Questions related to Oxygen Isotopes
Like carbon isotope from fossil tooth enamel, is oxygen isotope also have some specific values to define humid or arid areas?
I'm looking for a laboratory that measures clumped isotopes - Δ47. My research interests are carbonate minerals occurring in ultramafic rocks. I plan to reconstruct the formation conditions of various carbonates from ultramafic massifs from the north-east part of the Bohemian Massif. The carbonates were probably formed in both supergene and hydrothermal conditions and I aim to distinguish how these conditions had changed in terms of time and space. I would like to reconstruct magnesite precipitation conditions using clumped Isotope palaeothermometry.
Please let me know if you are open to collaboration and what are possible costs involved. Long-time scientific cooperation is possible :)
Contact me on Researchgate or firstname.lastname@example.org
I am doing a research on mass extinction on the Permian-Triassic boundary about 250Ma in Botswana Kalahari Karoo Basin to determine
Causes of extinction
paleo-climate and paleo-environment across the P-T boundary
I am planning on using stable carbon ẟ¹³C and ẟ¹⁸O compositions using ICP-MS method. How does the data obtained from ICP-MS look like?
How do you interpret the data?
I’m working on the use of stable isotope ratios in traceability studies of horticultural products. Based on literature and previous studies, I can use any tree part for the analysis when it comes to Sr isotope ratios. However, things change considering H and O, as their isotope ratio may vary considering different classes of organic compounds in plant materials, due to differences in the metabolic pathways of each class (to simplify, let’s consider that all the material was synthetized during the same time frame, e.g. same growing season).
So, I would like to know your opinions about the following points:
1. If I analyze δ2H and δ18O in different tree parts grown in the same period (e.g. shoots, leaves, fruits analyzed as bulk sample), should I expect that the different proportion among classes of organic compounds in each part can lead to a significant difference in their δ2H and δ18O?
2. Analyzing a specific class of organic compounds (after extraction) instead of the bulk sample, should I get the same value in all the different tree parts?
I found several papers discussing this specific topic but related to C and N isotope ratios, can you suggest me any papers related to H and O? Many thanks.
I hope you are doing well.
Could you please help me calculate the fluid oxygen isotope range also source temperature based on the analyzed magnetite's oxygen isotopic data?
Is there any excel file for automatic calculation?
Strong evaporation of soil water in arid areas, so how to compute the evaporation of soil water according to the hydrogen and oxygen isotopes?
Hi to all, I did an experiment with drinkable water of a spring (I bought the bottle). I put a part of this water in a fridge (water with natural CO2) in a large plate and I left in the fridge for 3 days (without any cover). My aim was to enrich water with heavy isotopes and to model the change of δ18O and δ2H during the fractionating.
The temperature in the fridge was around 0 and 1 °C. In the end of the experiment 16% of water was lost.
I measured in the laboratory (by IRMS spectrometry) the isotopes and these are the results:
· δ18O before the treatment: -8.7 and after the treatment in the fridge -6
· δ2H before the treatment: -58.5 and after the treatment in the fridge --46.3
I tried to model the changes of δ18O and δ2H during the fractionating and I used these formulas (regarding the transition ICE-VAPOUR):
For δ18O Majzoub (1971) plus O'Neil (1968)
For δ2H Majzoub (1971) plus Arnason (1969)
Using these formula I have a good result for the δ18O because at f=0.84 (that means 100-16% of water lost) I have more or less -6, but for the deuterium normally I must have -36 instead of -46.3.
How can I explain these results? Do you have some ideas?
It can be that the humidity affected the deuterium? and if yes, how the humidity affects the deuterium and which could be the formula?
I am only in the beginning phases of this research and could use all the help you are willing to give! If anyone has anything that may be of use to me, be it the oxygen isotope concentrations or articles about Neanderthal breathing habits please send it this way! Thank you!
I am trying to analyze some seawater and sea ice core samples for hydrogen and oxygen isotopic composition using a high temperature conversion — isotope ratio mass spectrometry method. I've seen groups mention that the salt in those samples can make analysis challenging, but I can't find specifics. What should I expect and what extra steps should I take for samples like these?
Any suggestions or methods/papers would be appreciated.
how can I know whether or not my result is influenced by the bacteria
when I culture the diatom and harvest the culture solution before my detecting of the figure about the phosphate oxygen isotope?
Solubility of apatite is highly addressed in mineralogical and material studies.
Heating is one of the major processes in apatite industry. In this study, synthesized
hydroxylapatite (HAp), geological fluorapatite (FAp), and bone bioapatite (BAp) were heated
at various temperature (100-900 oC) for analyses. The mineralogy and solubility of the three
apatites were analyzed by XRD, ATR-IR, and ICP. Release of Ca and P in water for BAp
reach the maximum when heated at 200 oC, i.e., 0.215 mmol/L for Ca and 0.106 mmol/L for
P. The value is higher than the maximum values (heated at 900 oC) of solubility for HAp and
FAp. The heating temperature at 600 oC is a re-crystallization point for all the three types of
apatites. Especially, the crystallinity of BAp is significantly elevated at >600 oC. Phase of
geological FAp is relatively stable during heating up to 900 oC. Phase of =-TCP is present
when heating HAp at 800 to 900 oC. In addition, BAp is transformed to the resemblance of
HAp. However, no =-TCP was detected for BAp during heating between 800 to 900 oC,
which is probably due to its Ca-deficiency.
materials and fertilizer.
One of my students got extremely negative values in oxygen isotopes for diagenetic carbonate structures << -20 per mil V-PDB. The issue is I have never seen any paper with values that negative before. I'd like to understand the implications for such odd values. I'd appreciate if anyone can point me toward relevant papers.
I need to measure the energy content of different types of periphyton and I can't find out how to do it. What is the critic mass needed? Is there any manual or protocol that I could use? Thanks!
To obtain the isotope composition of carbon and oxygen of an solution of CaCO3 in water the carbonate is precipitated as SrCO3.Then SrCO3 is analyzed by mass spectoscopy. Can this material be handled routinely in the same way as CaCO3 or does it need an extra protocol. In other words, can SrCO3 be analyzed in an array together with CaCO3 samples?
We are looking for a partner or a provider for stable isotopic analysis (S, C and O or any of these) on pore water and water column.
I'm interested to understand about the effects of isotopes on properties of a molecule. For example in hydrogen, helium or oxygen (which have isotopes) what is the general expectation on some properties like critical temperature, critical pressure, critical volume and normal boiling point and ideal liquid density of isotopes?
I mean as an example is it true to say that we should expect higher value in volume and density in heavier isotopes? or higher normal boiling point in heavier isotopes like D2 rather than H2?
As an example the normal boiling point of 16O16O is -182.95 C, is it true to consider the normal boiling point of 16O18O (which is heavier) a value like -182.5 C?
So if I conclude my question, what is the value of heavier isotopes against lighter isotopes in following properties: (answer by bigger or lower):
Normal boiling point?
Ideal liquid density?
and Acentric factor?
Thanks in advance.
In addition, does anybody has vapor pressures and other properties of oxygen isotopes like 16O18O?
I really need some experimental data or references which I could be able to have these properties.
Thanks in advance.
i want to know about the formation of NH4(gas or aq) from the combination N2 gas with H2gas; below the conditions.
just i think that N2 gas derived from magma reservoir,
but the production mechanism of H2 gas maybe CH4 and H2S gas from magma gas ? or by Desulfovibrio ? or abnormal meteoric water? or fracture of silicate minerals by earthquake (because very active volcano be located around)
in calc-alkalic andesitic and rhyolitic magma system, volcanic and organic rich sediments covered submarne vent system in garben caldera like crater. under the 20bar, 473K. seawater pH about 7~8, hydrothermal fluids near the vent system showed pH 5~6 (from diffusing hydrothermal fluid).
from the chemistry of pore water fluid in sediment core showed high concentration of ammonia.
from the oxygen isotope data that it is possible to mix among seawater, meteoric water and magma water.
The emphasis is on triple oxygen isotope system where mass-dependent fractionation is operating. A mass loss due to evaporation of water may cause an enrichment of heavier isotope (d18O compared to d17O). To model this scenario, I may need a reference to start with. I would apprecaite receiving suggestions regarding dehydration of phyllosilicates (having -OH group) during thermal metamorphism at ~850C. Assuming it is an open system allowing loss of part of evaporated water (enriched in d17O compared to d18O) while the rest of it is being recondensed. This scenario represents thermal metamorphism occurred on a H or L ordinary chondrite (types 5 or 6) parent body/ies (stony asteriods) assuming type 3 OC as a precusrsor having phyllosilicates formed after aqueous alteration.
Generally, there are three partial reactions during gibbsite dehydroxylation. Gibbsite will transform into boehmite at about 200℃. If I know the H/O isotope value of gibbsite, how can I get the value of boehmite. Alternatively, anyone knows the fractionation faactors between them.
I have a Speleothem isotope record of Indian summer monsoon(NW Himalan region) in which oxygen isotope shows wetter phase (16O enriched values). At the same time for the same speleothem (same depth and time as for oxygen) carbon isotope record shows C4 vegetation(13C enriched values).
How can it be possible? In which condition would it happened?
Because in tropical region the vegetation is governed by rainfall. If more rainfall then It should be C3 type vegetation(12C enriched) vegetation.
I am critical about a porphyry Cu-S ore occurrence while working on a porphyry granitoid in a cratonic shield of NE India . As my study shows positive indications in many parameters I studied like Sr and S isotopes, hypogene alteration pattern, detail geochemical signature etc. I need to investigate oxygen isotope and fluid inclusion to enhance my claim for drilling as geophysical works seems to be difficult in view of inaccessibility.
I asked a previous question as to whether dense ash aggregates (or "acc-laps") have ever been made in any wind tunnel lab thus far in their fully formed sub-spherical or ellipsoïdal shape ?
The answer has been: "not yet", even though this would allow to more closely simulate mixed phase aggregation under more realistic in situ ashcloud conditions.
I am wondering if any accretionary lapilli greater than about 10mm across or so have ever been collected immediately upon reaching the ground and studied immediately, or preserved in a cold box (to prevent them from any melting) and studied in the lab (eg. on a cryogenic SEM stage, or to measure their in situ temperature, and recover inner fluids from the intergranular space....) ?
The reason is that there is the hypothesis that they form like hailstones by riming, once they grow above a size characteristic of the drop break-up limit (5-6mm across). If this "volcanogenic hailstone" hypothesis is correct, then my expectation is that a proportion of accretionary lapilli larger than about 6mm diameter should still be frozen upon reaching the ground (especially if above-ground températures are close to 0°C; if not partial melting takes place), so that somewhat larger ones (say 10mm diameter ones) may still be frozen (despite partial melting) and still contain inner ice upon landing on the ground.
Has anyone checked for this ?
Assuming for a moment that larger sub-concentric acclaps can be sampled immediately, preserved and analysed for oxygen isotopes of any trapped ice water, then this could provide valuable data as to the temperature environments through which the acc-laps have been recycled again and again in the volcanic cloud before ultimately falling out.
Analogous oxygen isotope ratio studies of the subconcentric layers of hailstones from severe thunderstorms have provided such information in that case.
I am looking forward to hearing back.
Best wishes and kind regards,
It is well known that stable oxygen isotopic composition (δ18O) has been widely used to trace natural hydrological processes. In modern ocean research, δ18O has been used to obtain information on the origin and mixing of water masses, such as freshwater mixing, evaporation, precipitation and sea-ice formation. The δ18O of seawater is influenced by these foregoing factors. However, will δ18O of seawater be influenced by biochemical processes? Such as Photosynthesis and respiration? whether δ18O of seawater can be influenced by biological fractionation of δ18O (Dissolved Oxygen) in seawater? Can anyone provide me some references about this? Thanks!
What does the carbon and oxygen isotopic compositions of pedogenic carbonates tell us about the climate during which they formed, when they show positive, negative relationship, or even noncorrelation?
Ferromanganese crust is authigenic precipitation on surface of rocks in the deep ocean. As it is formed very slowly, its oxygen isotope should be equilibrium with that of the ambient sea water. However, different proportions of precipitated minerals, such as δMnO2, FeO(OH), among different layers make it complicated to identify the fractionation factors. If resolved, the oxygen isotope profile would be useful neither in establishing the age model of ferromanganese crust or in the past changes in the ocean envioronment. So, so anyone provide me any clues to resolve this problem, for example, the oxygen isotope fractionation factors between sea water and the oxides?
I am analyzing the relationship between stable isotope (d13C & d18O) from tree-rings and climate variables. And I want to interpret the response of d13C and d18O with monthly precipitation, humidity, temperature, etc. I found significant differences between tree species and sites (Humid and Dry forest) which I can only attribute as a noise related to specific-species and unknown factors. And inside of these unknown factors I was thinking if the lenticels could have a significant influence in the isotope fixation process, mainly the d13C. Two of my tree species have lenticels in the trunk (Maclura tinctoria) and in the young branches (Cedrela montana), and both are defoliated of 4 to 6 months in the year.
Since the lenticels are pathways for gas exchange similar to stomata, would it be possible that lenticels can play an important role in the carbon and oxygen fixation on the wood, and if so, how?
I will appreciate very much your comments.
My carbonate carbon isotope vaues from a Cenomanian-Turonian section (deposited during OAE 2) are depleted by more than 1.5–3‰ relative to contemporaneous marine calcite. Likewise, the δ18Ocarb values are also low compared to those found in Cretaceous pelagic sediments (Clarke and Jenkyns, 1999). ¿Could a demise of carbonate production explain carbonate carbon and oxygen isotope values depleted relative to contemporaneous marine calcite?
I'm not a scientist in this field, but I was just wondering whether these two datasets could help each other for the benefit of a better understanding of human mobility in the past.
As we know, both cellulose oxygen isotope and leaf wax hydrogen isotope could record the isotope information of precipitation. However, for cellulose, most case studies focus on peat study. For lake sediment, there seldom papers concerned. Could you share your ideas about this? Thanks.
i have Oxygen and deutrium concentrations for about 35 springs. i wonder if i can find any method to estimate the reservoir's temperature by using these concentrations
Does anyone have any information on the presence of 16O/18O oxygen isotope ratio in exhaled breath and the presence or stage of cancer?
I am analyzing triple oxygen isotopes of carbonates. While scanning on Mass Spectrophotometer (magnetic Field vs Intensity), the Nitrogen peak (mass 28, Cup 3) is very high. I didn't find any leak, is it user error or any suggestions to improve?
silt size samples gotten from drilled holes is to be analysed for carbon and oxygen isotopes. which analytical technique would give the best result? and what is the procedure for preparation of the samples for such analysis?
I am currently studying dolomitic limestones from the Upper Triassic and my samples of dolomite and calcite, after being measured for C and O isotopes, it came with the note that dolomite was corrected as being calcite effect at -0.8‰.
I know that one of the problems is related with the measurement procedure, once it it used phosphoric acid, but it may be also related with the dolomite problem, what kind of reaction formed the dolomite....
Thank you in advance.
I would like to get carbon and oxygen isotope composition of carbonate from organic-rich calcareous tufa (bulk). What is a suitable way to remove organic matter from the sediment? Is roasting of the sample at 380°C a reasonable way?
Large-scale low-δ18O magmas have been interpreted to have formed by remelting or assimilation of high-temperature hydrothermally altered rocks, such as those found in Iceland basalts and Yellowstone rhyolites. Formation of low-δ18O magma, in most cases, seems to related to rift or extensional tectonic environment. I just wonder whether low-δ18O may be formed at subduction zone and how it happens. Discussion or any relevant reference is appreciated.
I want to use Cramer et al. (2009) raw data of oxygen and carbon isotopes for a very specific time period (around 2 Ma long) to compare it to my oxygen and carbon isotopes from terrestrial record. My aim is to show that my site is affectd by global factors by comparing Cramer's data with mine. I don't have the same sample resolution as Cramer's: he has about 1000 data points while I have about 300. How can I solve the problem of difference in data resolution? Which methods would you suggest to address this issue?
I also would like to statistically compare my data with Cramer's, but my data is terrestrial so the oxygen isotope values are much lower (around -7 per mil). I would like to be able to compare the trends, not the actual values. Would anyone know which test(s) I could use?
I am undertaking some chemostratigraphic work with carbon and oxygen isotopes in carbonates. I have used basic petrographic techniques and (cold) cathodoluminescence to gauge diagenesis and alteration in my samples, though I am interested to hear about experiences other researchers may have had and what techniques they have used. Cheers!
I assume that apatite mineral in the lunar material is reacting with HCl at 75 degrees when I leach samples to remove any terrestrial contamination. The reason for this assumption is that the oxygen isotope compositions of unleached and leached bulk materials are different, i.e., leached are heavier than the unleached and it could happen if apatite reacts with HCl during leaching process causing -PO4 to go out into the water and ultimately out of the material to be analyzed for oxygen isotopes. Yet another assumption that it could happen only if apatite has heavy oxygen isotopes than the bulk material. I'd appreciate your feedback and suggestion if I could use any other chemical to remove terrestrial contamination (mostly carbonates and oxides) without disturbing the apatite in lunar samples. Thanks!
As I know, palaeoclimatologists use benthic foraminifera oxygen isotope to reconstruct the ice volume. However, this contains both Arctic and Antarctica information. Shall we separate the signal? Thanks.
In this paper, Lonnie mentioned the precipitation regime of Guliya is monsoonal, however, the oxygen isotope of Guliya is obviously different from classic monsoon-dominated areas in East Asian? Could you share your idea,thanks.
It is apparently better to use a ceramic or porcelain drill instead of a metal drill bit to sample bone and teeth for oxygen stable isotope analysis because the metal could alter the d18O signal. Could someone explain why this is?
I would like to analyze volcanic glass samples on the TC/EA for their oxygen isotopic ratio, but am not sure of a good standard to use. Does anyone know of articles that delve into this, or standards that have been used in the past?