ライフサイエンスコーパス: pCO2

1 , pCO2 2260 microatm) and severe OA (pH 7.1, pCO2 5584 microatm; and 6.7, pCO2 18480 microatm) on oys

2 OA compared to control conditions (pH 8.14; pCO2 470 muatm) for both species.

3 H values of 7.77 (pCO2 1400 muatm) and 7.47 (pCO2 3000 muatm)) upon copper toxicity responses in earl

4 we investigated effects of moderate (pH 7.5, pCO2 2260 microatm) and severe OA (pH 7.1, pCO2 5584 mic

5 ere OA (pH 7.1, pCO2 5584 microatm; and 6.7, pCO2 18480 microatm) on oyster gametogenesis, fertilizat

6 Here, we show that OA (pH 7.71; pCO2 1480 muatm) significantly increases the toxicity re

7 he impact of OA (seawater pH values of 7.77 (pCO2 1400 muatm) and 7.47 (pCO2 3000 muatm)) upon copper

8 cally migrating adult Calanus spp. crossed a pCO2 range of >140 muatm daily and showed only minor res

9 ined in the surface waters and experienced a pCO2 range of <75 muatm, showed significantly reduced ad

10 ndent and combined impacts of acidification (pCO2 = 424-426, 888-940 ppm-v) and warming (T = 28, 32 d

11 he corresponding gas pressures of CO2 alone (pCO2 approximately 3.6 bar) imply 60% saturation relativ

12 ation was depressed ~78% compared to ambient pCO2 .

13 gher under elevated pCO2 compared to ambient pCO2 .

14 Euramerica occurred in step with climate and pCO2 shifts, illustrating the biotic impact associated w

15 es is only the controlling factor of DIC and pCO2 concentrations.

16 solution compositions, with identical pH and pCO2, were used to precipitate an ordered, stoichiometri

17 n responses to both elevated temperature and pCO2 .

18 ment the combined effects of temperature and pCO2 on insect herbivory.

19 mbined stressors of elevated temperature and pCO2 were measured over a 24-day period in four Pacific

20 ies, was insensitive to both temperature and pCO2 within the levels tested here.

21 d large daily variations in pH (>1 unit) and pCO2 (>2000 ppm) and average pH values (pHT 7.73) much b

22 ts record the effects of climate warming and pCO2 rise across the twentieth century.

23 In sham-operated animals, pCO2 was 49.7 +/- 8.2 mmHg.

24 o be a net long-term effect of anthropogenic pCO2 increase and warming temperatures.

25 systems suffering chronic metal pollution as pCO2 levels rise and drive a reduction in seawater pH.

26 Atmospheric pCO2 is predicted to rise from 400 to 900 ppm by year 21

27 ea, and nutrient utilization and atmospheric pCO2 are tightly linked.

28 ire, organic carbon isotope, and atmospheric pCO2 data from early dinosaur-bearing strata of low pale

29 till present in central Asia and atmospheric pCO2 much higher.

30 ea surface temperature (SST) and atmospheric pCO2 values from pelagic sequences preceding and spannin

31 studied palaeosols to constrain atmospheric pCO2 between 2.75 and 2.2 Gyr ago.

32 riven predominantly by declining atmospheric pCO2 levels.

33 rriers resulting from decreasing atmospheric pCO2 levels.

34 re more important in determining atmospheric pCO2 than low latitudes, despite their much smaller area

35 m "greenhouse" climates and high atmospheric pCO2.

36 e response to a rapid decline in atmospheric pCO2 at the EOT.

37 e contributed to the increase in atmospheric pCO2 at these times.

38 Atlantic lags the second rise in atmospheric pCO2 during the late deglacial period.

39 usally linked with a 90% drop in atmospheric pCO2 during the Late Palaeozoic era.

40 A large and rapid drop in atmospheric pCO2 has been proposed as the driving force behind extin

41 caused by a gradual decrease in atmospheric pCO2 in response to solar brightening, alongside a decre

42 acial-interglacial variations in atmospheric pCO2 invoke a significant role for the deep ocean in the

43 millennial-scale variability in atmospheric pCO2 over the past 800 kyr.

44 ults would necessitate a rise in atmospheric pCO2 to levels three to four times as high as those esti

45 ly resulted in the first rise in atmospheric pCO2, whereas the density destratification of the deep S

46 was triggered by a reduction of atmospheric pCO2 that enabled the rapid buildup of a permanent ice s

47 luence of silicate weathering on atmospheric pCO2 levels on geologically short timescales (10(3)-10(5

48 additional negative feedback on atmospheric pCO2 levels.

49 effects of glacial weathering on atmospheric pCO2, we use a solute mixing model to predict the ratio

50 ospheres (over twice the present atmospheric pCO2) in a warmer low-latitude Cretaceous ocean would ha

51 anerozoic, coinciding with rapid atmospheric pCO2 increase and significant loss of biodiversity in ma

52 s iron carbonate, indicates that atmospheric pCO2 must have been less than 10(-1.4) atm--about 100 ti

53 ropical Pacific Ocean shows that atmospheric pCO2 was probably similar to modern concentrations or sl

54 into the future, with respect to atmospheric pCO2 .

55 sted of the injection of a solution at 4 bar pCO2 into a capillary tube packed with crushed calcite.

56 CAi activity determines the coupling between pCO2 (a function of tumor perfusion) and pHi (a potent m

57 much less certain, and the relation between pCO2 and climate remains poorly constrained.

58 Hypercapnia (elevated blood pCO2 > approximately 50 mm Hg) is a feature of several l

59 ic (most rapid and least dependent on breath pCO2) for ammonia, relative to time to attain complete n

60 te and the magnitude of pH change induced by pCO2 enrichment.

61 Delta(13) C in response to twentieth century pCO2 rise, a significant negative relationship (r = -0.5

62 ion show heterogeneous responses to changing pCO2 and ocean temperatures, with some records showing a

63 ges in sea surface partial pressure of CO2 ( pCO2 , calculated from the measured pH and total alkalin

64 higher partial pressures of atmospheric CO2 (pCO2 = 400 and 1000 ppmv).

65 on equation for the partial pressure of CO2 (pCO2 ) in lakes as a function of lake area, terrestrial

66 th a relatively low partial pressure of CO2 (pCO2) close to flue gas conditions.

67 known about how the partial pressure of CO2 (pCO2) in freshwater will be affected by climate change.

68 reasing atmospheric partial pressure of CO2 (pCO2) is a major threat to coral reefs, but some argue t

69 arth's history, the partial pressure of CO2 (pCO2) is much less certain, and the relation between pCO

70 Medians of partial pressures of CO2 (pCO2), pCH4 and pN2O were presented 864 muatm, 6.3 muatm

71 red low-atmospheric partial pressure of CO2 (pCO2).

72 re [measured as the partial pressure of CO2 (pCO2)] affects the content of the surface ocean, which i

73 ation [800 microatm partial pressure of CO2 (pCO2)] during the development and growth of an important

74 , 929-3223 muM) and partial pressure of CO2 (pCO2, 50-1313 muatm) observed over seven years.

75 of increasing atmospheric CO2 concentration (pCO2 ) and temperature on high-latitude forests are poor

76 small, low-cost unit for in situ, continuous pCO2 monitoring.

77 Microvascular oxygen pressure in the cortex (pCO2) was measured by quenching of phosphorescence.

78 ng for C4 photosynthesis in maize at current pCO2, it likely maintains high rates of photosynthesis w

79 perm competitiveness, but only under current pCO2 levels.

80 ental conditions were set at either current (pCO2 370 muatm) or end-of-the-century OA (pCO2 1,100 mua

81 antarctica) through exposure to present day pCO2 conditions and two potential future OA states (750

82 lag in the temperature response to declining pCO2.

83 nd with their natural exposures to different pCO2 ranges.

84 rent resilience to increased carbon dioxide (pCO2 ) concentrations has supported the view that copepo

85 tial pressure of atmospheric carbon dioxide (pCO2) and Paleogene climate is poorly resolved.

86 ospheric partial pressure of carbon dioxide (pCO2) and tropical marine surface temperatures during th

87 DIC and partial pressure of carbon dioxide (pCO2) associated with greater amounts of these oil-deriv

88 00 muatm partial pressure of carbon dioxide (pCO2) significantly increased not only otolith size (up

89 developed in the north central bay drew down pCO2, causing bloom waters to become a CO2 sink while th

90 Elevated pCO2 significantly increased the growth rates of Gracila

91 cypress (Taxodium distichum) at an elevated pCO2 of 80 Pa compared with controls at 40 Pa.

92 osed to ambient ( 400 microatm) and elevated pCO2 ( 2500 microatm) and/or subjected to competition wi

93 ever, the increase in metal flux at elevated pCO2 was equal between the reference and contaminated se

94 tion by UCYN-A is not stimulated by elevated pCO2 , then future increases in CO2 and warming may alte

95 e estuarine autotrophs benefit from elevated pCO2, the benefit can change when direct competition wit

96 to date have focused on impacts of elevated pCO2 on plankton and macrophytes, and have shown that ph

97 Offspring of elevated pCO2-treatment adults were significantly more vulnerable

98 ver, juveniles that were exposed to elevated pCO2 as larvae grew less than control individuals, repre

99 ly increased growth when exposed to elevated pCO2 but significantly slower growth when competing with

100 ngly affected by larval exposure to elevated pCO2 conditions.

101 sons of the short-term responses to elevated pCO2 in seaweeds with different life-history strategies

102 to study the effects of exposure to elevated pCO2 on trait-shifts observed throughout natural populat

103 sis and growth rates in response to elevated pCO2 the most, whereas longer-lived perennial species sh

104 acutely toxic to C. volutator under elevated pCO2 (1140 muatm).

105 netic variation for body size under elevated pCO2 , indicating that this trait can evolve.

106 ay increase nitrogen fixation under elevated pCO2 .

107 t calcification only at night under elevated pCO2 .

108 with dissolution ~86% higher under elevated pCO2 compared to ambient pCO2 .

109 ntrols on calcite dissolution under elevated pCO2 conditions.

110 gellates outcompeting diatoms under elevated pCO2.

111 ver, empirical studies using stable endpoint pCO2 concentrations find species exhibit variable biolog

112 strong stratification were found to enhance pCO2 accumulation, while in Petermann Fjord biological C

113 proxies challenges the notion that episodic pCO2 drawdown drove this major Cenozoic climate transiti

114 n/calcium ratios in foraminifera to estimate pCO2 during major climate transitions of the past 20 mil

115 s a proxy for winter conditions, we examined pCO2 dynamics from the onset of sea-ice melt to summer.

116 cells with high CAi activity, extracellular pCO2 fluctuations evoked faster and larger pHi oscillati

117 physiological traits (such as extracellular pCO2 or aerobic scope) cannot be distinguished.

118 cell pHi from non-steady-state extracellular pCO2.

119 Using IPCC data for pCO2 and pH under four future emissions scenarios (to th

120 Freshwater pCO2 varies across systems and is controlled by a divers

121 Although future freshwater pCO2 levels remain uncertain, studies have considered th

122 ing a better understanding of how freshwater pCO2 levels are regulated and how these levels may impac

123 ic CO2 may also indirectly impact freshwater pCO2 levels in a variety of systems by affecting other c

124 spheric CO2 may directly increase freshwater pCO2 levels in lakes, but rising atmospheric CO2 may als

125 by different factors and that the initial G(pCO2) is a modest predictor of ventilatory acclimatizati

126 surements prior to sustained hypoxia, only G(pCO2) predicted the subsequent rise in ventilation and c

127 apnia, the latter divided into peripheral (G(pCO2)) and central (G(cCO2)) components.

128 For G(pO2), G(pCO2) and G(cC O2), but not the sensitivity of PASP to a

129 High pCO2 altered biofilm development, allowing serpulids to

130 rown under predicted future (year 2050) high pCO2 (589 muatm) using Electron microprobe and NanoSIMS

131 Such a reaction progression at high pCO2 suggests that over long term the hydrated Mg-carbon

132 slightly acidic conditions generated at high pCO2.

133 a spp., may be more sensitive to future high pCO2 conditions compared with the more widely studied la

134 intermediate-scale pCO2 change and, if high pCO2 is relieved mid-succession, whether past acidificat

135 mportance of the timing and duration of high pCO2 exposure (i.e., discrete events at different stages

136 2 levels (from greenhouse conditions of high pCO2 in the Eocene to low pCO2 ice-house conditions in t

137 r are worsened by departures from prior high pCO2 conditions to which organisms had acclimatized.

138 respiration of organic matter produced high pCO2, resulting in Florida Bay being a CO2 source to the

139 esistance traits measured, plants under high pCO2 conditions had a lower leaf N content but higher su

140 s due to higher maintenance costs under high pCO2-environments.

141 tratified water column with suboxic and high-pCO2 bottom waters to a fully mixed and ventilated state

142 It is proposed that an extremely high-pCO2 atmosphere can result in highly (17)O-depleted atmo

143 tant component of fitness) under future high-pCO2 /low-pH conditions.

144 nder low pCO2 , and 0.50 +/- 0.30 under high-pCO2 conditions.

145 subtle differences in larval size under high-pCO2 rearing conditions, consistent with local adaptatio

146 Blood parameters (pH, Na(+), iCa, pCO2, pO2, glucose, Hct, lactate) and muscle pH confirm

147 Marine records show that the drop in pCO2 during this interval was accompanied by a significa

148 The fall in pCO2 likely allowed for a critical expansion of ice shee

149 study examines the effects of an increase in pCO2 (partial pressure of CO2) on groundwater chemistry

150 Here we show that an increase in pCO2 in the arterial blood triggers the immediate releas

151 ming event linked to a transient increase in pCO2, was comparable in rate and magnitude to modern ant

152 ew CO2 data showing significant increases in pCO2 (up to 800 muatm in Lake Michigan) and CO2 emission

153 mate was much more sensitive to increases in pCO2 than has been thought, or that one or more greenhou

154 s) and high (business-as-usual) increases in pCO2.

155 analog for the current anthropogenic rise in pCO2.

156 uments covariance between inferred shifts in pCO2, temperature, and ice volume consistent with greenh

157 revealed significant spatial variability in pCO2 , driven by differences in temperature, freshwater

158 term acclimatization to natural variation in pCO2 .

159 weathering modulated by initially increased pCO2 levels would have operated as both a direct and ind

160 pecific variability in response to increased pCO2 and changes in species interactions.

161 reduced growth during exposure to increased pCO2, abalone settlement was unaffected by prior CCRA ex

162 affected by prior CCRA exposure to increased pCO2.

163 ed by fluorescence, improved under increased pCO2 conditions after 60 days, although these difference

164 Increased algal productivity under increased pCO2 provided more food at the vent, resulting in higher

165 within a context of elevated and increasing pCO2 and pervasive wildfires.

166 However, increasing pCO2 may alter the bacterial community of marine organis

167 he other half being attributed to increasing pCO2 .

168 d towards lower growth rates with increasing pCO2 .

169 crophyte distribution shifts with increasing pCO2.

170 leveled off with decreasing hypoxia-induced pCO2 in awake rats, but monotonically decreased in anest

171 During hypoxia and ischemia, pCO2 decreased to 6.3 +/- 1.8 mmHg and 10.2 +/- 2.7 mmHg

172 ion, circumboreal map (0.5 degrees ) of lake pCO2 .

173 both species were subjected to high and low pCO2 conditions during gametogenesis.

174 conditions of high pCO2 in the Eocene to low pCO2 ice-house conditions in the Oligocene-Miocene) and

175 of size was 0.40 +/- 0.32 (95% CI) under low pCO2 , and 0.50 +/- 0.30 under high-pCO2 conditions.

176 ximately 40.53 Pa) and contrast with the low-pCO2 conditions under which C4 plants expanded their ran

177 h size (up to 25% larger area) at the lowest pCO2 levels reported to date, as well as the first repor

178 ental data and their response to manipulated pCO2 conditions (OA exposures).

179 rstood due to the difficulty of manipulating pCO2 at the ecosystem level to mimic realistic fluctuati

180 Marine pCO2 enrichment via ocean acidification (OA), upwelling

181 o realistically variable scenarios of marine pCO2 enrichment.

182 tion scenarios (380, 550, 750, 1000 microatm pCO2).

183 Beyond that, at 1000 microatm pCO2, biomineralisation continued but with compensated m

184 ter six months of incubation at 750 microatm pCO2, reduced carbonic anhydrase protein activity and sh

185 l and biogeochemical processes in modulating pCO2 , suggesting significant regional differences in CO

186 50% increase in hearing range at 2,100 muatm pCO2, which may alter the perception of auditory informa

187 decline in nauplii recruitment at 1000 muatm pCO2 .

188 d under acidification conditions (1000 muatm pCO2) compared to present day conditions (380 muatm pCO2

189 investigated the impacts of OA (+1000 muatm pCO2) on sperm competitiveness for the sea urchin Parace

190 (year 2100 scenario) with LC50 at 1084 muatm pCO2 .

191 d projected conditions of OA (390-1140 muatm pCO2 ).

192 e reference sediment, but only at 1140 muatm pCO2 .

193 were maintained under ambient and 1200 muatm pCO2 for 7 weeks, and net calcification rates were measu

194 and swimming activity at 800 and 2100 muatm pCO2 .

195 ompared to present day conditions (380 muatm pCO2).

196 ore extreme scenarios of 3500 and 5400 muatm pCO2 , cobia exhibited significantly reduced size-at-age

197 ed to the contaminated sediment at 750 muatm pCO2 , as well as increased DNA damage in organisms expo

198 Estimated relative mass in 800 muatm pCO2 treatments was 14% greater, and there was a similar

199 ic (pO2 approximately 100 Torr) normocapnia (pCO2 approximately 30 Torr, pH approximately 7.4) is com

200 In the dark, during normocapnic (pCO2=35 Torr, pHo=7.4) normoxia (pO2=100 Torr), high pCO

201 t (pCO2 370 muatm) or end-of-the-century OA (pCO2 1,100 muatm) scenarios, crossed in an orthogonal ex

202 Anthropogenic CO2 is expected to drive ocean pCO2 above 1,000 muatm by 2100 - inducing respiratory ac

203 The evolution of surface ocean pCO2 in key locations can therefore provide important cl

204 We calculate that an oceanic pCO2 level of > 800 microatmospheres (over twice the pre

205 ects persist, are reversed by alleviation of pCO2 stress, or are worsened by departures from prior hi

206 lly improved by accounting for the effect of pCO2 on discrimination (r(2) = 0.67, P = 0.002, n = 11).

207 gh early (pretransplant) negative effects of pCO2 on recruitment of these worms were still detectable

208 Increasing levels of pCO2 within the oceans will select for resistant organis

209 t to make predictions about future levels of pCO2.

210 The map of pCO2 was combined with lake area from the recently publi

211 : current (control: pH 8.052, 384.1 muatm of pCO2), a high CO2 treatment approximating the 0.2-0.3 un

212 for 2100 (high CO2: pH 7.830, 666.0 muatm of pCO2), and an intermediate medium CO2 (pH 7.967, 473.4 m

213 mediate medium CO2 (pH 7.967, 473.4 muatm of pCO2).

214 ntested hypothesis that the natural range of pCO2 experienced by an organism determines its sensitivi

215 were no significant drug or task effects on pCO2 or on global blood flow.

216 ell as perfusate gases and electrolytes (pH, pCO2, pO2, O2 saturation, Na(+), K(+), Cl(-), Ca(2+), HC

217 mption, renal vascular resistance (RVR), pH, pCO2, and perfusion pressure were measured.

218 is currently in flux, including seawater pH, pCO2, temperature, redox chemistry, irradiance and nutri

219 to each lung block was analyzed for pH, pO2, pCO2, and hematocrit to follow alterations in support ra

220 2 solubility at high latitude, the preceding pCO2 measurements translate into Antarctic surface-water

221 was 25 to 40 meters higher than at present, pCO2 appears to have been similar to modern levels.

222 There is a high carbon dioxide pressure (pCO2) in distal parts of the gland, and a CO2 analogue i

223 aint on the carbon dioxide partial pressure (pCO2) in ancient atmospheres.

224 ult in fluctuations of CO2 partial pressure (pCO2) that disturb cytoplasmic CO2-HCO3(-)-H(+) equilibr

225 er current or elevated CO2 partial pressure (pCO2).

226 atmospheric carbon dioxide partial pressure (pCO2).

227 , 30.3 degrees C) and CO2 partial pressures (pCO2 ) (400, 900, 1300 muatm).

228 depletion develops at CO2 partial pressures (pCO2 levels) that are often below that of the present at

229 The projected pCO2 concentrations increased the flux of nickel and zin

230 extracted from deep sea cores to reconstruct pCO2 from the middle Eocene to the late Oligocene (appro

231 of development respond to intermediate-scale pCO2 change and, if high pCO2 is relieved mid-succession

232 cultures under control and elevated seawater pCO2 concentrations, quantified settlement success and s

233 ses significantly (by 2-4%) at high seawater pCO2 relative to modern in both genotypes, and also incr

234 in future environments, i.e. higher seawater pCO2 .

235 Increased seawater pCO2 , and in turn 'ocean acidification' (OA), is predic

236 Increasing seawater pCO2 leads to ocean acidification (OA) with a reduction

237 reases significantly (by 4%) at low seawater pCO2 in one genotype.

238 varies significantly in response to seawater pCO2 in two genotypes of Porites lutea, whilst Porites m

239 ate reconstruction), cultured under seawater pCO2 reflecting modern, future (year 2100) and last glac

240 and rates of photosynthesis under subambient pCO2 are significantly impaired in the mutants.

241 esent a 135-kyr record of shallow subsurface pCO2 and nutrient levels from the Norwegian Sea, an area

242 ore the EOT and, superimposed on a long-term pCO2 decline, drove the Earth system toward a glacial ti

243 Our results demonstrate that pCO2 ranged between 1000 to 1500 parts per million by vo

244 roximately 250,000 measurements made for the pCO2 difference between surface water and the marine atm

245 mpared to low shore levels regardless of the pCO2 level that oysters experienced as larvae.

246 vation is consistent with the effects of the pCO2 on stomatal development and suggests that the evolu

247 rols that had been previously exposed to the pCO2 treatments.

248 ught to have played a dominant role in these pCO2 fluctuations, but it remains unclear how and where

249 ased survival of early stage progeny at this pCO2 concentration, has clear potential to damage popula

250 (collectively CCRA) from California to three pCO2 levels ranging from 419-2,013 microatm for four mon

251 nsidered the potential impacts of changes to pCO2 levels on freshwater biota.

252 were differentially expressed in response to pCO2 environment, but the pattern of change was highly c

253 Stage-specific responses to pCO2 (385-6000 muatm) were studied across different life

254 with low CAi activity was less responsive to pCO2 fluctuations.

255 d are thought to contribute significantly to pCO2 drawdown in the Southern Ocean.

256 al patterns of leaf photosynthesis (A) under pCO2 enrichment in the same trees.

257 osm facility, and in coastal mesocosms under pCO2 levels ranging from 400 to 2,000 muatm.

258 and females were not affected lethally until pCO2 concentrations >/=3000 muatm.

259 t experiments along a shallow water volcanic pCO2 gradient to assess the importance of the timing and

260 we estimate an average, lake area weighted, pCO2 of 966 (678-1,325) muatm and a total FCO2 of 189 (7

261 lii mortality rates increased threefold when pCO2 concentrations reached 1000 muatm (year 2100 scenar

262 by the rate, rather than magnitude, at which pCO2 enrichment occurs.

263 ng the reef varied by ca. 0.1 pH unit, while pCO2 shifted by >60 muatm, a shift equivalent to a ca. 2

264 sis (PG ) and respiration (R) increased with pCO2 indicating that the increased growth was, at least

265 r observations of enhanced productivity with pCO2 , which are consistent with previous reports for so