REY Patterns and Their Natural Anomalies in Waters and Brines: The Correlation of Gd and Y Anomalies

Rare earths and yttrium (REY) distribution patterns of the hydrosphere reveal systematic correlations of Gd and Y anomalies besides the non-correlated redox-dependent Ce and Eu anomalies. Eu anomalies are inherited by dissolution of feldspars in igneous rocks, whereas Ce, Gd and Y anomalies develop in aqueous systems in contact with minerals and amorphous matter. Natural, positive Gd and Y anomalies in REY patterns characterize high-salinity fluids from the Dead Sea, Israel/Jordan, the Great Salt Lake, USA, the Aral Sea, Kazakhstan/Uzbekistan, groundand surface water worldwide. Extreme Gd anomalies mostly originate from anthropogenic sources. The correlation of Gd and Y anomalies at low temperature in water bodies differ from geothermal ones. In nature, dynamic systems prevail in which either solids settle in water columns or water moves through permeable sediments or sedimentary rocks. In both cases, the anomalies in water develop due to repeated equilibration with solid matter. Thus, these anomalies provide information about the hydrological history of seawater, fresh groundwater and continental brines. When migrating, the interaction of aqueous phases with mineral surfaces leads to increasing anomalies because the more hydrophillic Gd and Y preferentially remain in the aqueous phase compared to their nearest neighbors. The correlation coefficients between Gd and Y anomalies in groundwater is 0.5–0.9. In lakes and oceans, it is about 0.1–0.8, under anomalous conditions it can increase to 1.


Introduction
The fourteen stable rare earth elements, REE, are unique because of the coherence of their chemical properties. Although Y is not a member of the REE suite, it behaves similarly to Ho in minerals crystallizing from siliceous melts due to the same ionic charge and nearly identical crystallographic ionic radii [1,2]. REE and Y are henceforth combined to REY. Under low-temperature conditions, the lanthanide contraction is expected to generate a continuous change from La(III) to Lu(III). Ce(IV) and Eu(II) behave differently according to oxydation and reduction, respectively. The fractionation of Gd(III) and Y(III) in phase separation processes such as either liquid-liquid extraction [3] or incorporation in mainly Ca minerals is caused by non-linear variation of physical parameters such as partial molal volumes [4] and formation constants of dissolved species. Hydroxo- [5][6][7], bicarbonato and carbonato complexes [8][9][10][11] and phosphato complexes [12,13] show anomalous behavior of Gd and Y. Chemical complexations of REY with chloride [14], fluoride [15,16] and sulfate [17] do not show deviations of formation constants of Gd and Y with respect to their nearest neighbors. In Figure 1a  Positive La, Gd, Lu and Y anomalies characterize modern seawater [18][19][20][21][22][23][24]. REE patterns of marine carbonates and phosphorites resemble those of seawater showing negative Ce and Eu and significantly positive Gd and Y anomalies [22,25]. The behavior of Gd is consistent with reduced adsorption onto particles and colloids in seawater compared to its nearest neighbors [26][27][28]. Chemical complexation with carbonate species and hydroxyl ions is strongly pH dependent. Incorporation of REY in calcite [29][30][31][32] and scavenging by FeOOH [33][34][35] reveals that Gd and Y are less involved and thus relatively increase in solutions compared to their nearest neighbors. They are also less adsorbed onto clay minerals [36] and less incorporated in phosphates [37,38] and sulfates [39][40][41].
According to [2,19], the fractionation between Y and Ho in oceanic depth profiles from top to bottom is controlled by desorption from particles settling from the eutectic zone. The residence times of Y and Ho in seawater are 5100 and 2700 years [2]. Investigating the local structure of Y 3+ and Ho 3+ in calcite by EXAFS revealed that Y-O and Ho-O distances in calcite are shorter than in corresponding aqua-ions [43]. Y-Ho fractionation is seemingly caused by involvement of 4f orbital electrons in covalent bonding of Ho (and all the other REE) in minerals, a contribution that is missing for Y.
The aim of this contribution is to focus on two aspects: the type of REY patterns and the occurrence of unequivocally natural REY anomalies, in particular, the possible correlation of Gd and Y anomalies in low-to high-salinity and cold to thermal groundwaters or brines. The Ce and Eu anomalies are touched upon because they characterize the redox potentials of the systems [44] and the environmental temperature, respectively [45][46][47].
Understanding the behavior of the REE series as a whole and the anomalous behavior of individual REE and Y improves our knowledge on aqueous REY geochemistry and extends the application of anomalies as tools in studying chemical processes in hydrology. Since very stable organic Gd complexes are used as pseudo-natural tracer in hydrology [48][49][50][51][52], the precise environmental background of Gd has to be known. Furthermore, the REY patterns and their anomalies allow to depict the catchment lithology of groundwater and its possible interaction with sediments containing ferric oxihydroxides, FeOOH, and/or phosphates [53,54]. The influence of organic matter is not a subject of this contribution.

Quantification of Ce, Eu, Gd and Y Anomalies
Conventionally, anomalies in normalized REE distribution patterns are defined either by the ratio of both normalized measured and interpolated abundances between their nearest neighbors or as direct ratios of normalized neighbors. Here normalization by C1 chondrite [55] is applied. The Ce anomaly is derived by extrapolation of the Pr-Nd trend (Equation (1), [56,57]) considering La possibly being enhanced due to methanotrophy [58]. Log(Eu/Eu * ) value is defined by Equations (2) and (3), except in case of the presence of anomalous Gd. With Gd often at the bend of the disparate trends of light and heavy REE and Eu commonly behaving anomalously, it is suggested to extrapolate log Gd * n from the mostly linear trend of the logarithms of normalized Tb, Dy and Ho in REY patterns ( Figure 3). Log(Gd/Gd * ) is then defined as the difference of the logarithms of measured and normalized Gd and the extrapolated log Gd * n (Equations (4) and (5)). The anomalous Y is given as a ratio of normalized Y and Ho. The anomalies are defined as Ce/Ce * -1, Eu/Eu * -1, Gd/Gd * -1 and Y n /Ho n -1 yielding either negative or positive values. In this study, only publications covering the series of REE and Y are considered [59]. This excludes all hydrological studies that do not report Y. log(Ce/Ce * ) = log Ce n /(2 log Pr n − log Nd n ) (1) log Eu * n =(log Gd * n + log Sm n )/2 (2) log(Eu/Eu * ) = log Eu n − (log Gd * n + log Sm n )/2 log Gd * n + log Ho n = log Tb n + log Dy n (4) log(Gd/Gd * ) = log Gd n + log Ho n − (log Tb n + log Dy n ) Subscript "n" indicates normalization.

Seawater
Worldwide, surface seawaters show lower REY abundances than their oxic deep ones [60]. Because water masses move along with the ocean conveyor belt, the REY patterns in deep ocean waters are not the result of processes in their local top water. Surface and oxic bottom waters are characterized by highly negative Ce anomalies such as in the area of the East Pacific Rise (Figure 4a) [61], the Indonesian Sulu Sea [24], the Java Sea (unpublished), the Fiji, Caroline and Coral basins built by atolls in the south Pacific [62] (Figure 4b) or the Mediterranean Sea (Figure 4c) [63]. Here the Ce anomalies in surface waters decrease and could be even absent (Figure 4b,c). The anoxic deep Mediterranean brine at 3400 m from the Tyro Basin, which is not involved in yearly overturning of the local water column, shows the highest REY abundance with positive Ce anomaly (Figure 4c). North Pacific [24]; Java Sea (unpublished); Sulu Sea [24]; Gulf of Thailand [2]. (b) Oceanic basins build by atolls [62]. (c) Tyro sub-basin in the eastern Mediterranean Sea [23]. (d) Correlation of Gd and Y anomalies in seawater.
In surface and bottom waters REY patterns of oxic ocean waters show positive Gd and Y anomalies which plot on the same trend line with a slope of about 0.8 (Table 1) and X-axis intercept of about 0.5 ( Figure 4d). In marine basins built by atolls, the depth-dependent anomalies of bottom and surface water follow different trend lines with slopes of 0.072 and 0.18, respectively. Their intercepts on the Y-axis of bottom and surface water are about 0 and 0.05, respectively. The surface waters from the Gulf of Thailand [64] at three different times in the monsoon-dominated year plot along the same correlation line as those of the surface water of basins in the South Pacific. Table 1. Slopes in Gd vs. Y anomalies in natural waters. Slope equals the ratio of (Gd/Gd * -1)/(Y n /Ho n -1).

Lakes and Continental Seas
Lakes and continental seas are the ultimate sinks of surface run-off and groundwater flow from continents. Their REY abundance depends on the lithologies of their drainage basins. The surface waters of lakes and seas show either REY patterns without Ce anomalies (Dead Sea, Middle East [65]; Great Salt Lake, USA (unpublished), Lake Ontario, USA/CND [66] or with Ce anomalies (Lago di Garda, Italy (unpublished); Lake Tiberias, Israel [67]; Lake Erie, USA/CND [66]. The REY patterns of surface waters of the hypersaline Great Salt Lake, USA, and the saline Aral Sea, Kazakhstan/Uzbekistan, show increasing abundances from Tb to Lu similar to seawater but contrasting the trend of the Dead Sea brine (Figure 5a). Increasing from 1960 the intensification of the irrigation program in Kazakhstan/Uzbekistan, the water from the Amu-Darya and Syr-Darya was diverted from discharging into the Aral Sea and, consequently, its water level fell due to evaporation. The Aral Sea and Lake Tiberias surface water show negative Ce and Eu anomalies typical for oxic conditions of water, whereas the Dead Sea shows none. The hypolimnion of Lake Tiberias shows no Eu anomalies but positive Ce anomalies [67] (Figure 5a).  [66]; Aral Sea (unpublished); Great Salt Lake (unpublished); Lago di Garda (unpublished); Lake Tiberias [67]; Dead Sea [65]. (b) Possible correlations between Gd and Y anomalies. Data for stratified Lake Tiberias are taken from [67]. Upper and lower tentative trends are given with slopes of about 0.7 and 0.3, respectively.
The Y and Gd anomalies plot between lines with slopes of 0.3 and 0.7 ( Figure 5b). Both suggested bordering lines show small Y axis intercepts for surface water. The developing anomalies of the Aral Sea plot between these lines. Note that Gd anomalies of Lake Erie and the Great Salt Lake do not plot on one of the indicated lines.

Rivers and Streams
The REY abundances in rivers and streams depend on the lithology of their catchment areas and their bedrocks. Rivers passing big cities in developed countries are contaminated by anthropogenic inputs of Gd via sewage [48,52,56,[68][69][70] (Figure 6a) and other REE via industrial waste waters [71,72]. Waters of small rivers and streams constrained to only one type of rock show a relationship to their bedrock [73,74]. The perennial streams in Israel show different REY patterns during wet and dry seasons ( Figure 6b). Depending on the REY anomalies of either limestones or alkali olivine basalts, these rivers and streams inherit Y, small Gd and often negative Ce anomalies, but rarely Eu anomalies. The REY patterns of water from limestones resemble those of their host rocks, such as the Jordan River north of Lake Tiberias. The REY pattern of water from the En Gedi waterfall is typical for interaction with limestones.  [48,49,52]; (b) Stream and rivers in Israel during wet (broken) and dry (bold) seasons; (c) Chao Phraya River in Thailand during three different seasons [64]; (d) Streams from various siliceous rocks and Quaternary sediments in Australia [56]. Note that Eu is often not reported; (e) Rivers in South East Queensland, Australia [57]; (f) Correlation of Gd and Y anomalies. Upper and lower tentative trends are given with slopes of about 1 and 0.5, respectively.
Positive Y and Gd anomalies show assumed correlations with variable slopes between 0.5-1 ( Figure 6f) and a wide scatter of data from the Pioneer River catchment with mostly larger Gd-anomalies than those of Yttrium. Weathering of basaltic-rock yields precipitation of FeOOH and scavenging of REY [75]. FeOOH not only precipitates in basalts but FeOOH colloids move with the infiltrating water into underlying aquifer rocks and affects the springs in limestones of Reah and Maqla in Israel (Figure 7c). Typical is the increase of Tb throughout Lu.

Spring Water
The springs from granitic rocks in the Black Forest, Germany, show maxima for normalized Y [76] (Figure 7d). Negative Eu anomalies are inherited from dissolution of feldspars and positive Y anomalies are generated by calcite precipitation during weathering. Gd anomalies seem to be very low or even absent. Due to the extrapolation procedure, Gd anomalies are uncertain when the values of Tb, Dy and Ho scatter. The two patterns from Central Sardinia originating from Carboniferous granitoids [77] resemble those from weathering limestones, probably due to weathering of marble in metamorphites nearby. All these spring waters show wide scatter of Gd and Y anomalies (Figures 5-7). Gd anomalies in samples from felsic rocks are between −0.15 and +0.05, whereas those from limestones scatter between 0.1 and 0.5 (Figure 7e).

Groundwater from Wells with Temperature below 20 • C
Groundwater from observation wells in Triassic to Pleistocene sedimentary rocks in the Permo-Carboniferous North-Western German Basin, NWGB, show regionally varying REY patterns (Figure 8a-d). The brackish to saline samples from observation wells above the old Stassfurt salt mine represent mixtures of fresh water and leachates of salts. The patterns of the groundwater from granites in the Black Forest, Germany [63], and from granites, basalts and gneisses in the Czech Republic [47] reveal variable types of REY patterns (Figure 8e). The correlation of Gd and Y anomalies scatter widely with slopes of trend lines of about 0.5 (Figure 8f).    [83]; (c) brines from wells along Lake Tiberias and the Dead Sea, Israel [75]; (d) Groundwater from limestones in the Mukheibeh well field, Yarmouk Gorge, Jordan [53]; (e) well water from the Quaternary sediments in the North-Western German Basin [79]. (f) Correlation of Gd and Y anomalies. The slopes scatter between 0 and 0.6.

Geothermal Water/Brine
The geothermal waters with temperature >50 • C from all over the North-West German Basin [78,79] produce brines from Permian to Jurassic formations. One of them resembles REY patterns as in Figure 9b. These brines show REY patterns with Y anomalies but rarely Gd anomalies (Figure 10a). The waters from the Italian geothermal fields of Larderello-Travale ( Figure 10a) and Piancastagnaio (Figure 10b) continuously decrease from La through Lu with variable Eu and positive Y anomalies [83,84]. Reactivation and fracking of the well Groß Schönebeck, drilled into the reddish Permian strata (Rotliegend) north of Berlin, yield a wide spread of Y and Gd anomalies due to fracking (Figure 10c) [85]. The brine from the conglomerate (4215 m) is low in REY abundance but shows the highest Gd, Y and Eu anomalies after fracking. The REY abundance in brines before fracking is represented by the two highest patterns. After fracking, the highest anomalies are registered, which decreased with time. The strongly saline and reducing, 4000 m fluid from the continental deep drilling, KTB/VB in SE Germany, is very low in REE but shows a strongly positive Eu anomaly, indicating that Eu was divalent under the reducing conditions and temperature of 119 • C [88] ( Figure 10d). The chemically reducing vent fluids from mid-ocean ridges [86,87] show strong Eu anomalies but no Gd anomalies and only very small Y anomalies (Figure 10d). These waters are low in pH (pH of 2 to 4 at 100 to 400 • C).
Among all these geothermal brines, only those from well Gross Schönebeck show Gd and Y anomalies which are highly correlated due to fracking (Figure 10e).

Discussion
Dissolution of minerals in soils, evaporites and weathering of catchment and underlying rocks are the fundamental processes by which any infiltrating precipitation is mineralized. REY in groundwater depends on leachable components and adsorption onto and ion exchange into mineral faces [54]. Weathering of igneous rocks leads to isomorphous replacement of Ca 2+ by REY 3+ during precipitation of mainly carbonates or scavenging by Fe-Mn oxihydroxides.

Water-Rock Interaction
Infiltration of precipitation with low REY abundance into sediments, sedimentary and igneous rocks hosting brines with high REY concentrations induces renewed equilibration between solid and fluid phases in their contact zone. Due to infiltration of HCO − 3 in fresh water, some calcite or aragonite precipitate and incorporate REY due to which the latter decrease in pore water. Most of the released REY from dissolving major, minor and trace minerals is locally adsorbed onto surfaces of recrystallizing minerals. For instance, more than 99% of released REY from dissolved limestones are immediately adsorbed by oxihydroxide coatings or bound by ion exchange in surfaces of carbonates [54].
In the Dead Sea ( Figure 5), flushed-in calcite is converted into aragonite [89]. Aragonite incorporates less REY than calcite [29]. Therefore, REY abundances increase in Dead Sea brine. During diagenesis of carbonate sediments under marine conditions, REY are increased in limestone [90,91]. The high variability of Ce anomalies in diagenetic carbonates is caused by synsedimentation of clay minerals containing higher REY abundances than in the original carbonate sediment.
During infiltration of Mg 2+ -rich modern Dead Sea brine at higher stands into adjacent limestones, REE decrease in concentration due to mixing with fresh water, showing negligible anomalies. Under these new conditions, Ho (like all the other REE) is lowered due to coprecipitation with carbonates and Y anomalies increase because of the decrease of Ho. Furthermore, Y is less incorporated in new minerals because of its hydrophillic character ( Figure 11). This process may explain the wide spread of anomalies in Figures 8f and 9f. Because the brines are saturated with respect to calcite or aragonite, the infiltrated and mixed brines interact with calcite surfaces which become magnesian-calcitic in composition and REY-rich due to ion exchange with Ca 2+ in calcite surfaces [54]. Y seems to be less involved in this process than Ho [43] and thereby Y/Ho increases in the aqueous phase. REY are preferably incorporated into Ca 2+ -bearing minerals because of the similarity of ionic sizes (CN VIII: Ca 2+ 1.26 Å; La 3+ 1.30 to Lu 3+ 1.12 Å; ref. [92]). In flow-controlled processes (either solids settling in the water column or water moving through pores), Gd and Y effectively develop positive anomalies with time because Gd and Y are less adsorbed and/or incorporated in minerals than their nearest neighbors. Thus, the hydrophillic Gd and Y are slightly accumulated in the aqueous phase (Figures 1, 2, 4, 5 and 8). In order to explain these positive Gd and Y anomalies in seawater, the incorporation of REY must be controlled by ion species that show less negative free energies of aqueous tervalent REY than Gd and Y (Figure 2a) and lower formation constants of MCO + 3 than their nearest neighbors (Figure 1a). The resulting difference in covalency and physico-chemical parameters seemingly is the source of the hydrophillic character of Gd and Y and different partition coefficients of REE and Y between calcite and solution.
Positive Eu anomalies in groundwater are inherited by weathering of feldspars with their positive Eu anomalies, such as in vent fluids and those from the geothermal wells KTB/VB and Gross Schönebeck (Figure 10). In seawater and waters of lakes and continental seas, the negative Eu anomalies are inherited from weathering of limestones with their negative Eu anomalies (Figures 4-8). Positive Eu anomalies are generated in reducing environments of high-temperature geothermal brines [45,47] when Eu(III) changes into Eu(II) and its radius changes from 1.14 to 1.39 Å (CN VIII) [92].
Cross plots of Gd anomalies in groundwater vs temperature yield increase of anomalies in the range of 10-20 • C and decrease from 30-90 • C (Figure 12a). Cross plots of Gd anomalies vs pH reveal steep increase of Gd in the pH range between 5 and 6 and decrease between 7 and 10 ( Figure 12b). This is in agreement with the reports in [93,94]. No dependence on salinity is visible up to 250 g/l TDS.

Scavenging by Fe-Mn-Oxihydroxides
In Fe-Mn oxihydroxides, adsorbed Ce(III) is oxidized to Ce(IV) and negative Ce anomalies develop in waters. In the oxygen-rich surface water of stratified lakes, negative Ce anomalies develop due to catalytic oxidation of Ce on particles coated by Mn-Fe oxihydroxides and REY are adsorbed [95]. Gd and Y are less scavenged than their nearest neighbors [10,33,35]. If these oxihydroxides dissolve under varied conditions, the resulting groundwater does not feature Gd anomalies and it has none to slightly negative Y anomalies (Figure 7d). If FeOOH is reworked by phosphates, groundwater with relatively high Gd but small Y anomalies result by precipitation of churchite, Y(HREE)PO 4 [76]. Such examples are given in Figure 13, where well waters of Bad Schwartau, Germany, Mukheibeh and nearby Ain Himma, Jordan show smaller Y anomalies than Gd anomalies. The Jordanian sources showed this behavior only in 2016, although they have been sampled since 2000 [53]. When settling particles pass the reducing bottom water, the Fe-Mn coatings are dissolved and generate positive Ce anomalies, such as in the hypolimnion of Lake Tiberias or in the deep Tyro basin (Figures 4c, 5a and 14). Although the processes in the epi-/hypolimnion of Lake Tiberias, Israel, differ in stratification in the Tyro basin, the final results are very similar ( Figure 14). Different are the quantities of Gd and Y involved. For instance, Y increases from 40 in oxic to 60 pmol/L in anoxic water in the yearly overturning Lake Tiberias, and from 200 to 400 pmol/L in the deep stagnant brine of the Tyro Basin in the eastern Mediterranean during many millions of years. Gd increases by factors of 5 and 10 in Lake Tiberias and Tyro Basin, respectively [59], which reflects the importance of REY transport from the oxic to the anoxic zones. REY from vent fluids, leachates of volcanic rocks along ocean ridges and marine volcanoes are scavenged by formation of oceanic Fe-Mn crusts and Fe-Mn nodules [44,95].

Gd-Y Anomaly Correlations
In accumulating systems such as oceans and the Dead Sea, presenting the results of fractionation over geologic times intercepts on either X or Y axes are common. The Xand Y-axis intercepts reveal build-up of anomalies in deep times. In lakes and continental seas, the ratio of Gd and Y anomalies is 0.3-0.7 and for springs about 0.5 and groundwater 0.3-0.9, for rivers 0.5-1 (Table 1). These different slopes are generated by different types of water/solid interactions (Figures 4d and 7), settling particles in oceanic basins and monomictic lakes ( Figure 5), changes between wet and dry status of streams (Figure 6b) or drastic changes of weathering conditions during monsoon seasons (Figure 6c). In stratified oceanic basins and continental lakes, the oxygen-rich surface waters show correlated positive Gd and Y anomalies. Under anoxic conditions, Y and Gd anomalies are smaller and greater due to REY released from coatings [23,96]. In stratified water bodies of ocean basins built by atolls, the two low-slope trend lines in Figure 4d represent large variations in Y anomalies but small ones in Gd anomalies.
Thermal waters either show limestone REY patterns without Gd and Y anomalies (Tiberias Main Spring) or REY patterns with positive Gd and Y anomalies due to leaching phosphates/gypsum as part of evaporites (Tiberias Roman Spring; Figure 7a) or cements from sandstones in the Arava valley ( Figure 9b). The Ce anomalies in Figure 9b,c are uncertain because the La values could be enhanced due the methanotrophy [58]. Gypsum and phosphate cemented sandstones yield convex patterns towards the X axis but with positive Gd and Y anomalies (Figures 9b and 10a). They differ by their algebraic signs of anomalies from water that has dissolved FeOOH ( Figure 7d). Locally, there may be interaction with specific minerals that control REY distribution. Such a formation is churchite, YPO 4 , known from lateritic soils [76], which in addition to Y contain preferably heavy REE.
The correlation of Gd and Y anomalies in different aqueous media may be described by their ratios or slopes in Figures 4-10 (Table 1). In seawater this slope varies between either 0.8 for open oceans or between 0.07 and 0.2 in oceanic basins of the South Pacific. Note that the monsoon-affected Gulf of Thailand (Figure 6c) perfectly fits into the surface water line of ocean basins in the South Pacific (Figure 4d).

High Gd Anomalies in Aqueous Phases
In Figures 6a and 13, Gd anomalies are much higher than expected by the correlation with Y anomalies. There are at least two reasons for this: • anthropogenic Gd supply to waters ( Figure 6a); • repeated mineral-aqueous phase interaction ( Figure 13).
The anthropogenic effect is best produced in rivers into which effluents from wastewater treatment plants discharge (Figure 6a). The source of high Gd values is their application as stable organic complexes as a contrast agent in magnetic resonance tomography in clinics and private practices. For similar reasons affected are also lakes such as the Great Salt Lake, USA, Lake Erie and to a lesser extent also Lake Ontario [66] or the Tokyo Bay [2,68]. Partial dissolution of Fe-Mn oxihydroxides formed during weathering of Fe-rich rocks such as basalts may yield waters with enhanced Gd values because HREE are precipitated as phosphates. Such geogenic high Gd anomalies are known from well waters of Bad Schwartau, Germany, and Mukheibeh 9 and Ain Himma, Jordan ( Figure 13).

Conclusions
The REY patterns in groundwaters differ when dominated by weathering of either sedimentary or igneous or metamorphic rocks. In general, REY patterns of waters from igneous rocks are characterized by positive Eu anomalies. Ce, Eu, G and Y anomalies are mostly inherited from sedimentary rocks. Inherited Gd and Y anomalies further develop during water-rock interaction. The influence of humic acids is not considered here.
Gd and Y anomalies are mostly linearly related, suggesting that they are fractionated by similar mineral-water interactions. The presence of Fe-Mn-oxihydroxides as adsorbent plays an important role. This may be the main reason why geothermal waters show small to no anomalies, at least in wells after long-time production. REY patterns of water from felsic rocks differ because of their different compositions of leachable REY tracer minerals.
In addition to the positive correlation of the Gd and Y anomalies, the following trends are common: • carbonato and probably phosphato complexes and scavenging by FeOOH colloids generate positive Gd and Y anomalies; • Gd anomalies decrease with increasing Y anomalies when surface brines interact with carbonate rocks. In such processes, REE are lowered by adsorption and ion exchange but this process does not affect Y to the same degree; • redox-cycling in stratified water bodies transport of REE by settling particles is more efficient than that of Y. For that reason, Y n /Ho n is lower in the anoxic than in the oxic zone; for Gd anomalies it is the opposite (e.g., Lake Tiberias and Eastern Mediterranean); • under chemically reducing or acidic conditions Gd and Y anomalies are not generated; • Gd and Y anomalies seem to be controlled by pH; • excepting Eu anomalies, the anomalies of Ce, Gd and Y vanish with increasing temperatures by ion exchange with other minerals and are therefore mostly absent in geothermal waters; • anthropogenic contamination of surface waters produces Gd anomalies uncorrelated with Y anomalies.