The neutrino was proposed by Wolfgang Pauli in 1930 to explain the continuous energy spectrum of nuclear beta rays. By Pauli’s hypothesis the missing energy was carried off by a lamentably “undetectable” particle. Enrico Fermi succeeded in formulating a theory for calculating neutrino emission in tandem with a beta ray1. Detecting Pauli’s particle required exposing many targets to an intense neutrino source. While working on the Manhattan Project in the early 1940s Fermi succeeded in producing a self-sustaining nuclear chain reaction, which by his theory was recognized to copiously produce antineutrinos. Antineutrino detection projects were staged near nuclear reactors the following decade. In 1955, Raymond Davis, Jr. found that reactor antineutrinos did not transmute chlorine to argon by the reaction: 37Cl (, e) 37Ar2. This result permitted the existence of Pauli’s particle only if neutrinos are distinct from antineutrinos. Davis later used the chlorine reaction to detect solar neutrinos using 100,000 gallons of dry-cleaning fluid deep in the Homestake Gold Mine. Reactor antineutrinos were ultimately detected in 1956 by Clyde Cowan and Fred Reines by recording the transmutation of a free proton by the reaction 1H (, e+) 1n3,4. This detection confirmed the existence of the neutrino and marked the advent of experimental neutrino physics.

Almost 60 years later neutrino research remains an active and fruitful pursuit in the fields of particle physics, astrophysics and cosmology. In addition to nuclear reactors and the Sun, detected neutrino sources include particle accelerators5, the atmosphere6,7, core-collapse supernovae8,9,10,11, the Earth12,13 and most recently the cosmos14. We now know that neutrinos and antineutrinos have “flavor” associations with each of the charged leptons (e, μ, τ) and these associations govern their interactions. Neutrino flavors are linear combinations of neutrino mass eigenstates (ν1, ν2 and ν3). This quantum mechanical phenomenon, known as neutrino oscillation, changes the probability of detecting a neutrino in a given flavor state as a function of energy and distance. Neutrino flavor oscillations along with their low cross section provide a glimpse into some of the most obscured astrophysical phenomena in the universe and most recently the otherwise inaccessible interior of our planet. Antineutrinos emanating from the interior of our planet constrain geochemical models of Earth’s current radiogenic interior. Antineutrino observations of the modern Earth’s interior coupled with cosmochemical analysis of chronditic meteorites from the early solar system allow scientists to model the geochemical evolution of the Earth across geologic time.

Recently, the blossoming field of neutrino geoscience, first proposed by Eder15, has become a reality with 130 observed geoneutrino interactions12,13 confirming Kobayashi’s view of the Earth being a “neutrino star”16. These measurements have constrained the radiogenic heating of the Earth along with characterizing the distribution of U and Th in the crust and mantle. The development of next generation antineutrino detectors equipped with fast timing (~50 ps) multichannel plates17 coupled with Gd/Li doped scintillator will allow for the imaging of antineutrino interactions. The imaging and subsequent reconstruction of antineutrino interactions produce directionality metrics. Directionality information can be leveraged for novel geological investigations such as the geo-neutrinographic imaging of felsic magma chambers beneath volcanos18. These exciting geophysical capabilities have significant overlap with the non-proliferation community where remote monitoring of antineutrinos emanating from nuclear reactors is being seriously considered19.

Antineutrino Global Map 2015 (AGM2015) shown in Fig. 1 merges geophysical models of the Earth into a unified energy dependent map of flux, both natural and manmade, at any point on the Earth’s surface. We provide the resultant flux maps freely to the general public in a variety of formats at AGM2015 aims to provide an opensource infrastructure to easily incorporate future neutrino observations that enhance our understanding of Earth’s antineutrino flux and its impact on the geosciences. In this study we first describe the particle physics parameters used in propagating antineutrino oscillations across the planet’s surface as shown in Fig. 2. A detailed description of the incorporation of anthropogenic and geophysical neutrino energy spectrum from 0–11 MeV is presented which allows for the four-dimensional generation (latitude, longitude, flux and energy) of the antineutrino map as shown in separate energy bins in Fig. 3. A vertically stratified model of the Earth’s density, shown in Fig. 4, based on seismological derived density models are combined with a cosmochemical elemental abundances to determine the geological signal of antineutrinos. This signal is then constrained by geo-neutrino measurements from KamLAND and Borexino and first order uncertainties associated with AGM map are then presented.

Figure 1
figure 1

AGM2015: A wordlwide flux map combining geoneutrinos from natural 238U and 232Th decay in the Earth’s crust and mantle as well as manmade reactor- emitted by power reactors worldwide.

Flux units are at the Earth’s surface. Map includes of all energies. Figure created with MATLAB45.

Figure 2
figure 2

AGM2015 reactor- flux in the 3.00–3.01 MeV energy bin (in logspace color).

Flux units are at the Earth’s surface. Note the visible θ12 oscillations at ~100 km wavelength. Figure created with MATLAB45.

Figure 3
figure 3

AGM2015 flux (/cm2/s/keV) displayed at 6 select energy bins out of the 1100 total AGM2015 energy bins, which uniformly span the 0 MeV–11 MeV energy range.

Each energy bin is 10 keV wide. In conjunction with 720 longitude bins and 360 latitude bins, the highest resolution AGM2015 map is a 360 × 720 × 1100 3D matrix comprising ~300 million elements total. Figure created with MATLAB45.

Figure 4
figure 4

AGM2015 luminosity per km2 per CRUST1.0 layer.

Each CRUST1.0 layer is composed of 180 × 360 1° tiles, each with a defined thickness (ranging from 0–78 km) and density (ranging from 0.9–3.4 g/cm3). Note the layers have different colorbar scales. Figure created with MATLAB45.

Neutrino Oscillations

AGM2015 incorporates the known 3-flavor oscillation behavior of antineutrinos. This starts with the standard 3-flavor Pontecorvo Maki Nakagawa Sakata (PMNS) matrix U:

where cij = cos(θij) and sij = sin(θij) and θij denotes the neutrino oscillation angle from flavor i to flavor j in radians. In this paper we assume

per a global fit by Fogli et al.20 in the case of θ12 and by measurements at the Day Bay experiment21 in the case of θ13. Phase factors α1 and α2 are nonzero only if neutrinos are Majorana particles (i.e. if neutrinos and antineutrinos are their own antiparticles) and have no influence on the oscillation survival probabilities, only on the rate of possible neutrino-less double beta decay. We assume α1 = α2 = 0 in this work. We likewise assume phase factor δ = 0, though this assumption may change in the future if evidence is found to support neutrino oscillations violating charge parity (CP) symmetry.

The probability of a neutrino originally of flavor α later being observed as flavor β is:

where E is the neutrino energy in GeV, L is the distance from its source the neutrino has traveled in km and the delta-mass term , in eV2. The last approximation assumes no charge parity (CP) violation (δ = 0), causing the imaginary terms to fall out. The * symbol denotes a complex conjugate and Uij denotes the element of the PMNS matrix U occupying the ith row and jth column. Equation (3) can be employed to determine the ‘survival probability’ of a of energy E GeV later being observed as the same flavor a distance L km from its source. In particular, the Pee survival probability of most interest to this paper can be expressed as Equation (4):

For simplicity we ignore the Mikheyev-Smirnov-Wolfenstein (MSW) effect22 on neutrinos as they travel through the Earth. We use the neutrino mixing angles and mass constants from Fogli et al. 201220 and Daya Bay 201421 to evaluate Equation (4) for all source-observer ranges and energies used in AGM, giving us the survival probability of seeing each source from each point in the map at each energy level. This is not a trivial task, requiring >1 × 1015 evaluations of Equation (4) for a full AGM2015 rendering. This is broken down into ~1 × 106 point sources, ~1 × 106 locations on the map at which the flux is evaluated and ~1 × 103 energy bins spanning the MeV energy range as shown in Fig. 3. Equation (4) can best be visualized in Fig. 2, which shows the θ12 ripples in the 3 MeV worldwide reactor- flux.

Reactor Antineutrinos

Reactor experiments have proven the viability of unobtrusive reactor monitoring and continue to contribute important information on neutrino properties including the possibility of additional light “sterile” neutrino flavors23. We use the International Atomic Energy Agency’s (IAEA) Power Reactor Information System (PRIS)24 to identify and locate 435 known man-made reactor cores in operation at the time of this writing. PRIS categorizes reactors into four states:

  • Operational

  • Under Construction

  • Temporary Shutdown

  • Permanent Shutdown

  • AGM2015 includes all “Operational” or “Temporary Shutdown” reactors, including many reactors in Japan affected by the Fukushima-Daiichi disaster, which are classified as “Temporary Shutdown” rather than “Permanent Shutdown.” PRIS shows 435 Operational and Temporary Shutdown reactor cores distributed among 193 sites, with 870 GWth total output after load factor considerations and 72 reactor cores among 42 sites (total 156 GWth at 100% load factor) currently Under Construction. The PRIS database reports thermal capacity directly, which is typically about three times electrical capacity (most reactors are about 30% efficient in converting heat into electricity). Historical “load factors” of each core are used to convert the total thermal capacity to projected current and future thermal power output. Load factors account for the down-time related to maintenance and other outages, allowing for AGM2015 to be a reliable estimate of worldwide antineutrino flux in its year of release. Typical PRIS load factors range from 70% to 90%. The 3 MeV AGM2015 reactor- flux map due to these 435 Operational and Temporary Shutdown reactor cores is shown in Fig. 2.

  • The reactor- energy spectrum assumes the shape of an exponential falloff in energy, with most reactor- released at the lowest energies. To obtain an reactor scaling we assume:

  • The mean energy released per fission Ef is around 205 MeV25.

  • The reactor thermal power Pth is related to the number of fissions per second Nf = 6.24 × 1021s−1Pth[GW]/Ef[MeV]25.

  • 6  created per fission19

  • 2  created per fission on average above the inverse beta decay (IBD) energy threshold of Eν ≥ 1.8 MeV19.

These assumptions yield 1.83 × 1020 (of all energies) emitted from a reactor, with 0.61 × 1020 emitted above the 1.8 MeV IBD detection threshold. This is a mean value representative of a typical pressurized water reactor at the beginning of its fuel cycle19. We find the summed worldwide reactor power output to be 870 GWth and the resultant luminosity to be and 0.04 TW. Jocher et al.26 is recommended for a deeper discussion of reactor- detection via IBD detectors.


Observations from geology, geophysics, geochemistry and meteoritics allow for a range of non-unique solutions for the composition of the Earth. The relative proportion of Fe, O, Mg and Si in chondritic meteorites individually varies by ~15% each and reflects spatial and temporal differences in where these rocks formed in the early solar nebula. Likewise, refractory elements have 25% variation in their relative abundance, which translates into a factor of two in absolute concentration difference of these elements. Even greater enrichment factors of these elements occur when the volatile inventory (e.g., H2O, CO2, N2) is mostly lost, as during terrestrial planet assembly. Finally, because the Earth’s core is taken to have negligible amounts of Th, U and K27,28,29, due to their limited solubility in core-forming metallic liquids, this becomes another 50% enrichment factor in the radiogenic elements in the silicate Earth. Consequently, compositional models predict between 10 and 30 ng/g U (and Th/U = 3.9, the chondritic ratio) for the silicate Earth. Given the planetary ratio of Th/U and K/U (1.4 ×104)30 and the absolute U content of the silicate Earth, its heat production for a 10 ng/g U model roughly corresponds to a surface heat flow of 10 TW and likewise 30 ng/g U to ~30 TW. Estimates of the Earth’s radiogenic heat production thus vary from low power models (10–15 TW of power from K, Th and U), through medium power models (17–22 TW) and to high power models (>25 TW)31. Accordingly, detecting the Earth’s flux of geoneutrinos can provide crucial data to test competing theories of the bulk Earth.

Two observatories, one in Japan (KamLAND) and one in Italy (Borexino), are making ongoing measurements of the surface flux of geoneutrinos at energies above the IBD threshold energy Eν ≥ 1.8 MeV. At Japan the flux measurement is (3.4 ± 0.8) × 106 cm−2 s−112, while at Italy the flux measurement is (4.3 ± 1.3) × 106 cm−2 s−113. Note that it is sometimes convenient to express geoneutrino flux as a rate of recorded interactions in a perfect detector with a given exposure using the Terrestrial Neutrino Unit (TNU)32, however in this work we focus on simple flux () and luminosity ().

AGM models the Earth as a 3D point cloud consisting of roughly 1 million points. National Oceanic and Atmospheric Administration (NOAA) Earth TOPOgraphical 1 (ETOPO1) “ice” data33 is used to provide worldwide elevations with respect to the World Geodetic System 84 (WGS84) ellipsoid. Zero-tide ocean surface corrections to the WGS84 ellipsoid were obtained from the National Geospatial-Intelligence Agency (NGA) Earth Gravitational Model 200834 (EGM2008) for modeling the ocean surface elevations around the world. Underneath these surface elevations we model 8 separate crust layers using CRUST 1.035, shown in Fig. 4, as well as a 9th adjoining layer per Huang et al.36 which reaches down to the spherical mantle, creating a seamless earth model. Certain crust tiles which are too large (about 200 km across at the equator) to be adequately modeled as point sources are instead modeled as collections of smaller tiles using numerical integration, which recursively subdivides large tiles into progressively smaller sub-tiles until the contribution of each is less than 0.001 TNU.

Geoneutrino flux is produced from the decay of naturally occurring radioisotopes in the mantle and crust: 238U, 232Th, 235U, 40K, 87Rb, 113Cd, 115In, 138La, 176Lu and 187Re37. However, we only consider 238U and 232Th in our flux maps as all other elements’ energy spectrum is considerably below the IBD energy threshold of Eν ≥ 1.8 MeV. All abundances for the crust and mantle can be seen in Table 1. As shown in Table 2, K is the largest contributor to luminosity but its energy is below the IBD threshold. All elements other than U, Th and K have a negligible contribution to the Earth’s luminosity.

Table 1 AGM2015 distribution and properties of U, Th and K, which are the main emitters of electron antineutrinos.
Table 2 Contribution of geoneutrino luminosities L in AGM2015 for 238U, 232Th and 40K emitted by the Earth.

Successful detection of below 1.8 MeV remains elusive; if successful the incorporation of the remaining radioisotopes would be beneficial to future versions of AGM. The Earth’s core was assumed to have no significant contribution to the flux due to limiting evidence for a georeactor38 and no appreciable amount of 238U, 232Th, or 40K isotopes27. While certain core models support upper limits of K content at the ~100 ppm level28, which would be sufficient for up to ~1–2 TW of radiogenic heating in the present day, “constraints on K content are very weak”29 and in the absence of stronger evidence we’ve chosen to assume a K-free core.

Mantle abundances were derived from empirical geo-neutrino measurements at KamLAND12 and Borexino13. We deconstructed the reported geo-neutrino flux from each observation into separate contributions from U and Th according to a Th/U ratio of 3.9. From each of these, we subtracted the predicted crust flux contributions36 at each observatory, averaging the asymmetric non-gaussian errors, to arrive at estimates of the mantle contributions. We then combined the estimates of the mantle U flux and the mantle Th flux contributions from each observation in a weighted average. The resulting best estimates for the mantle U and Th flux contributions were finally converted to homogeneously distributed mantle abundances using the spherically symmetric density profile of the Preliminary Reference Earth Model (PREM)39 along with a corresponding correction to account for neutrino oscillations. Corresponding values for K were found by applying a K/U ratio of 13,800 ± 130030. The resulting AGM2015 U, Th and K mantle abundances are presented in Table 1. The main sources of uncertainty in these estimates are the observational errors in the flux measurements and limited knowledge of the subtracted crust fluxes. A detailed description of the methods and relevant conversion factors used here are presented in Dye31.

AGM2015 neutrino luminosities are for total numbers of neutrinos. Although almost all are originally emitted as electron antineutrinos, on average only ~0.55 of the total remain so due to neutrino oscillations. We calculate the total Earth luminosity to be s−1. A detailed breakdown of 238U, 232Th and 40K geoneutrino luminosity from the lithosphere and mantle can be seen in Table 2 (for all energies), as well as in Table 3 for Eν ≥ 1.8 MeV. Figure 5 shows the combined AGM2015 crust + mantle flux.

Table 3 Contribution of geoneutrino luminosities L in AGM2015 above the IBD threshold Eν  ≥ 1.8 MeV for 238U, 232Th and 40K emitted by the Earth.
Figure 5
figure 5

AGM2015 geoneutrino flux due to 238U and 232Th decay in the Earth’s crust and mantle.

Flux units are at the Earth’s surface. Map includes of all energies. Figure created with MATLAB45.


The underlying interior structure and composition of the Earth is, in some regards, still poorly understood. The concentration and distribution of radioisotopes, whose decay chains produce geoneutrino flux, dominate the uncertainties. Therefore modeling of the distribution, energy spectra and total flux of geoneutrinos remains a challenging task on its own. A full description of the uncertainty in each element of the AGM flux maps is not available at this time, however, we have defined the uncertainties in the specific building blocks of the AGM in Tables 1 and 4 as well as the systematic uncertainties present in the various geoneutrino luminosity categories in Tables 2 and 3. The uncertainties in Tables 1 and 4 in particular can be used to create Monte Carlo instances of the AGM flux maps, which could be used to evaluate the variances in each element of the AGM flux map, as well as co-variances between map elements. Such a full-scale Monte Carlo covariance matrix is impractical, however, due to the large number of map elements, ~300 Million, which would end up producing a 300 Million × 300 Million full-size covariance matrix.

Table 4 AGM2015 reactor- parameters and oscillation parameters.

In most parts of the AGM2015 map uncertainties are strongly correlated over space and energy. This is due to the fact that the greatest uncertainty lies in ingredients that affect all map elements nearly equally, such as elemental abundances in the Earth’s crust and mantle. Other ingredients which might introduce more independent uncertainty, such as the volume or density of specific crust tiles, are much more likely to introduce minimal correlations, or only slight regional correlations. Since reactor- flux is generally better predicted than geo- flux and since near a core the reactor- flux will dominate the overall flux, we would expect smaller fractional uncertainties near reactors than in other regions of the world.

We attempt to apply systematic uncertainties to AGM2015 where appropriate and to derive these uncertainties from previous work in the field where possible rather than reinvent the wheel. For our uncertainty models we turn to Huang et al.36 and Dye31. Doing so allows us to apply systematic uncertainties to the various source categories in Tables 2 and 3 while avoiding the significant computational burden of a full Monte Carlo analysis, as well as the questions that would arise afterward of how to describe the various levels of regional correlation in flux uncertainty across space and energy.


Electron antineutrino measurements have allowed for the direct assessment of 7–29 TW31 power from U and Th along with constraining a geo-reactor <3.7 TW at the 95% confidence level12. Such measurements promise the fine-tuning of BSE abundances and the distribution of heat-producing elements within the crust and mantle. Several such models of the Earth’s antineutrino flux32,40,41 existed before the observation of geoneutrinos; with several recent models being presented with the inclusion of geoneutrinos36,42,43. All of the aforementioned models incorporate several geophysical models based on the crust and mantle from traditional geophysical measurements (seismology, chondritic meteorites, etc.) This effort, AGM2015, aims to consolidate all these models into a user-friendly interactive map, freely available to the general public and easily accessible to anyone with a simple web browser at

Future work includes completing a more detailed uncertainty study using Monte Carlo methods. Such a study requires an accurate understanding of the uncertainty in each of the AGM elements listed in Tables 1 and 4, however, as well as the correlations that govern their interactions. Future geo- measurements, updated flavor oscillation parameters, advances in crust/mantle models and the ongoing construction and decommissioning of nuclear reactors around the world necessitates a dynamic AGM map capable of changing with the times. For this reason we envision the release of periodic updates to the original AGM2015, which will be labeled accordingly by the year of their release (i.e. “AGM2020”).


AGM2015 uses CRUST1.035 to model the Earth’s crustal density and volume profile via eight stratified layers. Elemental abundances for U, Th and K and isotopic abundances for 238U, 232Th and 40K for each layer were defined by Huang et al.36. These values were coupled to well known isotope half-lives and multiplicities to create luminosities emanating from each crust tile. A similar approach was taken with the Earth’s mantle, with elemental abundances derived via estimates of geo- flux at KamLAND and Borexino44 and density profiles supplied via PREM39.

Man-made reactors were modeled via the IAEA PRIS24 database, with reactor- luminosities found to scale as 1.83 × 1020. Reactor- spectra were modeled as exponential falloffs from empirical data19, while 238U, 232Th and 40K spectra were modeled based on the work of Sanshiro Enomoto37.

Luminosities from each point-source were converted to fluxes at each map location via the Pee survival probability shown in Equation (4) and a full understanding of the source spectra of each point-source enabled a complete reconstruction of the observed energy spectra at each map location. “Smart” integration was applied where necessary to more accurately portray crust and mantle tiles as volume-sources rather than point-sources. All modeling and visualization was done with MATLAB45. Google Maps and Google Earth multi-resolution raster pyramids created with MapTiler46. All online content available at

Additional Information

How to cite this article: Usman, S.M. et al. AGM2015: Antineutrino Global Map 2015. Sci. Rep. 5, 13945; doi: 10.1038/srep13945 (2015).