerardia sp. and Leiopat

233 Because deep water provides refuge against ultraviolet radiation

234 Here we present a record of North Atlantic deep-water radiocarbon ventilation, which we compare wit

235 Deep water reaches the upper ocean predominantly south o

236 hs, which remains particularly suggestive of deep-water refugia effects in the MHI.

237 tions of aquatic taxa from marsh habitats to deep-water refugia in estuaries.

238 dominate and sessile forms are restricted to deep-water refugia.

239 diment organic matter in a 2.4 x 10(10) m(2) deep-water region surrounding the spill site indicate th

240 Biological observations from the deep-water remotely operated vehicle Isis in the austral

241 t system used more surface, mesopelagic, and deep waters, respectively.

242 The source of deep waters reverted back to the Southern Ocean 40 Myr a

243 round New Zealand are diverse with extremely deep waters, seamounts and submarine canyons that are su

244 The siderite enrichment that we observe in deep-water sediments is consistent with a stratified ear

245 ration rose most rapidly when North Atlantic Deep Water shoaled and stratification in the Southern Oc

246 te: specifically, diatoms thrive by 'mining' deep-water silicate brought to the surface by an unstabl

247 nue to observe fluorescent DOM components in deep waters, similar to those of degraded oil observed i

248 littoral sediment) and were very abundant at deep-water sites (profundal sediment).

249 in water, we examined the use of synthetic, deep water-soluble cavitands in the Staudinger reduction

250 A deep, water-soluble cavitand extracts a variety of neutr

251 ent bottleneck for lake trout by providing a deep water source of food where little was available pre

252 Comparison of our deep water source record with overturning strength proxi

253 -temperature physiological boundaries of the deep-water Southern Ocean environment.

254 into far-northern latitudes and returns cold deep waters southward across the Equator.

255 shikamides C-H, were isolated from different deep-water specimens of Theonella swinhoei and Theonella

256 ck between poleward transport of Circumpolar Deep Water, subsurface warming and AIS melt, suggesting

257 7)Os/(188)Os ratio (approximately 0.95) than deep waters, suggesting that human activities have alter

258 rs and an increase in the age of circumpolar deep waters, suggesting that the formation of the Antarc

259 The recent discovery of a deep-water sulfur-cycling microbial biota in the approxi

260 We observe a rejuvenation of circumpolar deep waters synchronous and potentially contributing to

261 carbon dioxide, Vostok air temperature, and deep-water temperature are in phase with orbital eccentr

262 ord is heavily contaminated by the effect of deep-water temperature variability, but by using the Vos

263 ecord, the delta(18)O signals of ice volume, deep-water temperature, and additional processes affecti

264 e previous glacial cycle the conclusion that deep-water temperatures were colder during glacial perio

265 of lethally warm, shallow waters and anoxic deep waters that acted to severely restrict the habitabl

266 of formation of North Atlantic and Antarctic Deep Water (the 'bipolar seesaw').

267 there were no return path of nutrients from deep waters, the biological pump would eventually deplet

268 Despite low concentrations in deep water, this reservoir is expected to contain most o

269 For decades, upward hydraulic lift (HL) of deep water through roots into dry, litter-rich, surface

270 eductions in the formation of North Atlantic Deep Water, thus providing a mechanism for observed clim

271 om the southernmost extent of North Atlantic Deep Water to reconstruct gateway-related changes in the

272 sults directly link increased ventilation of deep water to the deglacial rise in atmospheric CO2.

273 The supply of deep water to the Pacific Ocean is presently dominated b

274 e conclude that the export of North Atlantic Deep Water to the Southern Ocean has resembled present-d

275 The timescale for half of the deep water to upwell from 30 degrees S to the mixed laye

276 Upwelling of global deep waters to the sea surface in the Southern Ocean clo

277 rich ecosystems are mounting: The impacts of deep-water trawling are already widespread, and effects

278 alapagos kelp forests validate the extent of deep-water tropical kelp refugia, with potential implica

279 igmaCO2-depleted North Atlantic intermediate/deep water turns northward around the southern tip of Af

280 e the sustained production of North Atlantic Deep Water under glacial conditions, indicating that sou

281 tiated the Gibraltar Strait, and remained in deep water until they reached the Atlantic Ocean, when t

282 ecipitation reduction, but juniper increased deep water uptake and pinon increased shallow water upta

283 at both locations, which partly derive from deep water upwelled in the Southern Ocean, became a sign

284 There is growing evidence that the amount of deep water upwelling at low latitudes is significantly o

285 , suggesting that CO(2) released by means of deep water upwelling in the Southern Ocean lost most of

286 ce water stratification, renewed Circumpolar Deep Water upwelling, and advection of low delta13C wate

287 ocean, dissolved/particle interactions, and deep water upwelling.

288 Here we use a box model with deep-water upwelling confined to south of 55 degrees S t

289 remain higher at some stations than typical deep-water values for the GOM.

290 ventilation rate of the North Atlantic upper deep water varied greatly during the last deglaciation.

291 Both shallow- and deep-water ventilation ages drop across the last deglaci

292 spheric CO2 levels might result from reduced deep-water ventilation associated with either year-round

293 The cause of this deglacial deep-water warming does not lie within the tropics, nor

294 We show that North Pacific deep waters were substantially colder (4 degrees C) and

295 ofiling platforms enable self-calibration in deep waters where pH values are stable.

296 s sequence were deposited in well-oxygenated deep waters whereas the youngest were deposited in euxin

297 onsequences of the oxygenation of Baltic Sea deep waters, which are the coprecipitation of mercury sp

298 While no commercial-scale deep water wind farms yet exist, our results suggest tha

299 -3,600 m water depth, we find (14)C-depleted deep waters with a maximum glacial offset to atmospheric

300 Upwelling of anoxic deep waters would have supplied reduced N species (i.e.,