ライフサイエンスコーパス: deep water

1 of multicellularity, and typically found in deep water.

2 Seaway and intensification of North Atlantic Deep Water.

3 layers while trees have exclusive access to deep water.

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

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

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

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

8 arge amounts of methane accumulate in anoxic deep waters.

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

10 Es was defined by globally pervasive euxinic deep waters.

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

12 bon dioxide that occurs through upwelling of deep waters.

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

14 hese metals after the oxygenation of oceanic deep waters.

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

16 rasting with heavier isotopic composition in deep waters.

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

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

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

20 ground and below-ground organs, magnitude of deep water acquisition (WA(deep) ), shallow absorptive r

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

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

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

24 he La Voulte palaeoenvironment is considered deep water and had a soft substrate, V. parvulus could h

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

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

27 ms (that is, macro- and megafauna) living in deep waters and in benthic habitats, whereas monitoring

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

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

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

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

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

33 Deep-water animals accumulate TMAO to protect proteins,

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

35 00 and 1,400 million years ago, which record deep-water anoxia beneath oxidized surface water.

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

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

38 and informed the creation of fully protected deep-water areas in the Galapagos Marine Reserve that ma

39 e in terrestrial and shallow-water areas; in deep-water areas, in contrast, hydrocarbon seepage is ex

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

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

42 2000 from fixed locations in waist- and knee-deep waters at Chicago 63rd Street Beach, an embayed, ti

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

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

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

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

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

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

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

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

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

52 ne estimates are consistent with the GHGI in deep water but appear higher for shallow water.

53 monia-oxidizing archaea (AOA) are present in deep waters, but the mechanisms that determine ecotype f

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

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

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

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

58 While the retention of deep-water by seamounts is predicted from ocean circulat

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 sest to warm, salty, subsurface, circumpolar deep water (CDW), that is, consistent with enhanced pola

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

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

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

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

67 We suggest that variations in Nordic Seas deep-water circulation are precursors to abrupt climate

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

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

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

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

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

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

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

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

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

77 ethane-saturated oil droplets under emulated deep-water conditions, providing an opportunity to eluci

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

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

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

81 This paper reports a deep-water coral framework (a single colonial bush or a

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

83 as caused by buoyant plumes of nutrient-rich deep waters created by the substantial input of lava int

84 are a valuable endmember when studying this deep water cycle because hydration in Atlantic lithosphe

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

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

87 ntribute to the fates of live oil and gas in deep water, depending on the release conditions.

88 or El Faro rogue waves do in intermediate or deep-water depths.

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

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

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

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

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

94 s in shallow water (e.g., soil water) versus deep waters (e.g., groundwater), inducing primarily flus

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

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

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

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

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

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

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

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

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

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

105 mily Latrunculiidae) recovered during a NOAA deep-water exploration of the Aleutian Islands.

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

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

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

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

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

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

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

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

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

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

116 ure from the prevailing view that changes in deep water formation in the Labrador Sea dominate MOC va

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

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

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

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

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

122 Deep water formation that connects the two limbs of the

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

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

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

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

127 ikely due to rapid changes in North Atlantic deep-water formation and their impact on the global radi

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

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

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

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

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

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

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

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

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

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

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

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

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

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

142 diate waters and a negligible intrusion into deep waters (>1000 m).

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

144 n be incorporated into simulations of future deep-water habitat response to changing environmental co

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

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

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

148 from approximately 10 l water from Yangshan Deep-Water Harbour near the Yangtze River estuary in Chi

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

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

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

152 g and the relatively short residence time of deep water in the Basin.

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

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

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

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

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

158 n deep mixing and enhanced influx of Pacific Deep Water into UCDW, inducing a water mass structure th

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

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

161 We prove deep-water is retained by the seamount by measuring 2.4x

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

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

164 warming, acidification and deoxygenation of deep waters, leading to decreased food availability at t

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

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

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

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

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

170 results from an increase in the size of the deep-water marine phosphorus reservoir, associated with

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

172 -Scotland Overflow Water (ISOW) is a primary deep water mass exported from the Norwegian Sea into the

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

184 In the Amundsen Sea, modified Circumpolar Deep Water (mCDW) intrudes into ice shelf cavities, caus

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 climate system to changes in North Atlantic Deep Water (NADW) formation is fundamental to improving

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

189 Disrupting North Atlantic Deep Water (NADW) ventilation is a key concern in climat

190 the Nd isotope composition of North Atlantic Deep Water (NADW), a major component of the global overt

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

192 Deep-water nutrient injection in the North Pacific Subtr

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

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

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

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

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

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

199 PFAS concentrations in deep waters of the Lake Hazen water column were consiste

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

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

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

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

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

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

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

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

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

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

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

211 ods, and contributions from sinking mid- and deep-water organisms.

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

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

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

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 rained by modern anoxic basins, suggest that deep-water phosphate concentrations may have increased b

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

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

220 In deep water plumes, these communities were initially domi

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

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

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

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

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

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

227 Deep water reaches the upper ocean predominantly south o

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

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

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

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

232 dynamics of gas-saturated live petroleum in deep water remains a challenge.

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

234 aits that emerged from our analysis are: (1) deep water residing (>100 m); (2) cosmopolitan distribut

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

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

237 ation (PMF) analysis, we deduce that Red Sea Deep Water (RSDW) is an unexpected, potent source of atm

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

239 d-Permian extinction horizon, while those in deep-water sections occurred tens of thousands of years

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

241 a reservoir-size quantity of methane from a deep-water seep during the Pliocene, resulting from natu

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

243 er, [Formula: see text], defined in terms of deep-water significant wave height [Formula: see text] a

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

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

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

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

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

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

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

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

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

253 Most ctenophores are pelagic and deep-water species and cannot be bred in the laboratory.

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

255 idence of upwelled hydrothermally influenced deep waters stimulating massive phytoplankton blooms in

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 million years, we found that a reduction in deep water supply and a concomitant freshening of the su

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

262 t reports are mostly based on forests over a deep water table (DWT), which may be particularly sensit

263 ve gas emissions at oil and gas sites with a deep water table.

264 rkedly in diffuse porous species, sites with deep water tables, and in response to late-season drough

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

266 hallow Atlantic waters into colder, fresher, deep waters that move southward in the Irminger and Icel

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

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

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

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

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

274 We show that rates of nutrient supply from deep waters to the photic zone have dramatically increas

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

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

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

278 evel presently occupied by Upper Circumpolar Deep Water (UCDW), toward Nd isotope values more typical

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

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

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

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

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

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

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

286 Using a continuous record of deep water ventilation from the Nordic Seas, we identify

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

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

289 e using time series of still-water level and deep-water wave data from multiple locations around the

290 ve been largely applied to and validated for deep-water waves.

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

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

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

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

295 ropics to high latitudes and from shallow to deep water-which better align with species distributions

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

297 midshipman (Porichthys notatus) migrate from deep-water winter habitats to the intertidal zone in the

298 of deep-sea DOC is several times the age of deep water with a wide range from <100 to >10,000 years.

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.,