233U/236U signature allows to distinguish environmental emissions of civil nuclear industry from weapons fallout

Isotopic ratios of radioactive releases into the environment are useful signatures for contamination source assessment. Uranium is known to behave conservatively in sea water so that a ratio of uranium trace isotopes may serve as a superior oceanographic tracer. Here we present data on the atomic \documentclass[12pt]{minimal} \usepackage{amsmath} \usepackage{wasysym} \usepackage{amsfonts} \usepackage{amssymb} \usepackage{amsbsy} \usepackage{mathrsfs} \usepackage{upgreek} \setlength{\oddsidemargin}{-69pt} \begin{document}$$^{233}$$\end{document}233U/\documentclass[12pt]{minimal} \usepackage{amsmath} \usepackage{wasysym} \usepackage{amsfonts} \usepackage{amssymb} \usepackage{amsbsy} \usepackage{mathrsfs} \usepackage{upgreek} \setlength{\oddsidemargin}{-69pt} \begin{document}$$^{236}$$\end{document}236U ratio analyzed in representative environmental samples finding ratios of (0.1–3.7)\documentclass[12pt]{minimal} \usepackage{amsmath} \usepackage{wasysym} \usepackage{amsfonts} \usepackage{amssymb} \usepackage{amsbsy} \usepackage{mathrsfs} \usepackage{upgreek} \setlength{\oddsidemargin}{-69pt} \begin{document}$$\cdot$$\end{document}⋅10\documentclass[12pt]{minimal} \usepackage{amsmath} \usepackage{wasysym} \usepackage{amsfonts} \usepackage{amssymb} \usepackage{amsbsy} \usepackage{mathrsfs} \usepackage{upgreek} \setlength{\oddsidemargin}{-69pt} \begin{document}$$^{-2}$$\end{document}−2. The ratios detected in compartments of the environment affected by releases of nuclear power production or by weapons fallout differ by one order of magnitude. Significant amounts of \documentclass[12pt]{minimal} \usepackage{amsmath} \usepackage{wasysym} \usepackage{amsfonts} \usepackage{amssymb} \usepackage{amsbsy} \usepackage{mathrsfs} \usepackage{upgreek} \setlength{\oddsidemargin}{-69pt} \begin{document}$$^{233}$$\end{document}233U were only released in nuclear weapons fallout, either produced by fast neutron reactions or directly by \documentclass[12pt]{minimal} \usepackage{amsmath} \usepackage{wasysym} \usepackage{amsfonts} \usepackage{amssymb} \usepackage{amsbsy} \usepackage{mathrsfs} \usepackage{upgreek} \setlength{\oddsidemargin}{-69pt} \begin{document}$$^{233}$$\end{document}233U-fueled devices. This makes the \documentclass[12pt]{minimal} \usepackage{amsmath} \usepackage{wasysym} \usepackage{amsfonts} \usepackage{amssymb} \usepackage{amsbsy} \usepackage{mathrsfs} \usepackage{upgreek} \setlength{\oddsidemargin}{-69pt} \begin{document}$$^{233}$$\end{document}233U/\documentclass[12pt]{minimal} \usepackage{amsmath} \usepackage{wasysym} \usepackage{amsfonts} \usepackage{amssymb} \usepackage{amsbsy} \usepackage{mathrsfs} \usepackage{upgreek} \setlength{\oddsidemargin}{-69pt} \begin{document}$$^{236}$$\end{document}236U ratio a promising new fingerprint for radioactive emissions. Our findings indicate a higher release of \documentclass[12pt]{minimal} \usepackage{amsmath} \usepackage{wasysym} \usepackage{amsfonts} \usepackage{amssymb} \usepackage{amsbsy} \usepackage{mathrsfs} \usepackage{upgreek} \setlength{\oddsidemargin}{-69pt} \begin{document}$$^{233}$$\end{document}233U by nuclear weapons tests before the maximum of global fallout in 1963, setting constraints on the design of the nuclear weapons employed.

T he long-lived uranium (U) isotope 236 U (T 1=2 = 2.342Á10 7 years 1 ) is increasingly adopted as environmental tracer with advantageous chemical properties especially for oceanography [2][3][4][5] . U shows a conservative behavior in sea water and therefore can be transported over long distances in this environment. In oxidizing conditions of surface and ocean water uranium is present in oxidation state +VI as uranyl ion (UO 2þ 2 ) 6,7 . In the presence of complexing ligands such as carbonates or phosphates, which are readily available in ocean water, the solubility of U(VI) is enhanced by orders of magnitude [8][9][10] leading to the conservative behavior. An advantage of 236 U compared with the naturally occurring and therefore more abundant U isotopes 234 U, 235 U, and 238 U, is the high sensitivity to small anthropogenic U inputs to the large reservoir of environmental U. Considerable amounts of anthropogenic 236 U have been released into the environment by atmospheric nuclear weapons testings, reprocessing plants and reactor accidents. The total deposition as global fallout has been estimated at 900-1400 kg 5,11 and from reprocessing plants at 115-250 kg 5 . This clearly dominates over the natural global inventory of this isotope (a few kg) 12 . For time-resolved archives, elevated 236 U/ 238 U atom ratios can be attributed to a specific contamination source if the emission history is wellknown. This has been successfully demonstrated for global fallout in coral cores from the Caribbean Sea 13 and the Northwest Pacific Ocean 4 , for releases from the Sellafield reprocessing plant in sediments and water from the Irish Sea 14,15 and also for the contamination from the reactor accident in soils collected close to Chernobyl 16 . In these cases, the 236 U/ 238 U atom ratio serves as tracer for ocean currents 5,17,18 . However, in systems affected by several contamination sources with complex water circulation processes, such as the Mediterranean Sea 19 or the Arctic Ocean 20 , the lack of a second anthropogenic U isotope is a disadvantage compared with plutonium (Pu). Isotopic ratios of two anthropogenic nuclides, such as 240 Pu/ 239 Pu, allow further insight than that provided by a single isotope concentration or its ratio to an also naturally occurring isotope like 238 U. Isotopic ratios strongly depend on the production mechanism and hence, the emission source, which allows discrimination between possible origins of the contamination 21,22 . However, because Pu is a particle-reactive element, it shows high sedimentation rates in environmental waters (sea, river and fresh water reservoirs) because of the presence of colloids, and it is not well suited as a tracer for water transport processes. Recent technical developments at the Vienna Environmental Research Accelerator (VERA) enable low-level Accelerator Mass Spectrometry (AMS) measurements of anthropogenic 233 U (T 1=2 = 1.592Á10 5 years 1 ) in the environment. The low environmental abundance of 233 U is a challenge even for the highly sensitive detection technique AMS so that previous publications on 233 U either analyzed its concentration in samples collected close to a contamination source 23,24 or used 233 U, which had been added to the environmental sample, to normalize the 236 U results for mass spectrometric measurements. The combination of environmental 233 U and 236 U could play a similar role for the U isotopic system as 240 Pu/ 239 Pu for the Pu system. The isotopic ratio 233 U/ 236 U stays undisturbed by chemical fractionation in the environment as well as during sample preparation, simplifying the interpretation of the measurement results in the presence of mixing and dilution processes.
In the present study, the abundances of both 233 U and 236 U and the resulting 233 U/ 236 U atom ratios were investigated in samples from different natural reservoirs including corals from the Pacific Ocean, samples from the Irish and the Baltic Sea and peat bog samples from the Black Forest, Southwest Germany, which are influenced by different contamination sources. Our findings indicate a considerably lower production of 233 U relative to 236 U in thermal nuclear power plants compared with nuclear weapons which agrees with our understanding of the possible production mechanisms of the two isotopes. Consequently, the 233 U/ 236 U ratio has a great potential for emission source identification and hence as tracer for water transport processes. Furthermore, a time shift of −7 years in the deposition peak of 233 U from global fallout compared with 236 U was observed which indicates a more intensive use of enriched uranium in thermonuclear weapons or releases from 233 U-fueled weapons during the early phase of the US nuclear weapons testings and gives insights into nuclear weapons design where details still remain classified.

Results
Sources for anthropogenic 233 U. In general, the main emission sources for anthropogenic radionuclides are either atmospheric nuclear weapons tests or nuclear industry, i.e., reprocessing plants or reactor accidents. Since the vast majority of nuclear power plants which have been in operation until today have used a thermal neutron spectrum and U as fuel, the production of 233 U in nuclear reactors is strongly suppressed compared with 236 U 25 . Both, official sources, e.g. [26][27][28] and unauthorized web sites 29 on nuclear weapons design are naturally scarce or impossible to verify. Yet, even though there are information sources stating that at least one nuclear weapons test using a mixture of 233 U and 239 Pu as fuel has been conducted ("Teapot MET", April 1955 29 ), to our best knowledge, all nuclear weapon programs were clearly dominated by 235 U or 238 U, 239 Pu based weapons 30 . In short, the most relevant production path for 233 U via the reaction 235 U(n,3n) 233 U requires fast neutrons with energies above 13 MeV 31 . A contribution from the thorium fuel cycle 32 producing 233 U by thermal neutron capture on 232 Th can be considered as negligible. In contrast, 236 U can be also produced in nuclear power plants and fission bombs via 235 U (n,γ) 236 U using thermal neutrons, apart from the production by fast neutrons in thermonuclear weapons via the reaction 238 U (n,3n) 236 U. Therefore, a significant production can be expected in thermonuclear weapons containing uranium enriched in 235 U (sometimes referred to as oralloy). Fallout from the low-yield device "Teapot MET" (22 kt) mentioned in 29 can be assumed to be mainly locally restricted to the surrounding area of Nevada test-site (NTS) 33,34 . However, it is generally accepted that surface detonations of kilotons bombs cause tropospheric fallout, which is deposited in a band around the globe at the latitude of the test site (20 -50 N for NTS) 35 . Therefore, a contribution from the MET test to the total inventory of 233 U at the latitude band of NTS is, in principle, possible but can be expected to decrease in an eastward direction 36 . A detailed discussion of the production mechanisms of 233 U and 236 U can be found in the Methods section.
Selection of sample materials. The 233 U and 236 U content of samples from five different locations, which are summarized in Table 1, were analyzed in this study. Samples comprises sea water and sediment as well as a peat and coral core. In four cases, chemically separated U in an iron oxide matrix was available from archived AMS sputter targets (the kind of sample holder suitable for the AMS ion source) in which 236 U was previously determined. 233 U is often added as a chemical yield tracer, however, only samples which have not been spiked with 233 U during sample preparation were considered in the present work. If available, the 236 U/ 238 U data obtained in the corresponding previous study are listed in Table 1 with one sigma uncertainty. A more detailed sample description can be found in the Methods section.
The global fallout signature of 233 U/ 236 U in a peat bog core. The 236 U/ 238 U and the 233 U/ 238 U atomic ratios measured in the peat core are plotted against the age of the respective peat layer in Fig. 1a, dated by using the unsupported 210 Pb method 37 .Values for the 236 U/ 238 U ratios range from 7.2 Á 10 À7 to 9.2 Á 10 À6 and for 233 U/ 238 U from 1.1 Á 10 À8 to 1.8 Á 10 À7 (see also Supplementary Table 1). The observed 233 U concentration in this environment, which is not directly influenced by any nuclear source except global fallout as shown by analyzing the Pu nuclide vector 38 , is almost two orders of magnitude lower than the 236 U concentration. The 236 U/ 238 U data obtained in the present study agree reasonably well with the previously published data for the peat core 37 (compare Supplementary Fig. 1). Both depth profiles of 236 U/ 238 U and 233 U/ 238 U ratios (Fig. 1a) show a pronounced peak with the maximum value in 1961.5 and in 1955.3, respectively. The explosion yield of atmospheric nuclear weapons tests is narrowly distributed with an expectation value of 1959.5 and a standard deviation of 3.1 years (see Fig. 1b). This means around 90% of the total explosion yield of all atmospheric weapons tests (440 Mt 39 ) was released within only one decade and marks the most active phase of atmospheric nuclear weapons testing. Two main phases of atmospheric testing can be identified in Fig. 1b, i.e., 1952-1958 and 1961-1962, leading to the maximum global fallout in 1963, to which the 236 U/ 238 U maximum in the peat core was attributed 37,39 . The 236 U as well as the 233 U bomb peak detected in the peat core is approximated by Gaussian fits (black and gray solid lines) with similar widths, i.e., 19 ± 1 years and 18.6 ± 0.9 years (FWHM). As both nuclides were deposited predominantly during a rather narrow time interval, the peak shape results from migration of U in the peat. In contrast to the 233 U peak, the baseline of the 236 U/ 238 U does not reach pre-nuclear levels for younger layers as additional releases might have occurred. The resulting 233 U peak (peak center at AD 1953.5 ± 0.5) is shifted by 6.8 years towards older ages with respect to the 236 U bomb peak (peak center at AD 1960.3 ± 0.4).
This indicates that the maximum release of 233 U happened before the maximum deposition of global fallout and hence, can be attributed to the earlier testing phase, i.e., 1952-1958. Regarding the number of tests, the respective estimated yield and the altitude at which the tests were conducted, it can be deduced that atmospheric fallout from the earlier period was dominated by the U.S. program whereas the fallout maximum in 1963 was dominated by the USSR weapon tests 39 (see Supplementary Table 2). Considering the sampling location, the detected 233 U contamination can be therefore attributed either to some early thermonuclear explosions conducted by the US at the Pacific Proving Grounds (PPG) which are said to have used oralloy as tamper material 29 or unfissioned 233 U from the "Teapot MET" explosion in 1955.
The overall 233 U/ 236 U ratio for nuclear weapons fallout was calculated from the peak area of the two Gaussian fits of the 236 U/ 238 U and the 233 U/ 238 U data. In both cases, the sample with the age AD 1920.7 and a 236 U/ 238 U and 233 U/ 238 U atom ratio of (7.5 ± 1.5) Á 10 À7 and (1.1 ± 0.3) Á 10 À9 , respectively, serves as upper limit for the blank level which does not significantly affect the value of the overall 233 U/ 236 U isotopic ratio.
Dividing the peak area yields an average 233 U/ 236 U ratio of (1.40 ± 0.15)Á10 À2 . This value can be considered representative for compartments of the environment which do not preserve a high time resolution, and are only affected by global fallout. If the 236 U/ 238 U peak is disentangled according to the two phases of nuclear weapons testings (dashed black curves in Fig. 1a), a 233 U/ 236 U ratio of (5.1 ± 1.1)Á10 À2 for the earlier phase is obtained (see Discussion section for details).
The close-in fallout signature of the PPG in a coral core. The 233 U/ 238 U and 236 U/ 238 U atom ratios determined in the corals from Kume Island are presented in Fig. 2 as a function of the age of the respective coral band. The corals were cut along layers with low density which correspond to the fast growth rates during summer time. Hence, the year 1951, e.g., refers to the time period from summer 1950 to summer 1951. The individual 236 U/ 238 U atom ratios are in very good agreement with the results from the previous study 40 (see also Supplementary  Table 3). The stated 1 σ uncertainties of the 233 U/ 236 U ratio are clearly dominated by the comparably low statistics in case of the 233 U measurement due to the low abundance of 233 U in the corals and the availability of material left in some AMS sputter targets from the previous study.
In general, the 236 U/ 238 U and the 233 U/ 238 U atom ratio with a maximum of (1.05 ± 0.05)Á10 À8 and (1.6 ± 0.2)Á10 À10 , respectively, are almost three orders of magnitude lower than in the peat core. In the ocean water, fallout U is mixed with higher concentrations of natural U than in the peat bog so that the fallout signature is diluted before the U is concentrated in the corals. The level of the 236 U/ 238 U ratio for pre-nuclear samples is (1.0 ± 0.2)Á10 À10 and <3.1Á10 À12 for 233 U/ 238 U, respectively. Whereas two peaks of the 236 U/ 238 U data in 1954 and 1958 can be clearly identified in Fig. 2, there is only one maximum in the 233 U/ 238 U measurement data which is statistically significant, that is in the year 1958. The uncertainty of the 233 U/ 238 U ratio  29 . It also agrees with the assumption that the Ivy King test in 1952 was a pure oralloy fission device 41 and hence, did not generate enough fast neutrons required for the build-up of 233 U. Nevertheless, the 233 U abundance in the marine environment of the Pacific Ocean seems to gradually increase from 1953 on, suggesting that 233 U has been produced from the very first thermonuclear weapons, even though to a much smaller extent. The weighted average of the 233 U/ 236 U ratio (see Fig. 3) was calculated from the measured 233 U/ 238 U and 236 U/ 238 U ratios for three time periods (I-III) that are characterized by a different 233 U/ 236 U ratio. The ratios for samples before 1949 are not shown in this figure, as in most cases only upper limits for the 233 U/ 236 U ratio were obtained because of the low 233 U concentrations. In period I with no significant 233 U production, i.e., until 1956, the average 233 U/ 236 U = (0.31 ± 0.07)Á10 À2 is much lower than for the period 1957-1962. Period II is characterized by an increased release of 233 U probably caused b a  1920192519301935194019451950Year 19551965197019751980198519951990 1925 1930 1935 1940 1945 1950 1955 1960 1965 1970 1975 1980 1985 1995 1990 Fig. 1 233 U and 236 U signal in the peat bog compared with weapons yields. a Measured 236 U/ 238 U (black squares) and 233 U/ 238 U (gray dots) atom ratio in the peat core depending on the age of the peat layer. The measurement uncertainties shown are ±1 σ (s.e.m.). The solid lines represent a Gaussian fit of the 236 U (black line) and the 233 U (gray line) data indicating a time shift between the 233 U and the 236 U release. The 236 U peak can be disentangled by two Gaussian distributions (dashed black curves in a) corresponding to the two major testing phases of nuclear weapons with respect to the explosion yield (1952-1958 and 1961-1962)  by the close-in fallout of operation Hardtack I and an average 233 U/ 236 U ratio of (1.81 ± 0.15)Á10 À2 was obtained. The "1950" sample and also the "1955" sample, which corresponds to a possible first maximum in Fig. 2, show an elevated ratio but do not considerably affect the weighted average due to the large uncertainties. Starting from the year 1963 coinciding with the maximum of global fallout (period III), the ratio levels out to an average of (1.44 ± 0.12)Á10 À2 which is consistent with the global fallout average determined from the Western Europe peat samples.
The signature of nuclear power production in the Irish Sea. The 233 U/ 238 U ratios detected in Irish Sea sediment range from 9.6Á10 À9 to 5.9Á10 À8 and, hence, are comparable to the ratios found in the peat core (see also Supplementary Table 4 for details). The 233 U/ 236 U ratios of three samples, which have been diluted by a factor of 100, show a high uncertainty (Fig. 4) and therefore have a low significance for the interpretation of the 233 U/ 236 U ratios in the sediment.
The 233 U count rate from the undiluted samples was four orders of magnitude higher than from a U sample considered as instrumental blank for 233 U. Consequently, a clear 233 U signal was detected, but as shown by the depth profile in Fig. 4, the 233 U/ 236 U ratios in the sediment core are significantly lower than in the peat and the coral core. The weighted average from the sediment samples (n = 7) results in 233 U/ 236 U = (0.13 ± 0.02)Á10 À2 , which is consistent with the ratio determined in Irish Sea water of (0.11 ± 0.01)Á10 À2 . Hence, the weighted average of 233 U/ 236 U = (0.12 ± 0.01)Á10 À2 in the Irish Sea, close to the reprocessing plant Sellafield, is one order of magnitude lower than in nuclear weapons fallout found in the peat and coral core. In accordance with the theoretical discussion of the 233 U and 236 U production mechanisms in the Methods section, we attribute this low ratio to the U releases from the reprocessing plant because it indicates the lack of neutrons with energies above the threshold for the 235 U (n,3n) 233 U reaction. The elevated ratio of the sample from 19 cm depth deviates significantly from the calculated average; nevertheless it also clearly shows the low ratio expected for reactor dominated anthropogenic input.
Mixing of different source terms in the Danish straits. The measured 233 U/ 238 U, 236 U/ 238 U and 233 U/ 236 U ratios in two samples from the Danish straits (Kattegat) are given in Table 2. These two samples were collected in a similar region at a distance of only $40 km from each other and, as expected, show very similar values for the three atom ratios. The 236 U/ 238 U ratio is clearly elevated with respect to the natural abundance, which confirms the mainly anthropogenic origin of 236 U in the Danish straits. The 233 U/ 238 U ratio is quite low and comparable to the ratios found in the modern layers of the coral core from the Pacific Ocean. Within the uncertainties the 233 U/ 236 U ratios of the two samples are indistinguishable and the resulting average of (0.45 ± 0.02)Á10 À2 is situated between the value attributed to the reprocessing plant Sellafield (0.12 ± 0.01)Á10 À2 and to the global fallout (1.40 ± 0.15)Á10 À2 . This is consistent with the picture of the Danish straits being a mixing zone of water masses carrying global fallout signature with waters containing uranium originating from the reprocessing plants as well as fallout from the Chernobyl accident 42,43 .
As discussed in the previous section, no difference in the 233 U/ 236 U ratio between reprocessing plants and NPPs can be expected, and in this way no differentiation between a Chernobyl and a La Hague/Sellafield fraction is possible. However, the contribution of uranium from generic nuclear fuel and global fallout can be calculated by using a two end member linear mixing model, as commonly applied to Pu ratios, e.g., in 21 . The average 233 U/ 236 U ratio of the two Kattegat water samples and the 233 U/ 236 U ratio of global fallout (1.40 ± 0.15)Á10 À2 from the peat core and that of nuclear fuel (0.12 ± 0.01)Á10 À2 from the Irish Sea sediments yields a global fallout fraction of (25.8 ± 3.4)% at the sampling location in the Danish straits. As expected, the larger contribution comes from the nuclear power industry which is most probably caused by the considerable releases from the reprocessing plants as discussed before in this paper and in previous publications 5,18,42 .

Discussion
Environments affected by the Sellafield reprocessing plant or by nuclear weapons fallout were found to differ by one order of 1940 1942 1944 1946 1948 1950 1952 1954 1956 1958 1960 1962 1964 1966 1968 1970  NATURE COMMUNICATIONS | https://doi.org/10.1038/s41467-020-15008-2 ARTICLE NATURE COMMUNICATIONS | (2020) 11:1275 | https://doi.org/10.1038/s41467-020-15008-2 | www.nature.com/naturecommunications magnitude in their 233 U/ 236 U atom ratio. Reservoirs exposed to global fallout from nuclear weapons testings showed a 233 U/ 236 U ratio of around 1.4Á10 À2 . Depending on the contribution from close-in (PPG) fallout 233 U/ 236 U ratios up to 1.8Á10 À2 were found in a coral core from the Pacific Ocean. In contrast, the very low 233 U/ 236 U ratio of (0.12 ± 0.01)Á10 À2 detected close to Sellafield can be generally assigned to spent fuel from thermal NPPs. By analyzing the 240 Pu/ 239 Pu atom ratio and the 238 Pu/ 239þ240 Pu activity ratio, it has been shown that the present sediment core is neither influenced by the reprocessing of weapon-grade plutonium from the early operation of the reprocessing plant nor by global fallout, but carries the signature of high burn-up Pu which is characteristic for spent fuel from NPPs 14 . At present, the large majority of all NPPs in operation is still based on the U fuel cycle and uses a thermal neutron spectrum 44 , so that the different 233 U/ 236 U ratio allows a discrimination between emissions from civil nuclear industry and nuclear weapons fallout.
This finding is in good agreement with our theoretical considerations on the production of 233 U (see "Methods" section for details) from which we conclude that a significant production of 233 U is only possible in thermonuclear weapons using a tamper of highly enriched 235 U but not in U-based thermal nuclear power plants. However, the 233 U/ 236 U ratio from the period of testing at the PPG (II) is too low to explain the ratio found for global fallout, as the peat samples suggest a considerable dilution of the 233 U signal from the PPG by 236 U produced in a later phase of atmospheric nuclear weapons testing. If we assume that the input of anthropogenic uranium (U) can be attributed in a simplified view to only two time intervals corresponding to the two most active phase of atmospheric nuclear weapons testings, i.e., 1952-1958 and 1961/62 (compare Fig. 1b), then we can disentangle the isotopic signatures of the two phases. The dashed black curves in Fig. 1a show the fit of the corresponding Gaussian peaks to the data from the peat core. For this, we assume that all 233U originates from the PPG and thus shows up in the peak corresponding to the earlier phase of testing. This fixes the time offset of the peat data vs. the UNSCEAR data 39 for the explosion yields (Fig. 1b) to −2.3 years and the width of the distribution with σ = 16.8 years. The offset is calculated from a shift of the 233 U peak center at 1953.5 compared with the center of the distribution published by UNSCEAR at 1955.8 and is probably caused by the migration of U in the peat. The time difference between the 233 U/ 238 U and the 236 U/ 238 U peak center is taken as 5.9 years according to the UNSCEAR data. The ratio of the areas for the earlier time interval corresponds to 233 U/ 236 U = (5.1 ± 1.1)Á10 À2 . This is significantly higher than source ratio of (1.81 ± 0.15)Á10 À2 determined for the PPG in the coral samples. This points to an additional source of 233 U for which the 233 U-fueled "Teapot MET" explosion is a potential candidate. In order to estimate the contribution from the "Teapot MET" test to the global fallout, the source function of 233 U could be assessed sampling at different distances to the Nevada Test Site. As we can explain the peat data without a 233 U source in the later testing phase (1961-1962), a substantial use of oralloy in thermonuclear weapons seems unlikely. This phase was dominated by the USSR testing for which little information is available. At least, initial plans of the USSR suggest the use of natural or even depleted uranium as tamper in the RDS-37 device 45 , which was the first staged thermonuclear bomb tested by the USSR in November 1955 29 . Our findings, therefore, impose constraints on the weapons design and the resulting source terms also for other radionuclides released into the environment by nuclear weapons tests. For close-in fallout from the PPG, our data from the coral core already suggest a strong correlation between the 233 U/ 236 U ratio and the 235 U enrichment of the thermonuclear device. One of the reported aims of Hardtack I was the development of tactical nuclear weapons which should result in smaller and more efficient devices 26 . As it is known that a higher yield per mass of the device and thus a higher efficiency can be achieved by replacing natural uranium tamper by oralloy 46 , it is well conceivable that such devices were tested during Hardtack I. In addition, elevated 236 U/ 239 Pu ratios found in corals at Enewetak Atoll from the same time period also point to an oralloy tamper in one or more of the explosions during this test series 47,48 . Analysis of local fallout 233 U/ 236 U ratio from test sites can, therefore, add information on the fuel used during the different test series. Samples from the former USSR test sites Semipalatinsk (Kazakhstan) and Novaya Zemlya (Arctic Ocean) would be especially interesting because even less information on the USSR weapons design is available.
In addition, the study of the 233 U/ 236 U ratios at the different test sites is necessary to assess the effect of in situ production of 233 U by neutron capture on 232 Th contained in the soil/rocks which might offer the possibility to distinguish also local and global fallout. This could be especially relevant for surface and low altitude explosions, during which the surface material was exposed to the nuclear fire ball and got incorporated into the blast of the explosion 49 . Child and Hotchkis 24 found 233 U concentrations up to a factor of 100 higher within a 200 km zone around ground zero at Emu field and on the Montebello Islands 24 which they attributed to in situ production, followed by mobilization of the irradiated material. In contrast to this spatially very restricted local fallout from low-yield weapons tests 39 , global fallout is known to have been caused by the large, in particular thermonuclear tests conducted at the PPG by the US and at Novaya Zemlya test site by the USSR 50 . Therefore, small scale explosions, conducted also at other test sites like the Semipalatinsk or Nevada test site, can be considered as a negligible contribution to the in situ produced 233 U in global fallout. The estimation of the global budget of in situ produced 233 U is very difficult, as the production and mobilization rate depends on a number of parameters which are not sufficiently well known to the authors. The 233 U data from the peat core indicate a minor contribution from the Novaya Zemlya test site where the test program was dominated by air tests 39 in contrast to the near-surface explosions at the PPG where coral sand from the atolls was incorporated into the blast. For example, the Tsar bomb in October 1961 (50 Mt explosion yield) is known to have strongly affected the surface of Novaya Zemlya 51,52 so that a mobilization of irradiated material and thus, in situ produced 233 U, could be expected. Nevertheless, the measured 233 U data do not show a significant contribution from the later testing phase in 1961-62.
Apart from the mentioned local effects, the large potential for emission source identification in combination with the conservative behavior of U in oxic natural waters, makes the 233 U/ 236 U ratio well suited for tracing environmental transport processes. Compared with other mobile radionuclides, which are already used for oceanography, e.g., 137 Cs, 129 I, 99 Tc and the corresponding ratios, the 233 U/ 236 U ratio is independent from the emission history of the specific source, as it only depends on the fuel and the neutron spectrum and can be considered as more reliable. Especially, in complex oceanographic settings like the Baltic Sea with several contamination sources, i.e., global fallout, the reprocessing plants La Hague and Sellafield and fallout from Chernobyl, the detection of 233 U/ 238 U in addition to 236 U/ 238 U can quantify the contribution from global fallout. This was demonstrated for two samples collected at the Danish straits (Kattegat) for which a global fallout contribution of 25% was obtained. In case of a nuclear accident, the surplus of potential U releases to the background due to nuclear weapons can now be quantified.
In addition to the samples analyzed in the present study, which were collected in the Northern Hemisphere, future studies should aim to map the 233 U/ 236 U ratio for the Southern Hemisphere. As observed for Pu isotopes, isotopic ratios on the Southern Hemisphere show a higher variability [53][54][55] , because weapons fallout is dominated by the local fallout of the French tests in French Polynesia and the British tests in Australia. A next step in method development will be establishing a standard material for 233 U/ 236 U/ 238 U to be shared with other AMS laboratories.

Methods
Detailed sample description and preparation. The 233 U/ 236 U atom ratio was determined in seven samples from different depths of a sediment core (3-47 cm) from the Irish Sea which was collected by the Federal Maritime and Hydrographic Agency, Germany. Previous work suggests that the core showed no good stratigraphy 14,56 but was probably mixed by environmental reworking. The 236 U/ 238 U ratios determined in the sediment samples ranged from 1.35Á10 À5 to 4.36Á10 À5 and thus, were considerably elevated compared with natural background (10 À14 -10 À1012 ) or global fallout (% 5Á10 À811 ). The samples were clearly affected by the large amounts of uranium from spent fuel discharged by the Sellafield reprocessing plant. At the beginning of the plant operation in the 1950s and 60s, effluents were characterized by a low 240 Pu/ 239 Pu isotopic ratio (<0.07) due to the production of weapon-grade Pu. Later emissions originated from the reprocessing of spent fuel from thermal Nuclear Power Plants showed 240 Pu/ 239 Pu ratios higher than 0.20 21 . Dating of the sediment core using its 241 Pu content resulted in a maximum age of 34.0 ± 0.4 years before 2010 56 and, therefore, an isotopic signature of high burn-up fuel from NPPs was expected. This has been confirmed by the high 240 Pu/ 239 Pu ratios ranging from 0.20 to 0.33 detected in the sediment core 14 . Since the 236 U count rates detected from the Irish Sea sediment were considerably larger than 1000 s À1 in 14 , and thus prone to cross-contamination, the first batch of three original samples was diluted by approximately a factor 100.
In addition to the sediment samples, Irish Sea water, i.e., the certified reference material IAEA-381, now available as IAEA-443 57 , was analyzed with respect to its 233 U/ 236 U atom ratio within the scope of the present study. For this sample, no archived separated U target material was available and thus it was prepared from the original reference material. A time-resolved profile of the 236 U concentration over the past 80 years starting from 1992 as youngest age in an undisturbed ombrotrophic peat core was obtained in 37 . The layers of the peat core were dated by using the unsupported 210 Pb method. The data for the 236 U/ 238 U ratio showed a clear bomb peak with a maximum 236 U/ 238 U ratio of (7.4 ± 0.4)Á10 À6 at a depth corresponding to AD 1959. This is in good agreement with the most active phase of atmospheric nuclear weapons testing in the late 1950s and early 1960s. The analysis of the Pu isotopic ratios supports the finding that the peat is exclusively affected by global fallout 38 . Within the scope of the present study, the 233 U and 236 U concentrations were analyzed in 23 samples from the peat core covering the relevant time span from 1921 to 1992.
Due to their annual growth bands, corals represent a high-resolution archive of U, which is incorporated into the carbonate skeleton of the corals from the ocean water.
The 236 U/ 238 U ratios detected in the corals from Kume Island were clearly influenced by the close-in fallout 50 from the high-yield nuclear weapons tests conducted by the USA at the Pacific Proving Grounds (PPG), the Marshall Islands. The PPG are located in the North Equatorial current, which transported the closein fallout west and then, turning into the Kuroshio current, to the northeast, passing the location of Kume Island. Two distinct peaks were found with a maximum 236 U/ 238 U ratio of (11.0 ± 1.2)Á10 À9 and (8.55 ± 1.17)Á10 À9 , respectively, in the years of most intense weapons testing at the PPG regarding the yield of the explosions (Supplementary Table 1). Consequently, the two maxima were attributed to the two largest test series at the PPG, i.e., Operation Castle in 1954 and Hardtack I in 1958. In the present study, the 233 U/ 236 U ratio was analyzed in coral samples from Kume Island corresponding to the time interval from 1939 to 1970 with annual resolution.
From an on-going project on the distribution and temporal evolution of the 236 U concentration in the Baltic Sea 42 , two samples collected in the strait between Denmark and Sweden (Kattegat) were chosen for additional 233 U analysis. The Danish straits are a very interesting maritime environment for the study of the physio-chemical behavior of U, as brackish water from the Baltic Sea mixes with saline water from the North Sea and the Atlantic Ocean. Using the distribution of 129 I and 233 U in the North Sea, it has been shown 2,18 that releases from Sellafield and in particular from La Hague, are transported towards the Danish coast by the respective sea currents. This leads to the mixing of uranium originating from the reprocessing plants with U from global fallout. Accordingly, 236 U/ 238 U ratios detected in sea water from the Danish straits were found to be around four times higher than expected from global fallout indicating the presence of at least one additional contamination source 42 . Here, emissions from the reprocessing plants as well as fallout from the Chernobyl accident have to be considered as possible explanation.
Accelerator Mass Spectrometry requires the uranium to be embedded in several mg of solid material, usually Fe 2 O 3 , which means that a specific sample preparation has to be applied to the original environmental sample. A detailed description of the chemical extraction and purification of uranium from the different types of sample material is given in the respective previous publications, i.e., Irish Sea sediment 14 , peat bog 37 , corals from Kume Island 40 and Baltic Sea water 58 . Some archived uranium samples pressed into sputter targets for the ion source of VERA could be directly reused for the present work. A slightly modified procedure for the actinide separation 59 was applied to 200 mL of the reference material IAEA-381 Irish Sea water. U was first pre-concentrated using a Fe(OH) 3 co-precipitation and then purified using the UTEVA © resin from Eichrom Technologies, Inc. The final process step of the AMS sample preparation in all projects was a co-precipitation of U with Fe(OH) 3 which was then converted to Fe 2 O 3 by calcination in a furnace at 800-900 C. From the Irish Sea sediment different aliquots were prepared in the initial project with variations in the sample preparation. For the present work, we selected aliquots without any spike and thus, in some cases used different aliquots from the same original sample material than those published in ref. 14 . For the dilution of three of the samples, the sample material was removed from the respective archived sputter target and dissolved in 8.5 M HCl. A total of 100 mg of additional Fe were dissolved in each sample solution. Then, U was co-precipitated with Fe(OH) 3 using NH 4 OH. Starting from the Fe(OH) 3 , AMS targets were prepared as described before. As the 233 U count rates from the diluted samples were rather small (around 10 À3 s À1 ), a second set of sediment samples were measured in the original sample holder without additional treatment.
AMS measurement procedure. 236 U and 233 U were detected by the ultra-sensitive detection method Accelerator Mass Spectrometry (AMS) at the Vienna Environmental Research Accelerator (VERA), Austria. Actinides, in particular 236 U, are routinely analyzed at the AMS facility VERA and the corresponding set-up and measurement procedure has been described in detail before, and most recently in 60 . In short, U is extracted from a cesium sputter ion source as UO À molecules and then injected into the accelerator, operated at a terminal voltage of 1.65 MV for actinide measurements. A relatively high helium pressure is used in the terminal stripper to suppress the molecular background 61 , resulting in a stripping yield of around 21% for the selected charge state 3 þ . Isotopic background on the highenergy side, mainly due to 235 U and 232 Th, which is injected into the accelerator as 235 U 16 O 1 H À and 231 Th 16 O 1 H À , is efficiently filtered out by a 90 analyzing magnet, a Wien filter, an electrostatic analyzer, and a second, recently installed, 90 magnet. The remaining ions are identified in the final detection system, a Bragg type ionization chamber 62 . With this setup an overall detection efficiency of 5Á10 À4 and a detection limit for 236 U/U below 10 À11 was achieved 63 . The detection efficiencies for 233 U and 236 U can be assumed to be comparable due to the similar mass of the two isotopes. For a uranium oxide target prepared from our in-house 236 U standard Vienna-KkU ( 236 U/ 238 U = (6.98 ± 0.32)Á10 À11 12 ) mixed with Fe 2 O 3 (1:30), which can be considered as machine blank for 233 U, an upper limit for the 233 U/U ratio of 6Á10 À13 was measured. However, possible contamination from sample preparation are not included in this blank. Therefore, we made the conservative assumption that our blank level is equal or below the concentration of the sample with the lowest count rate of 233 U and 236 U events, respectively, for each sample material.
The 236 U and 233 U count rates in the ionization chamber were normalized to the 238 U current measured in a Faraday cup after the second electrostatic analyzer in order to take into account fluctuations in the source output and the ion optical transmission through the accelerator. The difference in detection efficiency between the Faraday cup and the ionization chamber was corrected by using the inhouse standard Vienna-KkU. A dead time correction was applied to the detector count rates of the undiluted samples from the Irish Sea sediment.
Comparison of 233 U and 236 U production The thermal neutron capture on 235 U and in particular the 238 U (n,3n) 236 U reaction induced by fast neutrons in thermonuclear explosions have been previously identified as the most important production channels for 236 U 11,12 The (n, 2n) and (n, 3n) reactions in (1), (2) and (3) require threshold energies of 6 MeV 64 and 13 MeV 31 , respectively. A production via these reactions in nature, therefore, is only possible by neutrons from cosmic rays at the presence of U, which is limited to the shallow subsurface of the Earth's crust (upper 2 m).
In addition, the cross-sections for the (n,3n) and (n,2n) reactions on 235 U, 238 U, and 234 U are low, i.e., below 1 barn, as demonstrated in Supplementary Fig. 2, showing F/EXFOR data 65,66 . Consequently, these reaction channels are negligible compared with thermal neutron capture on 232 Th (reaction (4)), which has a cross-section of 7.37 barn, especially in minerals with elevated 232 Th content, e.g., monazite. Peppard et al. demonstrated the presence of natural 233 U in pitchblende and Brazilian monazite concentrate by isolating the decay product 225 Ac. They observed a mass ratio of 233 U/ 238 U of (1.3 ± 0.2)Á10 À13 in pitchblende and (4 ± 2)Á10 À1167 in monazite. We have detected isotopic ratios of 233 U/U in yellowcake samples in the range of several 10 À14 at the Vienna Environmental Research Accelerator (VERA), as part of this work. When discussing anthropogenic sources for 233 U, it has to be noted that from a neutronics point of view, 233 U is very well suited as fuel for nuclear power plants and also for nuclear weapons. According to reaction (4), it can be efficiently bred from 232 Th which is the starting point for the proposed thorium fuel cycle 32 . In that way, 1500 kg of 233 U were synthesized in the USA 68 . Several reactor prototypes were operated especially in the 60s and 70s, e.g., the pebble-bed reactor in Germany, or the DRAGON experimental reactor in England. However, these prototypes or research reactors are by far outnumbered by the industrial application of the uranium fuel cycle in NPPs using a thermal neutron spectrum and the reprocessing of the fuel involved. Only extremely small amounts of 233 U are produced in U-fueled NPPs because of the small cross-sections involved (reactions (1)-(3)). Furthermore, the average energy of neutrons emitted by the thermal fission of 235 U is around 2 MeV with the energy distribution for the number of neutrons N(E) being described by the well-known Watt spectrum. Integration of the corresponding empirical formula NðEÞ ¼ 4:75 Á 10 6 sinh ð2EÞ 0:5 Á e ÀE ð5Þ with E given in MeV, results in a fraction of only 2:4% of all fission neutrons with energies above the threshold for (n,2n) reactions, i.e., 6 MeV, and of 0.01% with energies above 13 MeV, the threshold for (n,3n) reactions. In contrast, 235 U shows a thermal neutron capture cross-section of 95 b 1 , so that considerable amounts of 236 U are produced in NPPs. This difference in the production mechanisms of 233 U and 236 U is supported by the very low 233 U/ 236 U ratios of 1Á10 À6 obtained by reactor model calculations for the fuel of pressurized water reactors 25 . Apart from the direct release by 233 U-fueled weapons, i.e., the "MET" explosion of operation "Teapot" mentioned before, the only relevant production path for 233 U seems to be the reaction 235 U(n,3n) 233 U. Neutrons with energies of 14.1 MeV are provided in a thermonuclear device by the fusion reaction of deuterium and tritium 69 via d þ t ! α ð3:5 MeVÞ þ nð14:1 MeVÞ ð 6Þ Supplementary Table 1 gives an overview over the largest explosions regarding the yield during the era of atmospheric testing. The largest pure fission bomb tested purportedly using enriched 235 U, Ivy King, had a yield of 0.5 Mt 41,70 . For weapons tests with higher explosion yields, a device-dependent percentage of the energy is produced by fusion reactions that means neutrons above the threshold energy for the build-up of 233 U were released in the corresponding devices. Comparing Supplementary Fig. 1, the cross-section for the 235 U(n,3n) 233 U reaction at this neutron energy is maximum 0.1 b whereas the 238 U(n,3n) 236 U reaction has a cross-section of around 0.5 b. Therefore, a high 233 U/ 236 U ratio can only be expected in thermonuclear weapons containing uranium enriched in 235 U (e.g., oralloy, more than 90 % enriched 30 ). It has been reported that in the well-known Teller-Ulam configuration of thermonuclear weapons, oralloy was used as socalled blanket or tamper in a few devices which exploded during the period of atmospheric testings, i.e., Castle Nectar (1954) and Redwing Cherokee (1956) 29 with an explosion yield of 1.7 Mt and 3.8 Mt, respectively. Due to the limited experimental data on the production crosssection of 233 U (compare Supplementary Fig. 1) and the lack of information on the construction details of nuclear devices, a theoretical prediction of the 233 U/ 236 U ratio in global fallout can only be roughly estimated. Assuming a nuclear device with an average enrichment of 60% and only considering the 14 MeV cross-sections for the respective (n,3n) reactions results in a 233 U/ 236 U ratio of 4 %. Production of 236 U via neutron capture on 235 U can be neglected as the corresponding cross-section is below 10 À3 b for 14 MeV neutrons 65 . This theoretical value for the 233 U/ 236 U ratio only serves as an estimate for the order of magnitude; the production of both nuclides is more complicated than described before, because of possible destruction and repeated capture processes. As most nuclear devices are supposed to have been equipped with a tamper made from natural uranium 29 , the ratio in global fallout is probably further decreased. In general, the environmental 233 U concentrations are expected to be about 100 times lower than those of 236 U, i.e., 233 U/ 236 U % 1 %. To summarize, on average, fallout from nuclear weapons tests should show a higher 233 U/ 236 U ratio than emissions from thermal nuclear power plants or reprocessing plants which is in agreement with our measurement results and allows source identification for environmental contamination.

Data availability
The source data underlying Figs. 1a, 2, 3 and 4 and