Corresponding author: R. S. Miller, Department of Physics, University of Alabama in Huntsville, Optics Bldg. 300H, Huntsville, AL 35899, USA. (email@example.com)
 The Lunar Prospector (LP) and Lunar Reconnaissance Orbiter (LRO) orbital neutron spectroscopy data sets represent a unique comprehensive multimission lunar resource. A rigorous statistical approach has been used to (re)analyze neutron data from both missions to provide new details regarding the relationships between the individual detector data sets, as well as a new evaluation of enhanced hydrogen deposits at the lunar poles. Using the multimission epithermal neutron data set, we find water ice distributed broadly across the poles, but showing evidence for a dependence on topographical features. A footprint averaged water equivalent hydrogen (WEH) abundance of 106 ± 11 ppm at each pole, with maxima of 131 and 112 ppm at the north and south poles, respectively, is derived from the epithermal neutron data. We also report the first definitive detection of a fast neutron signature consistent with an enhanced hydrogen hypothesis. These data suggest a highly localized distribution, consistent with Shackleton Crater, corresponding to a footprint averaged WEH abundance of 194 ± 11. If confined to this crater, this abundance yields a localized deposit of ∼0.7% WEH. Details of the analysis approach are presented along with spatial distribution maps showing the intriguing enhanced hydrogen deposits at the lunar poles.
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 Since the dawn of the space age two missions have provided global neutron measurements of the lunar surface. NASA's Lunar Prospector (LP) and Lunar Reconnaissance Orbiter (LRO) have contributed important information about elemental abundances on the Moon using spectrometers capable of detecting neutrons across a broad range of energies. Of particular interest have been investigations focusing on the lunar poles, where the combination of topographic features and limited solar illumination conspire to form cold traps for volatile compounds such as water [Colaprete et al., 2010; Paige et al., 2010].
 The two missions were motivated by different, yet complimentary, goals. Launched in 1998, LP was conceived to address lingering top-level questions in the post-Apollo era. Of its five instruments, the neutron and gamma ray spectrometers (LP-NS and LP-GRS, respectively) are of interest here. They were designed to prospect the lunar regolith for elements that could help resolve open issues regarding lunar formation and evolution, as well investigate the presence of water in permanently shadowed craters at both poles [Feldman et al., 1998]. Both spectrometers were wide field-of-view instruments relying on orbital geometry to define the spatial footprint for lunar surface mapping. Using the LP-NS, enhanced hydrogen deposits were detected with inferred concentrations of ∼1.5% water equivalent hydrogen (WEH) within permanently shadowed craters [Feldman et al., 2000].
 Building on the success of LP and launched about a decade later, LRO was envisioned as a new beginning to an extended human presence in the solar system, starting with a return to the Moon. Instruments were therefore selected to support near-term human exploration including the selection of landing sites and resource identification. High spatial resolution mapping of polar hydrogen concentrations was a fundamental goal, requiring an instrument with surface localization capabilities better than the LP spectrometers. The Lunar Exploration Neutron Detector (LEND) was designed to meet this requirement using a suite of collimated and uncollimated detectors [Mitrofanov et al., 2010a].
 Both missions have produced valuable resources for lunar science and exploration. The orbital neutron spectroscopy results, however, have not been without controversy. Since before its launch, some in the lunar science community expressed concerns with the design and projected performance of the LEND instrument and in particular the effectiveness of the collimated subsystem [Lawrence et al., 2010]. The debate has continued since launch [Lawrence et al., 2011b; Eke et al., 2012; Mitrofanov et al., 2011], with questions raised as to the validity of the LEND data set, the analysis procedures used, and ultimately its interpretation. Resolving these issues is critical since the results will inform future lunar exploration endeavors.
 In principle, the LP and LRO neutron data sets are complimentary and together represent a unique comprehensive resource. Both data sets include a subset of uncollimated intermediate energy neutrons, thereby enabling an important comparison. Incorporating the fast (via LP-GRS) and collimated (via LEND) neutrons should enhance the science return since each contributes a new aspect to the investigations. This comprehensive lunar neutron data set can, and should, be used to address the documented debate in an effort to resolve the discrepancies and ultimately to focus on the lunar science challenge to provide new insights and a more complete picture of the Moon.
 With these motivations in mind the goals of this paper are threefold: (1) to evaluate the relationships among the neutron data sets and perform the necessary LP-LRO cross validation, (2) to utilize the available neutron data sets to qualitatively investigate the nature of the LEND collimated data and its usefulness to lunar science, and (3) to extract new polar hydrogen results by applying new statistical techniques to leverage the valuable the multimission neutron archive.
2. Orbital Neutron Spectroscopy
 The leakage flux of secondary neutrons has proven to be an important remote sensing tool not only at the Moon, but also for other airless solar system bodies [Prettyman, 2006]. Orbital neutron spectroscopy is commonly divided into three distinct energy regimes, thermal (low energy), epithermal (intermediate energy), and fast (high energy), each theoretically providing complimentary elemental abundance and compositional morphology information. The process starts with fast neutrons created by cosmic ray interactions in the lunar regolith. Through moderation and/or capture processes this fast neutron flux is modified, ultimately imprinting details of the intervening material on the energy distribution and flux of the escaping neutrons.
 Neutrons will rapidly lose energy in the presence of hydrogen due to elastic n-p interactions. This shifts some fast neutrons into the epithermal regime, and ultimately into thermal equilibrium with the regolith if the energy loss processes continue. As shown inFigure 1, the epithermal regime is the most sensitive to the abundance of hydrogen due to the efficiency of the energy loss by elastic scattering with hydrogen and absence of less efficient, competing processes such as inelastic scattering. The relative intensity between neutron energy regimes may give important stratigraphic information [Feldman et al., 1998, 2001; Prettyman, 2006; Feldman et al., 2011]. Observed neutron deficits, defined as reduced neutron count rates relative to a hydrogen-free region, are therefore indicative of energy loss and in turn suggestive of an enhanced hydrogen abundance. It is important to note that moderated (thermal) neutrons may also be captured by elements having large neutron capture cross sections, making them useful for nonhydrogen prospecting as well.
 The comprehensive LP-LRO lunar neutron data set spans all three energy regimes. Specifically, both the LP and LRO spectrometers were sensitive to neutrons within all three energy classifications. However, due to its low counting rate and surrounding mass the LRO fast neutron data set will not be considered in this work. Details of the instruments and the individual data sets are briefly reviewed below.
2.1. Lunar Prospector Spectrometers
 Lunar Prospector orbited the Moon for approximately 1.5 years beginning in January 1998. Initially placed into a 100 km circular, polar orbit, it was lowered to 30 km for the final 6 months of the mission. The LP-NS included two identical3He proportional counters, one covered with Sn and the other with Cd [Feldman et al., 1999]. Although both detectors were sensitive to epithermal neutrons (0.4–100 eV), only the Sn-covered detector was sensitive to (thermal) neutrons with energies below the Cd cutoff at 0.4 eV.
 Fast neutrons (0.6–9 MeV) were detected using the scintillator-based LP-GRS [Feldman et al., 1999]. This instrument incorporated a borated plastic scintillator as a charged-particle veto surrounding a BGO crystal forγray detection. Fast neutrons were identified using a double-pulse signature: neutron moderation and signal generation in the plastic scintillator, followed by neutron capture [Genetay et al., 2003].
 To maximize the effectiveness of neutron observations it is important to be close to the emitting source. Therefore only data acquired during the 220 days of low-altitude (30 km) operations are used for the analysis presented here. This includes epithermal (LP-epi) and fast neutrons (LP-fast) accumulated in 8 and 32 s intervals, corresponding to 1.8 × 106 and 4.4 × 105 sample intervals, respectively. All data were obtained from the Planetary Data System (PDS) public archive; data reduction details for these data sets can be found elsewhere [Maurice et al., 2004; Lawrence et al., 2006].
 Thermal neutrons are not used in this work since they are not a uniquely sensitive probe of hydrogen deposits. It should also be noted that the LP spectrometer team used a modified neutron data set for their analyses of the lunar poles [Feldman et al., 1998; Maurice et al., 2004]. This hybrid epithermal-thermal data product was produced in an effort to maximize sensitivity to hydrogen relative to other elements. A second hybrid data product, consisting of all moderated neutrons (<0.5 MeV), was unique since it included neutrons from the previously unexplored high-energy epithermal (HEE) region between 100 eV and 500 keV [Genetay et al., 2003]. However, because a principle goal of this work is a direct comparison with LEND, no hybrid data products are used here. Other data corrections are described by Maurice et al. .
2.2. Lunar Exploration Neutron Detector
 The Lunar Exploration Neutron Detector (LEND) is unique since it incorporates a combination of uncollimated and collimated 3He sensors [Mitrofanov et al., 2008, 2010a]. One of the four uncollimated sensors (SETN) is configured for epithermal neutron detection (>0.4 eV), as are the four collimated sensors (CSETN). The latter are installed within a collimating module intended to provide improved spatial resolution relative to uncollimated sensors. This collimator has external layers of polyethylene and internal layers of 10B designed to moderate and absorb neutrons incident from beyond the collimator's 5.6° field of view (half-opening angle).
 The present analysis uses the LEND averaged science data (ALD), consisting of spatially averaged data acquired from September 2009 through September 2010 at a nominal mapping altitude of 50 km above the lunar surface. Averaged LEND data includes count rates for both uncollimated and collimated detectors, exposure times, and auxiliary housekeeping data. Archived data available at the PDS have been divided into north and south polar regions (|lat| ≥ 80°) and an equatorial region having resolutions of 0.5° × 0.5° (14,400 grid cells, each pole) and 1° × 1° (57,600 grid cells), respectively.
2.3. Rebinned Data
 To facilitate analysis all data sets were (re)binned using the Hierarchical Equal Area Isolatitude Pixelization (HEALPix) paradigm [Gorski et al., 2005]. This approach is advantageous for studying spatial distributions since it enables equal area binning of a sphere. Spatial resolution is defined by a grid resolution parameter Nside that ultimately dictates the number of pixels as Npix = 12Nside2, with Nside valid on a dyadic scale (i.e., Nside = 2k, k ≥ 0). Because they are equal area, HEALPix pixels have solid angles Ωpix = 4π/Npix, and an angular resolution θpix = .
 The choice of resolution parameter is driven, in part, by detector spatial resolution. Uncollimated detectors viewing a spherical body have a field-of-view half-opening angle given byθFoV = sin−1(Rm/Rm + h), where h is the spacecraft orbit altitude and Rm is the lunar radius, while an approximate estimate for the radius of the spatial footprint on the lunar surface is simply r = h tan(θFoV). Table 1 gives the fundamental fields of view for each neutron data set. It should be noted that oversampling can reduce the achievable spatial resolution [e.g., Lawrence et al., 2003]. Therefore, utilizing pixels somewhat smaller than the fundamental spatial resolution is desired as long as the resulting counting statistics uncertainties do not dominate over any spatial variations.
Table 1. Orbital and Spatial Resolution Parametersa
Surface Footprint Radius (km)
Geometric parameters were used to define fundamental spatial resolution performance of neutron data sets. Note that the CSETN resolution assumes a 100% efficient, fully collimated instrument with a field of view as defined in the table.
 Under the assumption that the CSETN is fully collimated it should have the best achievable spatial resolution of the four instruments. In principle, this would require Nside = 128 (k = 7, Npix = 196608, θpix = 0.46°) to provide a resolution just larger than that of the CSETN. However, because the spatially averaged LEND ALD data set is used here, Nside = 64 (k = 6, Npix = 49152, θpix = 0.93°) is appropriate and selected a priori to meet the spatial resolution requirements. All LP and LRO data sets were (re)binned using this resolution parameter.
3. Neutron Count Rate Distributions
 Global count rate distributions for the rebinned LP and LEND data sets are shown in Figure 2. Spatial variations within the maps are indicative of elemental abundance changes [Feldman et al., 1998, 2001; Prettyman, 2006] with many features, such as those associated with the nearside maria, common to all data sets. Key differences, however, do exist. For example, the LP-epi count rate shows a deficit within the maria, yet the LP-fast rate is enhanced in the same region. A visual inspection of the LEND maps show a similar deficit for the SETN data, yet the CSETN map suggests an enhancement similar to that seen in the LP-fast map. This latter observation is curious since the CSETN data is supposed to be a collimated subset of the SETN data.
 In an effort to quantify the relationships among the data sets the 2-D global maps have been reduced to the 1-D latitude profiles shown inFigure 3. These profiles have been integrated over longitude and for clarity lunar latitude has been converted to a variable starting from equator (0°), passing through the north and south poles (90° and 270°, respectively), and returning to the equator. To more clearly illustrate variations within the individual data sets, many corresponding to specific lunar features, latitude profiles for specific 1°-wide longitude slices are shown inFigure 4.
 As expected, a number of features are common among the data sets. For example, the two uncollimated epithermal data sets (LP-epi and SETN) have similar profiles throughout the equatorial and polar regions. In contrast, the LP-fast profile is dominated by the nearside maria apparent in the global maps, and shows a dichotomy of structure at the north and south polar regions. A quantitative analysis provides additional insights.
3.1. Correlation Analysis
 The Pearson product moment correlation coefficient (1 ≤ r≤ 1) is used to quantify the strength of the correlations between data sets, with the limits corresponding to perfect anticorrelation and correlation, respectively. In this application, the correlation coefficient measures similarities in relative amplitude (or shape) only, and is not used to evaluate the physics implications of the absolute neutron rates. Coefficients obtained using the longitude-integrated latitude profiles (e.g.,Figure 3) are tabulated in Table 2. Also given are the corresponding significances for the observed correlations, measured as a z score relative to the null hypothesis r = 0.
Table 2. Pearson Product-Moment Correlation (r) for Longitude-Integrated Latitude Profilesa
The significance (given as a z factor) for each correlation coefficient is shown in parentheses.
 Two highly significant correlations stand out. The first, between the LP-epi and SETN profiles, is expected since both data sets presumably sample the same lunar neutron component. Of particular note, however, is the high degree of correlation between the LP-fast and CSETN profiles. Naively, this is an unexpected result since the CSETN was intended to provide a collimated subset of epithermal neutrons, and hence should be highly correlated with the SETN and LP-epi profiles, which it is not. This strong correlation suggests a CSETN data set dominated by a nonepithermal component, a result supported visually by the global maps.
 A benchmark for an epithermal-fast correlation is provided by the LP data sets, and is a metric for qualitative investigation of the CSETN data. This benchmark is an anticorrelation (as expected;Table 2), driven in part by the dramatic differences in the equatorial count rates that support the presence of elements having large neutron capture cross sections [Lawrence et al., 2006]. Using a linear combination of the LP data sets, the relative weights are adjusted until the LP-epi/LP-fast correlation (r= −0.6) is degraded and consistent with the LP-epi/CSETN correlation at the 90% C.L., i.e., in the range −0.24 ≤r ≤ −0.07. This qualitative approach suggests that the CSETN is not a pure epithermal sample, and is instead consistent with a “model” having a fast epithermal admixture ratio of 1:0.77 ± 0.11. Although an independent sample of HEE neutrons was not included in this analysis they are also a likely, and perhaps dominant, component of the CSETN data set [Lawrence et al., 2011b; Eke et al., 2012].
 Similar anticorrelations, albeit at lower significances, are observed between the LP-fast/SETN and the LP-epi/CSETN profiles. Because of the SETN's similarity to the LP-epi the former anticorrelation is expected, mimicking the one observed between the LP data sets. The latter is consistent with the high degree of correlation between the CSETN and LP-fast profiles.
 Global count rate distributions, latitude profiles, and correlation analyses are consistent with the hypothesis that the CSETN is not a collimated epithermal data set as originally intended. Rather, it has a significant nonepithermal (HEE and fast) component and may even be dominated by it. The efficiency for direct HEE or fast neutron counting using 3He counters is low, requiring another model for their detection by LEND. Presumably these neutrons are incident from beyond the instrument's field of view, are moderated as they pass through the collimator, and subsequently detected as epithermal neutrons. Although only a detailed instrument simulation and/or laboratory calibration effort would be definitive, this model is consistent with the results outlined above.
 Comprehensive energy- and incident angle–dependent efficiencies would likely enable a deconvolution of the various neutron components, and possibly the recovery of a collimated epithermal component. In the absence of this critical performance information it is necessary to treat the CSETN data set as is, since any effort to separate the collimated and noncollimated contributions would impose unknown systematic effects and ultimately prove counterproductive. One is, therefore, forced to give up the notion of a collimated data set and its presumed benefits to spatial resolution, and utilize the data set as an uncollimated detector sensitive to a combination of fast and epithermal neutrons. It is important to note, however, that this does not imply that the CSETN data set is unusable. On the contrary, additional efforts to characterize its performance and response will ultimately benefit neutron spectroscopy and lunar science investigations.
 As discussed above, the choice of pixel size was driven by the assumption of an effective collimated data set. Although this assumption is not supported by the correlation analysis, the choice of pixel size will be retained for the analysis that follows. This represents a tradeoff between maximizing statistical significance (larger pixels→improved statistics) and maximizing spatial resolution (smaller pixels→improved surface mapping). The impact of this choice for polar analyses is discussed in greater detail below.
4. Polar Analysis
 Two fundamental features are apparent in the epithermal neutron (LP-epi and SETN) latitude profiles: significant variation at equatorial latitudes and a clear reduction of the neutron count rate at the poles, with both mimicking similar features first identified by Lunar Prospector [Feldman et al., 1998, 2001]. Of particular interest here are the polar deficits. Previous analyses have provided either a general description, such as the integrated magnitude of the deficits in the polar regions that can mask topographic-dependent nonuniformities [e.g.,Feldman et al., 2001], or utilized a model-dependent spatial deconvolution approach [Elphic et al., 2007; Teodoro et al., 2010]. A rigorous, independent, statistical methodology appropriate for hypothesis testing [Miller, 2012] is complimentary and utilized here to infer the spatial distribution of hydrogen at the poles and its significance.
4.1. Likelihood Ratio Method
 Proper determination of statistical significance and confidence intervals are often overlooked experimental challenges. In fact, approximate methods are commonly used for simplicity or to reduce computation requirements. However, the importance of using an accurate analysis methodology must take precedence over ease of use, particularly in low signal-to-noise experiments. Details of the statistical analysis framework employed here can be found elsewhere [Miller, 2012] but are briefly reviewed below.
 Statistical techniques can incorporate the fundamental discrete statistical distributions governing particle detection experiments, including underlying uncertainties. This is critical for an accurate determination of significance. The statistical descriptions relevant to this work are based on particle counts, not rates, and therefore require the use of exposure distributions as well as the neutron rates presented above. Here exposure is defined as the amount of time the spacecraft subsatellite point is within a given pixel for a constant measurement geometry. Representative exposure maps of the polar regions showing the principle benefit of a polar orbit—enhanced sampling at the poles—are presented in Figure 5; similar exposures are obtained for all the data sets used here.
 Let Ho represent an hypothesis based on some a priori knowledge of a physical model containing p free parameters. Furthermore, let H represent another, more complex, hypothesis that contains q + p parameters. The likelihood ratio method (LRM) is useful when comparing the two hypotheses and determining the level of confidence that can be placed on hypothesis H compared to the null hypothesis Ho.
 Given a quantity k, the likelihood that it was drawn from each of these two parent distributions is denoted L(k|H) and L(k|Ho), respectively. To determine the degree with which the data may support hypothesis H over Ho a likelihood ratio is computed,
and since in general H incorporates hypothesis Ho this ratio satisfies R ≥ 1. In a classical interpretation the statistic λ = 2 ln R follows a χ2 distribution with q degrees of freedom if the null hypothesis is true, with Ho rejected if λ exceeds some predetermined critical value λc; the confidence level is P(χq2 < λc). Techniques such as this have been successfully employed in a variety of scientific endeavors, including X-ray andγ ray astrophysics [Cash, 1979; deBoer et al., 1992].
 In the scenario considered here the two hypotheses correspond to dry (hydrogen-free ) regolith (Ho) and regolith with a nonzero hydrogen abundance that ultimately produce a neutron deficit (H). The likelihoods for H and Ho are simply the Poisson distributions fP(k; μs) and fP(k; μb), respectively. Here k is the number of counts detected within a map pixel, μbthe expected number of counts based on a hydrogen-free hypothesis, andμs = k. Detectors requiring background subtraction (e.g., imperfect collimation) require the Skellam, rather than the Poisson distribution [Miller, 2012].
 The hydrogen-free count estimate can, in principle, be obtained either from models or empirically from actual data. The latter approach is used here. Since the region of interest is poleward of 80°, the average count rate is extracted from a 10° latitude band region just outside this region under the assumption that it is outside the (potentially) hydrogen-enhanced polar regions and excludes most of the equatorial latitudes having significant count rate variations. It should be noted that the results presented below are robust to this choice and do not change markedly if a latitude band between, say, 60°–70° is chosen instead. The resulting “background,” or expected, count estimate (μb) was then obtained for each pixel by multiplying this average rate by the relevant pixel exposure. This procedure was repeated for each of the four independent data sets used in this work.
 The difference between the two hypotheses is simply a neutron suppression factor, i.e., δ = (μs − μb)/μb. Therefore, with one degree of freedom (q = 1) the critical value of λ corresponding to a Gaussian equivalent of 5σ (chance probability of 5.7 × 10−7) is λc = 25, and values exceeding this threshold imply that the null hypothesis can be effectively rejected. Marginal significance, corresponding to a Gaussian equivalent of 3σ, is obtained using λc = 9. It is important to note that by itself the λ-statistic cannot distinguish between an enhancement (δ > 1) and a deficit (δ < 1), and requires additional information (e.g., μs and μb) to do so.
4.2. Polar Likelihood Maps
 Spatial distributions of the λ statistic are shown in Figures 6 and 7for the north and south polar regions, respectively. As expected, the two epithermal data sets (LP-epi and SETN) show highly significant deficits centered near the poles, with asymmetries that may be indicative of morphology effects. A 2-D spatial correlation, using the Pearson product moment statistic described insection 3.1, quantifies the similarities and supports the interpretation that the two epithermal data sets have mapped map the same selenographic distribution (Tables 3 and 4). Differences in significance are accounted for by a tradeoff between the higher count rate of the LP-NS (due to lower altitude) and the additional exposure time of LEND.
Table 3. Pearson Product-Moment Correlation (r) for the North Polar λ Statistica
The significance (given as a z factor) for the each correlation coefficient is shown in parentheses.
Table 4. Pearson Product-Moment Correlation (r) for the South Polar λ Statistica
The significance (given as a z factor) for the each correlation coefficient is shown in parentheses.
 The LP-fast data set shows a significant localized deficit slightly offset from the south pole, the first fast neutron signature detected at the lunar poles. Other associated features include a nearly symmetric circumpolar deficit just below the required significance threshold, and strong evidence supporting a fast neutron enhancement consistent with the South Pole-Aitken (SPA) basin. The spatial correlation analysis (Table 4) suggests the fast and epithermal neutron distributions are different, due in part to the SPA enhancement and the fast neutron deficit being more tightly concentrated near the pole.
 Neither the LP-fast (north pole) nor CSETN (north or south pole) maps have features exceeding the required threshold, although it is possible that the choice of pixel size led to a reduction in significance. As discussed previously, this choice is a compromise between spatial resolution and statistical significance. To investigate if this has had a negative impact on the analysis we note that the significance of an actual resolved “source” will evolve with pixel size. Specifically, it will increase as pixel size is enlarged, reach a maximum when pixel size and the effective detector footprint (point spread function) are well matched, finally decrease when the pixels become larger than the physical extent of the source. This trend occurs in a predictable way for a known (or assumed) point spread function.Figure 8shows the evolution of the most significant pixel for the LP-fast and CSETN maps as a function of pixel size. Also shown is the relative change expected for a Gaussian point spread function. Only the south pole LP-fast data set shows the required evolutionary trend while also exceeding the detection threshold at a particular scale. Therefore, we can conclude that a fast neutron signature at the south pole is real, while other features remain subthreshold.
 Although it is tempting, one must be careful not to overinterpret the low-significance features within the LP-fast and CSETN maps. Based on significance and the pixel size–evolution trends only the south pole fast neutron signature can be considered a positive detection given the significance threshold chosen a priori (λ ≥ 25). It is, however, intriguing to note the modest correlation between the CSETN spatial distribution and the epithermal maps, suggesting that this data set may yet provide statistically significant detections given additional exposure time, a prediction anticipated elsewhere [Miller, 2012]. This is certainly true at the south pole where the CSETN map mimics key features of the epithermal maps.
 Although a detailed analysis of the λ statistic (significance) maps and their relationship to lunar topography is forthcoming (R. S. Miller et al., manuscript in preparation, 2012), a cursory analysis is instructive. In addition to being a measure of significance, the λ statistic is also a proxy for the actual abundance of polar hydrogen. The LRM approach characterizes the statistical significance of “source” pixel counts relative to an expected background, ultimately giving a direct relationship between the neutron suppression factor and the λ statistic. An example of the δ − λ relationship is shown in Figure 9, reinforcing the notion that increasing statistical significance (larger λ) corresponds to a larger deficits (more negative δ). The dependence of the neutron suppression factor on hydrogen (water) content of lunar regolith is also shown in Figure 9 for both epithermal and fast neutrons.
 Using these relationships the significance maps have been converted to water content distributions. As originally proposed here, the LP and LRO neutron data sets represent a comprehensive lunar resource with maximum science return obtained by utilizing data from both missions. Comprehensive maps showing the epithermal-derived distribution of water ice at the lunar poles are shown inFigure 10. The multimission epithermal data set combined observed counts from the LP-epi and SETN data sets, preserving relative rates and exposures and incorporating no scaling. Specifically, total counts for each pixel were obtained by adding the number of counts, i.e., the product of count rate and exposure, from each mission data set. Only pixels meeting or exceeding the detection threshold chosen a priori have been used (λ ≥ 25).
 At the north pole the epithermal-derived water distributions appear to reach the edges of the large impact craters (e.g., Hermite, Rozhdestvenskiy, Plaskett, Byrd) but do not extend deep into them. Similar trends are apparent in the south pole maps, with the addition of a clear association with the Cabeus region. A footprint averaged WEH abundance enhancement of 0.05 ± 0.01% (56 ± 11 ppm) exists poleward of 80° at each pole, with maxima of 0.073% (81 ppm) and 0.065% (72 ppm) at the north and south poles, respectively. Since these are enhancements above nonpolar levels (∼50 ppm [Feldman et al., 2000, and references therein]) the polar footprint averaged WEH abundances are 106 ± 11 ppm, with maxima of 131 ppm (north) and 112 ppm (south). These epithermal-derived abundances and spatial distributions are consistent with other estimates [e.g.,Lawrence et al., 2006; Teodoro et al., 2010]. A detailed analysis of the hydrogen abundance maps, their relationship to lunar topography, and a comparison with previous estimates including those of LEND [Mitrofanov et al., 2010b, 2008] is forthcoming (Miller et al., manuscript in preparation, 2012).
 In contrast to the epithermal results, the fast derived water distribution is limited to the south pole and highly localized. In fact, at the canonical map resolution level of 28 km (k = 6, θpix = 0.93°) the significance is confined to a single pixel consistent with the location of Shackleton Crater (diameter of 21 km). Unfortunately, a single pixel does not facilitate a meaningful statistical analysis. Therefore, the detection threshold was reduced to marginal significance (λ ≥ 9), increasing the number of “source” pixels while maintaining the fundamental source significance. The resulting fast derived water distribution map has a footprint averaged WEH enhancement of 0.13 ± 0.01%, corresponding to a final WEH abundance of 194 ± 11 ppm (Figure 11).
 If this fast neutron-derived hydrogen enhancement is indeed confined to Shackleton crater the measured rate at orbit is different than that on the surface due to geometric instrument response factors. A forward model approach can be used to estimate the rate on the lunar surface [Lawrence et al., 2006, and references therein]. Specifically, the relationship is linear, Rsurf = aRorbit + b, where Rorbitis the ratio of the observed (orbital) neutron count rate to a hydrogen-free region,Rsurf is the same ratio on the lunar surface, and a (=4.775) and b (=−3.775) are fitted parameters obtained from the forward model analysis. For Shackleton Crater we observe a 1.5% reduction in rate relative to the null hypothesis latitude band rate (13.4 counts/s) measured at orbit. This gives Rsurf = 0.928, corresponding to a 7.2% rate reduction on the lunar surface, and yields a WEH enhancement of ∼0.7% within the crater (e.g., Figure 9, right).
 The detection of the fast neutron signature, and its colocation with Shackleton crater, is interesting and requires additional investigation. Why is this detection special? Are there other effects that could mimic a similar statistically significant result? One possibility is a local change in regolith average atomic mass, 〈A〉. Although this effect does indeed lead to significant enhancements of fast neutrons in some regions, e.g., South Pole-Aitken basin, it is important to note that the feature consistent with Shackleton is a neutron deficit rather than an enhancement, and hence is suggestive of a hydrogen enhancement. Additional analyses that leverage the elemental concentrations derived from thermal neutron and orbitalγ ray measurements, however, will help clarify this aspect of the signature. On the other hand, if indicative of an actual localized hydrogen deposit, is this detection only the result of the good statistics near the pole (e.g., observational exposure), and if so what limits are obtained from other polar regions? Are there layering issues; that is, is there a possibility that hydrogen exists closer to surface here than other regions? What do the combined fast neutron and epithermal neutron results say about the polar regions? These questions are the focus of ongoing analysis efforts.
 Obviously, a collimated neutron data set would be beneficial to the polar hydrogen deposit interpretation. No effort to utilize the CSETN data set to derive water content is incorporated here since no detections met the required detection threshold chosen a priori and because of the interpretation challenge due to the multiple neutron source contributions described previously.
 Multimission orbital neutron spectroscopy observations of the Moon have been used to evaluate the relationships between the LP and LRO neutron data sets, and derive hydrogen (water ice) abundance maps of the lunar poles. Treating these data as a comprehensive resource a number of useful results have been obtained. First, the uncollimated epithermal data sets from each mission are found to be well correlated, both in significance and spatial distribution, supporting a conclusion that they sample the same neutron source(s). In addition, using a robust statistical analysis methodology the significance and spatial distribution of the polar neutron deficits have been evaluated, including the first detection of a fast neutron signature. In contrast to the broadly distributed epithermal-derived polar hydrogen deposits, this fast neutron detection is highly localized and consistent with the location of Shackleton crater. Finally, a detailed evaluation of global maps and relationships between individual data sets suggests that data from the collimated instrument aboard LRO (LEND) is consistent with an admixture of both fast and epithermal neutrons, degrading the collimated aspect of this instrument and making science interpretation difficult. Although no statistically significant polar detections have been identified using this data, additional exposure time is likely to change this result.
 This work was supported by the NASA Lunar Science Institute grant NNA09DB31A.