ライフサイエンスコーパス: carbon isotope

1 vidual and their diet) total carbon (TC) and carbon isotope (13)C (delta(13)C) and (14)C (F(m)) were

2 The stable carbon isotope (13)C is used as a universal tracer in pl

3 cellent agreement has been found between the carbon isotope amount ratio value measured by MC-ICPMS a

4 (R = 0.9997) was obtained between corrected carbon isotope amount ratios and expected carbon isotope

5 ratio mass spectrometry measurements is that carbon isotope amount ratios are measured as C(+) instea

6 new avenues for the measurement of absolute carbon isotope amount ratios in a wide range of samples.

7 ed carbon isotope amount ratios and expected carbon isotope amount ratios of the four chosen NIST RMs

8 n measured for four reference materials with carbon isotope amount ratios ranging from 0.010659 (delt

9 Absolute values for carbon isotope amount ratios traceable to the SI are giv

10 w method for the measurement of SI traceable carbon isotope amount ratios using a multicollector indu

11 efore, it is suitable for the measurement of carbon isotope amount ratios within the natural range of

12 Compound-specific carbon isotope analyses also have been used here to char

13 Geochemical biomarkers and stable carbon isotope analyses fingerprint the presence of oils

14 and delta(15)N values) and compound-specific carbon isotope analyses of individual fatty acids (delta

15 We combine both organic and calcite carbon isotope analyses of individual specimens of these

16 ly recorded in carbonate rocks, thousands of carbon isotope analyses of late Precambrian examples hav

17 ed the use of compound-specific chlorine and carbon isotope analysis (Cl- and C-CSIA) to assess CP bi

18 to continuous flow compound-specific stable carbon isotope analysis mass spectrometry for concentrat

19 On the basis of the carbon isotope analysis of 42 natural caffeine samples i

20 tio mass spectrometer (LC-IRMS) in 2004, yet carbon isotope analysis of unpolar and moderately polar

21 by aerobic acetic acid bacteria and, lacking carbon isotope analysis, are more generally used as indi

22 ethane seep communities, in conjunction with carbon isotope analysis, has led to their use as biomark

23 in GC x GC is compatible with high-precision carbon isotope analysis.

24 add support to the deductions made from the carbon isotope analysis.

25 iew outlines for the first time the expected carbon isotope and noble gas compositions of captured CO

26 Here we present high-resolution carbon isotope and sulphur isotope records from the Huqf

27 sely dated high-resolution speleothem oxygen-carbon isotope and trace element records of Central Asia

28 ariability at both cave sites, inferred from carbon isotope and trace element records, shows climate

29 combine measurements of radiocarbon, stable carbon isotopes and element ratios to correct for rock-d

30 y) climatic fluctuations reflected in stable carbon isotopes and sedimentary facies in lacustrine str

31 New palynological, wildfire, organic carbon isotope, and atmospheric pCO2 data from early din

32 e large-amplitude (over 10 per mil) negative carbon isotope anomalies, and use these data in a new qu

33 ynodont therapsids, coinciding with negative carbon-isotope anomalies.

34 Here we present the first dual-carbon isotope-based (Delta(14)C and delta(13)C) source

35 cretion-differentiation history but also for carbon isotope biosignatures for early life on the Earth

36 n temperature and degree of fractionation of carbon isotopes by phytoplankton at temperatures below a

37 Fractionation of carbon isotopes by plants during CO(2) uptake and fixati

38 The analysis of tree-ring carbon isotope composition (delta(13)C) has been widely

39 e of explaining the observed changes in both carbon isotope composition and calcium carbonate accumul

40 rs, and the positive correlation between the carbon isotope composition and oxygen content of modern

41 Moreover, stable carbon isotope composition indicated that crystals are o

42 The carbon isotope composition of calcite formed during this

43 eenhouse climates are based primarily on the carbon isotope composition of calcium carbonate in fossi

44 re three profound negative delta(13)C(carb) (carbon isotope composition of carbonate) excursions in t

45 ntiomeric fractions (EFs), compound-specific carbon isotope composition of DDT and its metabolites, a

46 We measured the carbon isotope composition of fry oil in French fries pu

47 d by calculating the stand-level increase in carbon isotope composition of late wood from a wet to a

48 from volcanic arcs and demonstrated that the carbon isotope composition of mean global volcanic gas i

49 etermine peat accumulation rates) and stable carbon isotope composition of moss cellulose (to estimat

50 erized by remarkably stable delta(13)C(org) (carbon isotope composition of organic carbon) values but

51 on when analysing large-scale changes in the carbon isotope composition of terrestrial substrates.

52 Examining stable carbon isotope composition of tree rings in addition to

53 uating the phylogenetic distribution of CAM, carbon isotope composition will reflect these diffusive

54 These morphospecies-correlated carbon isotope compositions confirm the biogenicity of t

55 A broad compilation of modern carbon isotope compositions in all C3 plant types shows

56 rom the observed spread toward more negative carbon isotope compositions in Neoproterozoic (1.0-0.542

57 Here we apply hydrogen and carbon isotope compositions of plant wax lipids in two l

58 The carbon isotope compositions were compared to the source

59 ork for ecological interpretations of stable carbon-isotope compositions (expressed as delta(13)C val

60 Here, we present dual carbon isotope constrained (Delta(14)C and delta(13)C) s

61 These genes are highly expressed and methane carbon isotope data are consistent with hydrogenotrophic

62 The organic carbon isotope data combined with measurements of oxygen

63 Here we compile all published oxygen and carbon isotope data for Neoproterozoic marine carbonates

64 orthern boreal forest, we compiled published carbon isotope data from 14 high-latitude sites within E

65 We present carbon isotope data from 452 fossil teeth that record di

66 In contrast, carbon isotope data from cercopithecids indicate that C4

67 Here we use carbon isotope data from early to mid Pliocene hominin a

68 We find that carbonate and organic carbon isotope data from Mongolia and Canada are tightly

69 carbon storage using radiocarbon and stable carbon isotope data from the Brazil and Iberian Margins.

70 Carbon isotope data show that Australopithecus bahrelgha

71 e data in the context of iron speciation and carbon isotope data suggests biogeochemical cycling acro

72 Paleomagnetic/magnetostratigraphic and carbon-isotope data allow sections to be correlated acro

73 We present carbonate and organic matter carbon-isotope data that demonstrate no decoupling from

74 Precursor and product carbon isotope delta values consistently fit a linear re

75 nt a new, annually resolved record of stable carbon isotope (delta(13) C) data determined from Larix

76 edimentation and a negative excursion in the carbon isotope (delta(13)C) composition of carbonate min

77 Within these limits, the carbonate carbon isotope (delta(13)C) record becomes insensitive t

78 ed +2 per thousand increase in the carbonate carbon isotope (delta(13)C) record by approximately 445

79 ion with a recently published benthic stable carbon isotope (delta(13)C) record from the southernmost

80 s study analyzed the potential of the stable carbon isotope (delta(13)C) value as a structural microc

81 This study used carbon isotope (delta(13)C)-based calculations to quanti

82 Here we develop a high-resolution carbonate carbon isotope (delta(13)Ccarb) record for 3.20 million

83 Barium-to-calcium ratios (Ba/Ca) and carbon isotopes (delta(13)C) measured in long-lived cora

84 A pronounced negative carbon-isotope (delta13C) excursion of approximately 5-7

85 ,000 to 55,000 years ago based on oxygen and carbon isotopes determined by ion microprobe and uranium

86 quid chromatography (LC) based on postcolumn carbon isotope dilution mass spectrometry (IDMS) was dev

87 re tested for their genetic association with carbon isotope discrimination (CID), a time-integrated t

88 al mechanisms underlying variation in stable carbon isotope discrimination (Delta(13)C) are largely u

89 Carbon isotope discrimination (Delta(13)C) in cellulose

90 Leaf hydraulic conductance (K(Leaf)), carbon isotope discrimination (Delta(13)C), leaf mass pe

91 Carbon isotope discrimination (Delta) for untreated poll

92 enzyme activity, gas exchange, and real-time carbon isotope discrimination (Delta).

93 A model defining carbon isotope discrimination (delta13C) for crassulacea

94 f 14 SNPs were associated with the traits of carbon isotope discrimination (n = 7), height (n = 1) an

95 x = 8.3) show a progressive increase in both carbon isotope discrimination and as light decreases.

96 ch as an AP2 transcription factor related to carbon isotope discrimination and glutamate decarboxylas

97 terior Alaska to examine long-term trends in carbon isotope discrimination and growth of black and wh

98 af water-use efficiency (WUE) as measured by carbon isotope discrimination and increased plot-level L

99 flux densities (isofluxes) and derive canopy carbon isotope discrimination as an integrated proxy for

100 Wi was estimated from carbon isotope discrimination in archived herbage sample

101 ferences were found in cuticle thickness and carbon isotope discrimination in near-isogenic lines dif

102 Carbon isotope discrimination in plant leaves (Deltaleaf

103 urements of photosynthesis coupled to online carbon isotope discrimination showed that leaves within

104 We used carbon isotope discrimination to show that TE is increas

105 ritical determinant of growth rate, and high carbon isotope discrimination values reflecting optimal

106 oxygen/chlorophyll fluorescence method), and carbon isotope discrimination were measured on plants un

107 nductance as well as with a long-term proxy (carbon isotope discrimination) for gas exchange, suggest

108 for association with phenotypic variation in carbon isotope discrimination, foliar nitrogen concentra

109 levels were associated with changes in leaf carbon isotope discrimination, indicating altered water

110 nd improved water use efficiency measured as carbon isotope discrimination.

111 The carbon isotope distribution within sugars has been shown

112 Here, we present a model for understanding carbon isotope distributions within the deep Earth, invo

113 st hydroclimate because the fractionation of carbon isotopes during photosynthesis is strongly influe

114 igh frequency, large amplitude variations in carbon isotopes during the 8.2 ka event, coupled with pu

115 For methane formation, a carbon isotope effect ((12)CH3-S-CoM/(13)CH3-S-CoM) of 1

116 n up to +5.1 per thousand) along with normal carbon isotope effect (epsilonreactive position of -12.6

117 r carbon (AKIE) in order to characterize the carbon isotope effect at the reactive positions for the

118 lefinic (13)C isotope effect and small alpha carbon isotope effect is indicative of an asynchronous t

119 The carbon isotope effect on the alpha-pyrrole carbon and th

120 sotope fractionation, without any detectable carbon isotope effect, that was observed for 3-bromophen

121 wise, degradation consistently showed normal carbon isotope effects (epsiloncarbon=-5.0 per thousand+

122 The observed carbonyl carbon isotope effects [(13)(V/K)] were 1.0135 +/- 0.000

123 The similarity of the magnitude of the carbon isotope effects argues for formation of a common

124 Experimental evidence, including carbon isotope effects measured by (13)C NMR, were indic

125 In contrast to the expected larger primary carbon isotope effects relative to chlorine for C-Cl bon

126 r, biotic transformations resulted in weaker carbon isotope effects than respective abiotic transform

127 Significant carbon isotope effects were observed for nucleophilic su

128 The carbon isotope enrichment factor (epsilon) measured duri

129 Carbon isotope enrichment factors (epsilon(c)) for gamma

130 Carbon isotope enrichment factors for SMX (epsilon(C)) w

131 Carbon isotope enrichment factors obtained from an optim

132 on at microbial membranes was observed, with carbon isotope enrichment factors of -2.2 per thousand,

133 15 (well T1), and was found accompanied by a carbon isotope enrichment of 5 per thousand and 2.9 per

134 the mechanisms behind Earth's most dramatic carbon isotope event, we obtained coupled stable isotope

135 This finding not only negates carbon isotope evidence for methane release during Marin

136 The terrestrial-plant carbon isotope excursion (about -4.5 to -6 per mil) is s

137 Eocene thermal maximum (PETM) and associated carbon isotope excursion (CIE) are often touted as the b

138 This carbon isotope excursion (CIE) is consistent with the re

139 n years ago) is marked by an abrupt negative carbon isotope excursion (CIE) that coincides with an ox

140 cted in sedimentary components as a negative carbon isotope excursion (CIE).

141 e rise contemporaneous with a large negative carbon isotope excursion (CIE).

142 g the globally recognized Steptoean Positive Carbon Isotope Excursion (SPICE) that indicates a major

143 cursion in phase with the Steptoean Positive Carbon Isotope Excursion (SPICE), a large and rapid excu

144 ,384-3,342 p.p.m.v. during the height of the carbon isotope excursion across all sources postulated f

145 extraterrestrial impact occurred during the carbon isotope excursion at the P-E boundary.

146 When applied to the carbon isotope excursion at the Palaeocene-Eocene bounda

147 and continued until the end of the Lomagundi carbon isotope excursion ca. 2,060 Ma.

148 -foraminifera measurements of the associated carbon isotope excursion from Maud Rise (South Atlantic

149 Single-foraminifera measurements of the PETM carbon isotope excursion from Maud Rise have been interp

150 rom the Paleocene-Eocene thermal maximum and carbon isotope excursion in cored sections at Ancora and

151 mpensation depth and a >2.5 per mil negative carbon isotope excursion in marine and soil carbonates.

152 Concomitant with the carbon isotope excursion marking the PETM we document a

153 or the greatly enhanced magnetization of the carbon isotope excursion sediment but whose origin is th

154 characteristically record a larger-amplitude carbon isotope excursion than marine substrates for a si

155 risis predates the onset of a major negative carbon isotope excursion that points to subsequent sever

156 Toward the end of the carbon isotope excursion there is an increase in the del

157 Intermediate waters warmed before the carbon isotope excursion, in association with downwellin

158 extinctions and is tied to a large negative carbon isotope excursion, reflecting perturbations of th

159 n by the comings and goings of the Lomagundi carbon isotope excursion, the longest-lived positive del

160 kground and maximum pCO(2) levels across the carbon isotope excursion.

161 enation in the waning stages of the positive carbon isotope excursion.

162 We find that coincident with the negative carbon-isotope excursion carbon dioxide is first drawn d

163 A pronounced carbonate carbon-isotope excursion during the Ediacaran Period (63

164 Negative carbon isotope excursions measured in marine and terrest

165 Exceptional patterns for carbon isotope excursions resulted from massive carbon b

166 Conspicuous global stable carbon isotope excursions that are recorded in marine se

167 The many carbon isotope excursions that parallel those for oxygen

168 They are characterized by carbon-isotope excursions in marine and terrestrial rese

169 read marine organic-carbon burial and coeval carbon-isotope excursions.

170 Our data show that net carbon isotope fractionation (Delta(13) C), decreased by

171 sm by strain NaphS6 was linked to negligible carbon isotope fractionation (epsilonC = -0.2 +/- 0.2 pe

172 ne dioxygenases was associated with moderate carbon isotope fractionation (epsilonC = -0.8 +/- 0.1 pe

173 chlorination was associated with significant carbon isotope fractionation (epsilonC = -2.0 per thousa

174 Here, carbon isotope fractionation by Dehalococcoides mccartyi

175 y accounting for the fundamental increase in carbon isotope fractionation by land plants in response

176 This absence of measurable carbon isotope fractionation considerably facilitates th

177 ve of this study is to quantify chlorine and carbon isotope fractionation during NAPL-vapor equilibra

178 Our data indicate constant carbon isotope fractionation for acetate formation at di

179 This study demonstrates that carbon isotope fractionation is a valuable approach for

180 aporization in a sand column, no significant carbon isotope fractionation is observed (epsilon(C) = +

181 extent and range of isomer and enantiomeric carbon isotope fractionation of HCHs with Sphingobium sp

182 bacteria we measured (a) enantiomer-specific carbon isotope fractionation of MCPP ((R,S)-2-(4-chloro-

183 Carbon isotope fractionation of sulfamethoxazole (SMX) d

184 llular microscale mass transfer on microbial carbon isotope fractionation of tetrachloroethene (PCE)

185 In this work, carbon isotope fractionation of the three dichlorobenzen

186 ctively; Fenton-like degradation resulted in carbon isotope fractionation only, leading to LambdaC/Br

187 ms through a combination of enantiomeric and carbon isotope fractionation to characterize the degrada

188 While carbon isotope fractionation was generally small, observ

189 Carbon isotope fractionation was investigated for the bi

190 on = -1.3 per thousand to -2.0 per thousand) carbon isotope fractionation was observed.

191 seems, therefore, a stronger indicator than carbon isotope fractionation.

192 The surprisingly large difference in the carbon-isotope fractionation factor between the CO(2)(m)

193 the structure, vibrational frequencies, and carbon-isotope fractionation factors of the carbon dioxi

194 nt, and cofactor-limiting conditions, stable carbon isotope fractionations remain consistent for give

195 d the global history of [CH4] and its stable carbon isotopes from ice cores, archived air, and a glob

196 The collapse of sea surface to sea floor carbon isotope gradients has been interpreted as reflect

197 sulfur isotopes in sulfate (delta(34)SSO4), carbon isotopes in dissolved inorganic carbon (delta(13)

198 Stable carbon isotopes in fossil tooth enamel are used to estim

199 We added measurements of carbon isotopes in respired CO(2) to constrain the age o

200 al ecosystems can be quantified using stable carbon isotopes in soils.

201 water-use efficiency (W i ), estimated using carbon isotopes in tree rings, suggesting trees are gain

202 Carbon isotopes indicate multiple carbon sources in the

203 in the results of lipid biomarker and stable carbon isotope investigations of tissues, bandaging, and

204 s especially useful in rapid carboxylic acid carbon isotope labeling, however development toward its

205 Here, we used stable carbon isotopes, leaf nitrogen content and stomatal meas

206 than traditionally determined from a global carbon isotope mass balance and may have varied over geo

207 Here we show that the carbon isotope mass balance is also significantly affect

208 is sink constitutes a minor component of the carbon isotope mass balance under the modern, high level

209 and gross carbon fluxes affect the long-term carbon isotope mass balance, and may lead to reassessmen

210 a shallow aquifer was monitored using stable carbon isotope measurements at a field site near the tow

211 tal development, we present 1.037 new stable carbon isotope measurements from 33 archaeological sites

212 000-year Antarctic ice-core record of stable carbon isotope measurements in atmospheric methane (delt

213 Here we present stable hydrogen and carbon isotope measurements of terrestrial-plant- and aq

214 om a worldwide dataset of >3,500 leaf stable carbon isotope measurements.

215 The carbon isotope method (AOAC 998.12) compares the bulk ho

216 The technique is compared to an established carbon isotope method in three C3 species.

217 Stable carbon isotopes of CH4 and CO2 further indicated the pos

218 Here, we show that carbon isotopes of leaf wax derived lipids (n-alkanes),

219 m the present study reveal 14 instances (C12 carbon isotope) of multiple m/z ions having the same nom

220 s, significant advances have been made using carbon isotopes, 'omics' analyses and surveys of respira

221 usly published field data showing a negative carbon isotope pattern (-2 per thousand) at the fringes

222 however, the interval of peak magnitude for carbon isotopes precedes that of sulfur isotopes with an

223 The carbon isotopes preserved in the Ca-rich carbonate phase

224 ns by measuring the natural abundance stable-carbon-isotope profile of corn- and sugar cane-sweetened

225 Carbon isotope ratio ((13)C/(12)C=delta(13)C) of 100 pin

226 d substrates or products is reflected in the carbon isotope ratio (13C/12C) in GTP or GDP, which is d

227 To identify these adulterations, stable carbon isotope ratio analysis (SCIRA) was performed on t

228 95; AOAC 998.12, 2005) and Internal Standard Carbon Isotope Ratio Analysis could not efficiently dete

229 o mass spectrometry (HT-LC/PDA/IRMS) for the carbon isotope ratio analysis of unconjugated steroids.

230 mal dependence (<1 per thousand) of measured carbon isotope ratio on methane concentration.

231 methodology for the determination of stable carbon isotope ratio was evaluated in comparison with th

232 ectroscopy to determine the bulk (13)C/(12)C carbon isotope ratio, at natural abundance, in inorganic

233 af as a tracer of past rainfall by analysing carbon isotope ratios (delta(13) C) of modern leaves.

234 using bone and enamel apatite rely mainly on carbon isotope ratios (delta(13)C) and to a lesser exten

235 We also assessed the agreement in carbon isotope ratios (delta(13)C) between hair and RBCs

236 Serial carbon isotope ratios (delta(13)C) in canine enamel from

237 Ma), extended intervals of anomalously high carbon isotope ratios (delta(13)C) indicate high rates o

238 Wood warbler carbon isotope ratios are more depleted than typical for

239 Carbon isotope ratios can be determined with accuracy an

240 Carbon isotope ratios from terrestrial plant wax biomark

241 rm pulses coinciding with rapidly decreasing carbon isotope ratios may in part be the result of a rad

242 The carbon isotope ratios of milk protein and milk fat as we

243 ext we present the first method to determine carbon isotope ratios of pharmaceuticals that cannot be

244 Variations in benthic carbon isotope ratios of up to approximately 1.4 per mil

245 rprinting (P-SIF) is a method to measure the carbon isotope ratios of whole proteins separated from c

246 Intramolecular carbon isotope ratios reflect the source of a compound a

247 Carbon isotope ratios were well correlated with satellit

248 The CSIA profiles showed large shifts of carbon isotope ratios with depth (up to 24 per thousand)

249 Carbon isotope ratios, geographical and climate data, fo

250 upled to optical and electron microscopy and carbon isotope ratios, we demonstrate that the Mn is hos

251 unlikely given the enriched nature of their carbon isotope ratios.

252 Carbon-isotope ratios of seed collected from 4-month-old

253 Large-scale surveys of carbon-isotope ratios typically show a strongly bimodal

254 corresponds with the Shuram excursion in the carbon isotope record and seems to have involved the oxi

255 well as a 10 per thousand difference in the carbon isotope record between Yangtze Gorges and basin s

256 e present to our knowledge the first organic carbon isotope record derived from the organic matrix in

257 We combine our pH data with a paired carbon isotope record in an Earth system model in order

258 The long-term, steady-state marine carbon isotope record reflects changes to the proportion

259 ), a large and rapid excursion in the marine carbon isotope record, which is thought to be indicative

260 gical evidence for this pathway based on the carbon isotope record.

261 Stable carbon isotopes record diet changes, principally enablin

262 abrupt shift in deep-ocean circulation using carbon isotope records from fourteen sites.

263 niferal records with benthic and bulk stable carbon isotope records from the Pacific, Southeast Atlan

264 Plant wax carbon isotope records indicate a decline in C4 plants i

265 are, in large part, derived from the stable carbon isotope records of carbonate rocks and sedimentar

266 ased on long-term global methane and methane carbon isotope records.

267 The Mars Phoenix spacecraft measurements of carbon isotopes [referenced to the Vienna Pee Dee belemn

268 We further report on new paired carbon isotope results from carbonate and organic matter

269 combination of several age constraints from carbon isotopes showed that warming had a similar effect

270 wball' state, it would not have left extreme carbon isotope signals in cap dolostones.

271 The intramolecular carbon isotope signature generated by online pyrolysis (

272 Significant variability in the stable carbon isotope signature indicated temporally shifting e

273 echnique which determines the intramolecular carbon isotope signature of AEOs generated by online pyr

274 as to determine the natural abundance stable-carbon-isotope signature of commonly consumed foods of p

275 is the occurrence of exceptionally depleted carbon isotope signatures (delta(13)C(PDB) down to -48 p

276 Carbon isotope signatures (delta(13)C) of SMX were measu

277 m hydrothermal fluids and suggest that their carbon isotope signatures are a consequence of thermogen

278 Because the diamond hosts have carbon isotope signatures consistent with surface-derive

279 he food chains they support also have unique carbon isotope signatures.

280 Correlation based on carbon isotope stratigraphy and sequence stratigraphy in

281 We use dinoflagellate cyst and stable carbon isotope stratigraphy to date the active phase of

282 We show that the combined oxygen and carbon isotope systematics are identical to those of wel

283 Here, a ramped pyrolysis carbon isotope technique is employed to investigate ther

284 nts and, when combined with well-established carbon isotope techniques, may provide additional inform

285 In one approach, based on analysis of carbon isotopes, the persistence of carbon is inferred;

286 erica, China and Europe, using noble gas and carbon isotope tracers.

287 Emissions from trees had an average stable carbon isotope value (delta(13)C) of -66.2 +/- 6.4 per m

288 method (AOAC 998.12) compares the bulk honey carbon isotope value with that of the extracted protein;

289 the polysulfone membrane does not alter the carbon isotope values (+/-0.5 per thousand).

290 using marine sediment records of oxygen and carbon isotope values and of calcium carbonate content f

291 e benzene and monochlorobenzene (MCB) stable carbon isotope values at a fine vertical resolution (3 c

292 tal records show an abrupt negative shift in carbon isotope values at approximately 55.8 Myr ago.

293 th shoaled, ocean temperatures increased and carbon isotope values decreased in the equatorial Atlant

294 Enamel carbon isotope values from teeth of human-hunted gazelle

295 Fatty acid and bulk stable carbon isotope values of cave-adapted shrimp suggest tha

296 We measure a decrease in the carbon isotope values of the hopanoids at the onset of t

297 ccompanied by invariant or decoupled organic carbon-isotope values, has been explained with a model t

298 e numerous reports of natural intramolecular carbon isotope variability, there are no literature repo

299 enic carbonate sink helps to explain extreme carbon isotope variations in the Proterozoic, Paleozoic,

300 * Carbon isotopes were measured on annual rings of glacial