Fractionation Trends and Variability of Rare Earth Elements and Selected Critical Metals in Pelagic Sediment from Abyssal Basin of NE Paciﬁc (Clarion-Clipperton Fracture Zone)

: The geochemical and mineralogical characteristics of pelagic sediments collected from the Interoceanmetal Joint Organization (IOM) claim area, located in the eastern part of the Clarion-Clipperton Fracture Zone (CCFZ; eastern tropical Paciﬁc), are described in this paper. The concentrations of rare earth elements (REE), as well as other selected critical elements contained in 135 sediment samples of siliceous clayey silts, are presented. The vertical and spatial variabilities of elements, with particular emphasis on REE as well as metals of the highest economic interest such as Cu, Ni, and Co, are detailed. The applied methods include grain size analysis by laser di ﬀ raction, geochemistry examination using ICP-MS, XRF, AAS, and CNS spectrometry, and XRD analysis of mineral composition (Rietveld method). Additionally, statistical methods such as factor analysis (FA) and principal components analysis (PCA) were applied to the results. Finally, a series of maps was prepared by geostatistical methods (universal kriging). Grain size analysis showed poor sorting of the examined ﬁne-grained silts. ICP-MS indicated that total REE contents varied from 200 to 577 ppm, with a mean of 285 ppm, which is generally low. The contents of critical metals such as Cu, Ni, and Co were also low to moderate, apart from some individual sampling stations where total contents were 0.15% or more. Metal composition in sediments was dominated by Cu, Ni, and Zn. A mineral composition analysis revealed the dominance of amorphous biogenic opaline silica (27–58%), which were mostly remnants of diatoms, radiolarians, and sponges associated with clay minerals (23% to 48%), mostly Fe-smectite and illite, with mixed-layered illite / smectite. The high abundance of diagenetic barite crystals found in SEM − EDX observations explains the high content of Ba (up to 2.4%). The sediments showed complex lateral and horizontal fractionation trends for REE and critical metals, caused mostly by clay components, early diagenetic processes, admixtures of allogenic detrital minerals, or scavenging by micronodules.


General Physical and Chemical Behavior of Rare Earth Elements
Rare earth elements (REE), also called rare earth metals, comprise the 15 lanthanides with atomic numbers from 57 to 71, i.e., lanthanum, cerium, praseodymium, neodymium, promethium, samarium, europium, gadolinium, terbium, dysprosium, holmium, erbium, thulium, ytterbium, lutetium, as well as two nonlanthanide elements that have properties that are similar enough to allow them to be included in this set, i.e., scandium and yttrium. Promethium, which may be formed in nuclear reactions, does not naturally occur on Earth in significant quantities [1]. REEs have unique chemical similarities, being usually divided into light (LREE = Light Rare Earth Elements; La to Gd) and heavy (HREE; from Tb to Lu and Y). Sometimes added is a "medium" (MREE; Eu to Er) division [2].
REEs are considered hydrolysates, since ions are easily hydrolyzed in aqueous solutions. In lanthanides, the pH of hydrolysis ranges from 8 for La to 6.2 for Lu. Therefore, REEs can be fractionated by hydrolysis in natural solutions over a large pH range. Due to small REE amounts in rocks and waters, lanthanide mobility in natural processes is more often controlled by the ability to form compounds from organic and inorganic ligands than by dissolving components. This capacity increases with the reduction of ion beams from HREE to LREE, which results in increased HREE content in standard charts, including sea water. However, average concentrations in porewater do not show this trend [3]. Limited REE mobility is associated with adsorption tendency on solid particles, mostly due to ion pair formation on the surface of particles, or simultaneous precipitation during the formation of solid phases, mainly due to subsequent isomorphic exchange and the adsorption on newly formed solid phases [4].
In sediments, sedimentary rocks, and sea water, most lanthanides indicate +3 oxidation state, with exceptions being Ce and Eu. Under aerobic conditions, trivalent cerium can be oxidized to Ce 4+ , and form compounds that are sparingly soluble (mainly CeO 2 ). Therefore, oxygenated water is depleted of complexion, that is enriched in oxygenated sediments. Similarly, in hypoxic water (under suboxic conditions), suspended Ce is mobilized and thus released, while in anaerobic sediments, Ce deficiency usually occurs [5]. This phenomenon of the enrichment or depletion of Ce in relation to neighboring REE is called a positive or negative Ce anomaly (Ce an ). The value of Ce an = 1 means that Ce is not different from the mean concentration in standard samples. Ce an < 1 is a negative Ce an , while Ce an > 1 indicates enriched Ce [6]. The highest Ce an is characteristic for hydrogenetic cobalt-rich crusts, phosphatized crusts, as well as hydrogenetic polymetallic nodules and micronodules. Diagenetic nodules exhibit a small positive or even negative Ce an , while fast growth rate crusts located in the immediate vicinity of hydrothermal sources, as well as carbonate sediments and seawater, are usually characterized by a negative Ce an [7,8]. Pelagic clays are mostly characterized by a positive Ce an and elevated MREE level, mainly due to the extraction of lanthanides from seawater by hydrogenic iron oxyhydroxides, and in case of Ce, also by manganese oxyhydroxides. In the sea water column, an increase of dissolved REE at below surface-depth due to the desorption of suspended REEs is noted, and the lowest value of a negative Ce an usually occurs at~200-300 m, which is directly associated with the upper oxygen minimum zone (OMZ). Therefore, the Ce an reflects the redox reactions in both water and sediments [6].
Eu also occurs at two oxidation levels (+2 and +3), and enrichment or deficiency also leads to the formation of a positive or negative Eu an , which can be an indicator of the inflow to sedimentation zones of abyssal material usually derived from hydrothermal solutions, fluids, volcanic rocks, and fragments of alkaline rocks [9]. A positive Eu an is an indicator of high-temperature hydrothermal solutions (as a result of water-basalt reaction), and may be associated with hydrothermal transformations of sedimentary rocks. A low positive Eu an is characterized by diagenetic nodules [8]. The supply of suspended and dissolved material in rivers, which is subordinately supplemented by aeolian material, the halmyrolysis of igneous rocks, or hydrothermal processes, is considered to be the main REE source in sea water. Evidence exists of the hydrothermal origin of REE-enriched sediment in LREE, especially

REE in CCFZ
According to factor analyses of chemical sediment components from the northern CCFZ, REE are positively correlated with Fe and Co, which suggests formation to be strongly influenced by hydrogenic processes (slow precipitation of metals from/under influence of seawater), and Ca-phosphate sources. The positive iron and cobalt relation may be the result of Co accommodation in the structure of amorphous Fe-rich gels, with different behavior under redox conditions. The nickel behavior is related to worse oxidation potential, compared to Co, which suggests accumulation within Mn-rich oxyhydroxide structures [33]. At the same time, REE show positive correlations with Al, K, and Ti, and negative correlations with Cu and Ni, which may suggest the influence of detrital material. Positive relations between Mn, Ba, Sr, Ni, and Cu are considered to be a diagenetic process effect [34]. Ni and Cu are related mostly to slow hydrogenic Mn-oxyhydroxide growth. Ba is usually included in diagenetic barite. Sr may be related to vacancy places in barite, or as small impurities in clay minerals or zeolites. The enrichment mechanism of REE in pelagic siliceous clayey silts from the western CCFZ is characterized by REE contents between 400 and 1000 ppm and significant negative Ce an [35].
REE and metal contents are usually related to Fe variations in interstitial water, which are strong reducing agents. The development of reducing conditions in sediment leads to an increase in Ce and LREE. The change from reducing oxidizing conditions promotes a more prominent decrease in Ce and LREE relative to HREE. A sharp rise of Ce content is related to reduction and transfer from solid sediment phases into interstitial water. LREE displays the lowest mobility during diagenesis. The accumulation of phosphates from interstitial water on diagenetic iron oxyhydroxide leads to additional extraction of HREE [4,36]. The development of reducing conditions in sediments is related to the oxidation of organic matter with oxidants including dissolved oxygen, nitrates, Mn +4 oxyhydroxides, Fe +3 oxyhydroxides, or sulfates [37].
The relationship between sedimentation rate, local hydrodynamics and pore-water geochemistry, with respect to the nodule coverage in CCFZ, has been studied by numerous authors [38,39]. The results indicate that sites entirely without nodules, or with only small ones, are characterized by higher sedimentation rates, lower contents of leachable manganese, and higher rates of nitrate and manganese oxide reduction below the oxygen penetration depth. These sites are also characterized by increased proportions of fine-grained sediment at the surface, a lower content of mobilizable authigenic manganese, and higher amounts of refractory manganese. Different coarse-grained particles, with higher amounts of leachable manganese and lower amounts of refractory manganese, occur in regions with large and medium-sized nodules [39]. Manganese mobilization in CCFZ sediment was and is strongly affected by shifts of oxic-suboxic redox boundary and bioturbation intensity [40], especially during Late Pleistocene-Holocene [41].
The main aim of this paper is to present a geochemical and mineralogical description of 135 sediment samples of siliceous clayey silts collected from the abyssal basin of NE Pacific (Clarion-Clipperton Fracture Zone). This study presents the vertical and spatial variability of selected metal contents, with the main emphasis placed on REE, Cu, and Ni, as well as Co and other metals. The relations between grain size, depth in the sediment column, and mineral and chemical compositions are also discussed, with special emphasis on neighboring polymetallic nodules polygons and the metal-rich sediments of the central Pacific.

Geological Setting
CCFZ is located in the northeast equatorial Pacific abyssal basin, between two fractures: (i) Clarion to the north, and (ii) Clipperton to the south ( Figure 1). The CCFZ area is approximately 5.5 million km 2 , extending 5200 km between 116 • W and 155 • W, and 1000 km between 5 • N and 15 • N. To the east, the zone bounds the Mathematicians Ridge (MR), which is believed to be the Paleo-East Pacific Rise (PEPR) western slope, west of the Line volcanic island arc [42,43]. Location of the CCFZ sampling area within the awarded to contractors (adapted from [44]); on the right, location of IOM H11 polygon on the geomorphological map of the seafloor [45].
Since the greatest concentrations of polymetallic nodules (PM) have been discovered in the CCFZ, this region has the best prospects for future deep-sea mining [46,47]. The PM are formed there mostly by hydrogenetic accretion and oxic-suboxic diagenesis [48]. Due to the great interest in PM, CCFZ is one of the better-known areas of ocean floor. Cartographic, bathymetric, seismic, sedimentological, economic, and environmental research have been conducted in this area since the mid-1960s [38,49,50]. This region is under the jurisdiction of the International Seabed Authority (ISA), Kingston, Jamaica, which has entered into 15-year contracts for exploration for polymetallic nodules with sixteen contractors [51].
The CCFZ geomorphological structure conforms to the pattern of a typical seabed structure for mid-ocean ridges and adjacent basins. A gradual increase of average depth from 3800-4200 m at 115 • W to 5400-5600 m is observed to the West. The average slope varies from 0.57 • in the east, to less than half a degree in the western part. Several volcano-tectonic units have been identified, such as the Cooper Rise, Central Rise, East Rise, and Shimada Seamount. In addition to these features, the seafloor is characterized by a regular bathymetric pattern that consists of a system of adjacent linear groups of ridges and valleys, aligned approximately perpendicular to the boundary between the Clarion and Clipperton Fracture Zones. Distances between neighboring crests vary from 1 to 10 km, with elevations above surrounding terrain up to hundreds of meters [31]. The CCFZ ocean crust is 10.6-10.8 km thick, and is composed of two complexes: (i) tholeiitic basalts, and (ii) overlying sediment cover, with a thickness of 100 to 300 m, and age range from Late Cretaceous to Quaternary [43,52].
The surface sediments within CCFZ are characterized by zonal distribution, and are represented by two classes with a few subclasses of biogenic sediments: (i) carbonate sediments, within which carbonate silts and clays, as well as carbonate oozes can be distinguished, and (ii) siliceous sediments (mostly red clays, diatom-radiolarian silts and oozes). Mixtures of these two end-members are predominant across the vast majority of the CCFZ seabed. Additionally, some minor sediment types are recognized, such as zeolitic clays or sediments heavily enriched with volcanic and hydrothermal components [52]. The carbonate compensation depth (CCD) ranges from 4000 to 4500 m, and is deepest in the westernmost CCFZ, shallowing towards the western Central America coast [42,53].
The surface sediments were classified using the Clarion lithostratigraphic groups, with three formations distinguished: (i) Line (F L ), (ii) Marquise (F M ), and (iii) Clipperton (F Cl ). F L is mostly represented by zeolitic clays, diatom-radiolarian silts, and siliceous silty clays, which are of the late Eocene and Oligocene ages. Based on the lithological composition of sediments and genesis within the formation, four lithostratigraphic units were distinguished: (i,ii) Marquise: F M I and F M II , (iii) Clipperton F Cl III , and (iv) F Cl IV [42,54].
The sediments studied in this paper belong to the F Cl IV unit, characterized by considerable lithological variability, the largest thickness of all units, as well as a macroscopically visible zonation. This unit is mostly represented by calcareous silty clays (up to 47% of CaCO 3 ), and Ethmodiscus silty clays (up to 32% of SiO 2am ). The uppermost horizon, the so-called semiliquid geochemically active sediment layer, is composed of two types of sediments: (i) siliceous silty clays (up to 30% SiO 2am ), and (ii) slightly siliceous clayey silts (less than 10% SiO 2am ). Sedimentation of this unit began during Pliocene and continues to this day [42]. Biological productivity and organism activity in CCFZ sediment is high in comparison with other oceanic basins [55]. Due to the higher biologically related uptake of nutrients, such as C, N, P, Si, and Ca in surface water, and the further remineralization in deepwater, the REE and metals accumulated more extensively in deeper Pacific basins compared to those in the Atlantic Ocean [56].
Sixteen contractors signed 15-year contracts for exploration for polymetallic nodules in the CCFZ. One of the first was the Interoceanmetal Joint Organization (IOM), a consortium of six states: Bulgaria, Cuba, Czech Republic, Poland, Russia, and Slovakia. The IOM exploration area is located in the eastern CCFZ and is composed of two separate blocks, B1 and B2, with a total area of 75,000 km 2 . Samples studied in this paper come from the IOM H11 exploratory area (located in B2; Figure 1) which constitutes a polygon that covers 5380 km 2 , and is rich in PM. The seafloor topography is dominated by elongated, streaked, and rounded patchy-like zones, showing high nodule coverage (>13 kg/m 2 ). Nodule-free sites are usually covered by soft siliceous-clayey sediments, often associated with high biogenic productivity or erosional near-bottom currents [46,57].

Sample Collection and Processing
A total of 135 samples from 45 sampling sites were collected in 2009 using a Reineck box corer (Ocean Instruments, Fall City, WA, USA), during the IOM research R/V "Yuzhmorgeologiya", in the IOM H11 polygon ( Figure 2). The surface area of the box corer is 0.25 m 2 and the maximum penetration depth 0.5 m, from where nondisturbed soft sediments were taken for analysis. Samples were recovered at a depth range from 4313 to 4529 m. The investigated sediments are mostly siliceous-clayey silts.
Based on macroscopic description, the samples were divided onboard into four horizons (called here also layers or sections). The main criteria were: (i) the sediment color, (ii) water content, and (iii) sediment consistency ( Figure 3): • horizon A-semiliquid geochemically active surface layer (0−5 cm; number of samples: 45), subsequently called "active layer" [43]. This horizon contains the highest amount of nonburied polymetallic nodules, which were removed from the samples before analysis. The horizon is characterized by a dark brown to brown color, the highest water content, and friable consistency. • horizon B-the upper part of the middle section (9−17 cm; n = 45). This layer is transitional between the uppermost semiliquid horizon A and the denser horizon C below. This sediment is beige with brownish bioturbation traces, lower water content than the uppermost layer, and is also more firm.   Since the number of horizon D samples is too few for separate statistical analyses, this interval is omitted in the present study.

Grain Size Distribution Analysis
The sediment grain size distribution was analyzed by laser-aided measurements using a Malvern Micro Analyzer 300 at the Institute of Marine and Environmental Sciences, University of Szczecin (IMES-USz, Szczecin, Poland). The lyophilized sediment samples were placed in 500 mL glass beakers filled with distilled water.
For better fractionation of sediments, samples were subjected to a 4-min water-based ultrasonic disintegration treatment, at a sound frequency of 20 kHz and water pump speed of 2000 rpm [59]. Each sample was treated with a 7 mL 1.6% sodium pyrophosphate dispersant solution. Analytical data were processed by the Malvern software (Malvern Panalytical Ltd., Malvern, UK) with conversion of values (for best optical laser coefficient) to the polydispersed illite + sodium pyrophosphate dispersion model [60]. The grain size analysis was recalculated using the Gradistat software (version 8, Kenneth Pye Associates Ltd., Shinfield, UK) in order to obtain the basic statistical grain size parameters. Grain size results use the ϕ unit according to formula (1) [61,62]: where D is mean grain size (mm).

Mineralogy
The bulk of the mineralogical XRD analysis was done on 41 selected samples, using a PANalytical Empyrean diffractometer (Malvern Panalytical Ltd., Malvern, UK). The analytical settings were as follows: monochromatic CuK-α radiation at 35 kV and 30 mA, scans from 5-70 • (2θ), step size 0.024 (2θ), using a wide angle detector (PIXcel 3D), conducted at the Faculty of Chemical Technology and Engineering, West Pomeranian University of Technology, Szczecin, Poland (WPUT). The X-ray diffraction results were recalculated using the Rietveld method and the RockJock software (version 11) [63]. The amorphous silica content was estimated as a background increase observed in X-ray diffractograms [64]. Due to the high resolution of obtained bulk diffractograms, clay minerals separation for further analyses was omitted. Also, no chemical treatment was applied to the clays. The matching of clay polytypes was done based on earlier experiments by Maciąg et al. [65], where separated clay subfraction <0.004 mm was heated, oriented, and glycolyzed. A quantitative analysis was performed based on the repetitive calculation of patterns (around 7 to 9 iterations), and finally, by comparison with experimental patterns, according to highest fit quality, expressed by the lowest residuals and highest goodness of fit. Kaolinite and chlorite were identified by the presence or absence, and the position, of the first low angle diffraction peak (~10Å for kaolinite, 14-14.2Å for chlorites).
Iron and manganese contents were analyzed by the AAS method at IMES-USz. The 30 sediment samples (each 0.6 g) were digested using a microwave oven with a mixture of three acids: 8 mL HNO 3 65%, 2 mL HCl 10%, and 2 mL H 2 O 2 30% [60]. The analysis was performed with a Unicam Solaar 969 flame atomization spectrometer. Biogenic element concentrations (TC, TN, TS) were analyzed at the same institute, using the same number of samples, by CNS spectrometry on a Vario MAX CNS Element Analyzer [66]. The total phosphorus content was estimated for 30 samples with the flow-injection absorbance photometric method (FIA), using an MLE photometer (Germany) [67]. Before measurement, samples were mineralized as AAS, with analyses also being conducted at IMES-USz.
A minor and trace elements analysis, including REE, was done on 135 samples. The elements were determined following [68] and after full acid digestion (HNO 3 , HF, HClO 4 and Aqua Regia), by ICP-MS (ELAN DRC II, Perkin Elmer, Waltham, MA, USA), at the Central Chemical Laboratory, Polish Geological Institute-National Research Institute (PGI-NRI), Warsaw, Poland. The ICP-MS data were normalized to the Post Archean Australian Shale (PAAS) [69]. To show differences in normalization standards, the eight most characteristic samples were normalized to the World Shale Average (WSA) [70], North American Shale Composite (NASC) [71], Upper Continental Crust (UCC) [72], PAAS, and chondrite [73].
To determine the individual sediment component groups and sample imaging, we used a Hitachi SU8020 ultrahigh-resolution field-emission scanning electron microscope (UHR FE-SEM, Hitachi High-Technologies Corporation, Tokyo, Japan). For analysis, material was separated by water flushing of selected samples with a φ = 0.063 mm sieve, or by gravitational sedimentary suspension in a glass cylinder filled with distilled water. The Energy-Dispersive X-rays (EDX) spectra were collected and analyzed in the NSS 3.0 software. The data were collected at WPUT.

Data Processing
Maps, graphs, and lithological profiles were prepared using the Surfer 9, Grapher 10, and Strater 4 software (Golden Software Inc., Golden, CO, USA). The basic statistics for the total population and each sampling level were calculated separately, using Statistica Statsoft 7 (Statsoft, Tulsa, OK, USA). Construction of correlation coefficient matrices used 45 samples within each sampling interval. Valid cases were presented for p = 0.95, and were compared/removed pairwise. Factor analysis (FA) and principal components analysis (PCA) were performed separately for each horizon. The final components were expressed by normalized varimax rotation. A comparison of the same statistical data within all sampling horizons determined the number and types of geological factors and potential influences of each factor on metal scavenging processes.
The generalized maps of mean grain size, total contents of Cu, Ni, and Co, total REE, and amorphous SiO 2 /clay minerals ratio were made using the geostatistical methods available in Golden Software Surfer 9 software. Because of the observed significant spatial data trend and drift, universal kriging was applied for contouring. The basic trend maps were constructed using simple polynomial 1st (one directional variability), or binominal 2nd degree functions (two-directional variability). Afterwards, omnidirectional variogram models were constructed for each map. We applied the linear trend equation as the drift function [74]. For two maps (total content of metals in horizons B and C), anomalous data points were removed from the data set. For maps of grain size, metals, and REE distribution, the full data set of 45 samples was used. In the case of amorphous SiO 2 and clay minerals ratio, maps were produced using data from 13 sample stations.
The use of geostatistical methods is not the main topic of this paper; therefore, similar or more detailed information about spatial modelling in the study area can be found in [75][76][77].
Additionally, normalized REE spider diagrams were oriented towards the maximum trend directions, and color scale was applied for better geographical presentation. This presentation allowed us to orient normalized REE contents with the spatial directions, and show differences in LREE/MREE/HREE fractionation according to the various data trends.

Grain Size Analysis
The grain size analysis indicated that 90% of studied samples were fine silts. The mean grain size varied from 5.86 to 8.08 ϕ (x = 6.83 ϕ), while the median ranged from 5.75 to 8.08 ϕ (x = 6.97 ϕ). Around 84% of samples showed unimodal particle size distribution, while 16% were characterized by bimodal distribution. Sorting coefficients varied from 1.06 to 1.82 (x = 1.53); however, in 72% of the samples, sorting was in range of 1.4 to 1.7.
According to classification [61], the sediments under study were poorly sorted. Over 80% of the samples showed coarse-skewness, while the rest were nearly symmetrical. Kurtosis ranged from 0.76 to 1.19 (x = 0.96), where 29% of samples were platykurtic, while the remainder were mesokurtic. Grain size fraction variability in the different depth horizons was mostly similar. The silt and clay content slightly increased in horizon C, while the sandy fraction decreased. The sandy subfraction content (>0.063 mm; <4 ϕ) in all 135 sediment samples ranged from 0.01 to 17.5% (x = 5.73%), while silt (0.004-0.063 mm; 4-8 ϕ) varied from 78.26% to 96.36% (x = 89.96%), and clay (<0.004; <8 ϕ) in 86% of samples ranged from 15% to 30%. The complete sedimentological data for individual horizons A, B, and C is presented in Table S1.

Bulk XRD Mineralogy
As per the general mineral composition (Figure 4), the analyzed sediments were dominated by amorphous, mostly biogenic opal-A, comprised of radiolarian tests, siliceous sponge spicules, or diatom frustules. Additionally, admixtures of amorphous siliceous volcanic glass with vitreous tephra composition were identified. The amorphous SiO 2 content varied from 27% to 58%. The greatest differences in silica content were observed in horizon C, where contents were from 27% to 57%, with a mean of 45%. The horizon B differences were smaller, ranging from 30% to 58%, with a mean of 47%. The differences within the horizon A were small (43-51%), with a mean of 47%. The amorphous silica content decreased slightly in deeper parts of the sediment column.
The clay content varied from 23% to 48%, and showed similar variability to the amorphous silica. Clay showed greatest variability in horizon C, varying from 23% to 48%, with a mean of 32%. The clay minerals content in horizon B was similar, and varied from 24% to 48%, with a mean of 32%. The clay contents within horizon A were less variable (28% to 34%), with a mean of 32%.
Illite was represented by fine-crystalline illite 1Md and detrital illite 1M 1 [80]. The total illite contents varied from 10% to 18.7%, with a mean of 13.2%. The content of illite slightly increased within horizon B and C (usually 2-3% more compared to horizon A), mostly due to the illitization process caused by burial diagenesis. The single-layered illite 1M was less represented (usually <2%). Additionally, randomly ordered mixed-layered illite-smectite occurred, with I/S between 0.5 and 0.7 [81].
The important identified diagenetic mineral was barite, with a mean content of 1.6%, and a minimum and maximum of 1.04% and 3.30%, respectively. The barite content in the sediment column was rather stable, though extreme values occurred in horizons B and C, in some cases exceeding 3%.
The other diagenetic mineral was halite, which formed during the removal of interstitial water from sediments, i.e., during sample drying. Halite contents varied from 3.3% to 7.9%, with a mean of 5.2%, and gradually decreased in horizons B and C, mostly due to lower porosity, compared to horizon A.
The allogenic components were represented by detrital quartz (of mostly aeolian genesis), plagioclase, and dark heavy minerals, such as pyroxenes. The quartz and plagioclase contents were quite similar, and varied from 3.8% to 10%, with means of 6.5% and 7.1%, respectively. The plagioclase was mostly of the andesine type, with less bytownite and oligoclase endmembers. The highest plagioclase content occurred in horizon C. Additionally, there were traces of pyroxenes (<1%) augite and enstatite types.

Geochemistry of Major Components, Trace Metals, and Biogenic Elements
All data of the major, minor, and biogenic elements is shown in Table S2. As shown by the EDXRF analysis of major elements, concentrations of Si and Al in all samples varied from 19% to 29.7%, and 4% to 6%, respectively. The highest contents of Si and Al were observed in horizon B. The mean content of both elements was respectively 23% and 5.3%, and was significantly lower in horizon C, mostly due to the dissolution of organic silica and transformation of clay minerals.
Concentrations of alkali metals (Na, K) were quite low (mean value 2.8%), ranging from 1.4% to 2.6%, and 2.6% to 3.2%, respectively. Potassium content was significantly lower in horizon C (x = 1.9%). The alkaline earth metal concentrations (Mg, Ca) were uniform, with a mean of 1.4% in both cases. A slight increase of Ca was observed in horizon C. The mean Ti content varied from 0.34% to 0.54%. The Cl content, due to diagenetic removal by halite crystallization, was lowest in horizon C. Contents of biogenic-associated P were lowest in horizon A (0.05% to 0.1%), and significantly increased deeper in the sediment column, with mean values of 0.64% and 0.84% for horizons B and C, respectively.
The AAS results show that Fe did not demonstrate important vertical differentiation. In horizons A, B, and C, mean iron concentrations reached 4.01%, 4.18%, and 4.02%, respectively. The Mn content was usually between 0.3% and 0.5%, with Mn/Fe ratios respectively of 0.12, 0.08, and 0.07.
The CNS analyses yielded low concentrations of carbon, nitrogen, and sulfur, which usually decreased with depth. The C content varied from 0.21% to 2.12%, with a mean of 0.55%. The N content was usually <0.1%, slightly decreasing with depth. The S content ranged from 0.33% to 0.70%, and was rather stable for all horizons. Mean values of C:N:S:P ratios were 5.4:0.2:6.6 in horizon A, 5.0:0.2:0.8 in horizon B, and 7.4:0.2:0.6 in horizon C.
A comparison of major and biogenic elements is presented in Figure 6.  The Cu concentration in horizon C varied from 197 to 1173 ppm, with a mean of 301 ppm. The Ni content ranged from 49 to 467 ppm, with a mean of 80 ppm. The Co content ranged from 17 to 277 ppm, with a mean of 43 ppm. The Ba content was similar to that of horizon A, ranging from 6170 to 13,645 ppm, with a mean of 8217 ppm.
Mean concentrations of Zn and Pb were quite stable within the sediment profile, and ranged from 93 to 199 ppm and 13-52 ppm, respectively. The Zn/Cd ratio increased from 590 in horizon A to 1609 in horizon C. The mean Sr and Rb concentrations were almost equal in all horizons, ranging from 348 to 353 ppm, and from 80 to 83 ppm, respectively. The Sc contents varied over 16-31 ppm. The highest Cr content occurred in horizon A (up to 627 ppm), and the lowest in horizon B (10 ppm).
The Mo content was characterized by a coefficient of variation as high as 270% (for horizon C). The highest Mo variability occurred in horizons B and C, respectively, by coefficients of variation as high as 219% and 145%, as well as by Ca (89%) over horizon C, and Ni (73%) over horizon B. The smallest variabilities are typical for Ti (2%), K (3%), Al (4.5%), Cl (5%), and Mg (9%), as observed in horizon A. The Th and U contents were also low and varied over 7.0−12.3 ppm and 1.0−1.9 ppm, respectively. The Th/U ratio was from 6.15 to 6.54, and usually increased with depth. The mean Cu:Ni:Co ratios were 2.1:2.7 in horizon A, 2.6:2.3 in horizon B, and 3.7:1.8 in horizon C.

Rare Earh Elements
As shown by the ICP-MS, total REE content varied from 200 ppm to 577 ppm, with a mean of 285 ppm (Figure 7). The total light rare elements (ΣLREE) content ranged from 127 ppm to 339 ppm, with a mean of 182 ppm. Total heavy rare earth elements (ΣHREE) concentration ranged from 23 ppm to 83 ppm, with a mean of 33 ppm. The highest mean contents of ΣREE, as well as ΣLREE, for horizon C were 291 and 187 ppm, respectively. In this horizon, REE were dominated by Ce, Y, Nd, and La (with means of 66, 56, 47, and 37 ppm, respectively). The highest ΣREE content variability, expressed by the coefficient of variation, occurred in horizon C (26%), and the lowest in horizon A (10%).
The  Higher diversity in PAAS-normalized REE distributions occurred in horizon B, where several samples showed strong positive Y an , expressed by Y SN /Ho SN ratio higher than 1 (max. 1.11), while other samples showed slight negative Y an (Y SN /Ho SN < 1). A few peaks of Y an are clearly visible in the spider diagram (Figure 9), which show positive Y an that may be related to increased contents of bioapatite, zeolites, or plagioclases. Negative Ce an in horizon B indicates a wide range, and varied from 0.36 to 0.81, with a mean of 0.71.

SEM-EDX
The SEM-EDX analysis confirmed the presence of the components found by XRD analysis, including detrital minerals such as quartz, plagioclase, pyroxenes, as well as diagenetic barite, and micronodules, small amounts of volcanic glass, and nonidentified lithoclasts (Table S3). Zeolites and calcite were not confirmed. Among the biogenic components, the biogenic skeletal remnants of radiolarians, sponges, and diatoms were identified. Foraminifera, mostly agglutinated and rare calcium carbonate, as well as phosphate remnants (carbonate-fluorapatite-CFA) occur in the form of fish teeth or skeletal debris (Figure 11a-f). The increased barium content in all horizons was associated with barite (BaSO 4 ). Diagenetic barite crystals occurred in the form of elongated coffin-shaped euhedral crystals, with dimensions that varied 20 to 100 µm (Figure 12a). Analysis by EDX revealed low substitution of Ba by Sr (up to 1.5%). Chemical impurities also include Si (1.3%), Fe (0.5%), Ca (0.1%), and K (0.1%).  Table S3.
Plagioclase signatures are typical of volcanic debris (Figure 12b). Domination by Ca and Na suggests the presence of bytownite-andesine-oligoclase endmembers. Additionally, in the feldspar debris, traces of Y (up to 200 ppm, not presented in this paper), Cr, Ti, and metals such as Cu and Ni were identified.
The examined micronodules were small Mn-Fe particles, usually <2 mm in diameter, formed in sediments by complex diagenetic-hydrogenic processes, which showed increased contents of metals, such as Ni, Cu, Co or REE (Figure 12c,d). The weight amount of micronodules in the selected sediment horizons may reach a few percent [84,85]. Micronodules showed high levels of Mn, with a mean content of 50.8%. The mean content of Fe was 13.5%, while for Ni + Cu, it was 3.0%, and in some cases, exceeded 5%. Micronodules showed admixtures of external components, mostly debris or clay aggregates, rich in Si and Al, totaling 8-9%. Additionally, micronodules showed increased Zn contents and traces of Ti, Na, Ca, Mg, K, Ba, Sr, Mo, Sc, and F. The level of phosphatisation was low, usually <0.1%. The contents of S and Cl were also low.
According to some geochemical signatures (Figure 13), micronodules from IOM H11 were formed by a diagenetic influx of hydrogenic processes (so called mixed-type). The complete SEM-EDX geochemical data for micronodules are presented in Table S3. Biogenic phosphates were represented by carbonate fluorapatite (CFA), which contained impurities of metals such as Ni or Zn, usually around 3-4%. Additionally, increased contents of S, Cl, and F were identified. The CFA may show elevated contents of REE, dominated by Y and La, which may reach more than 0.5%. Analyzed fish remnants showed traces of Fe, Mn, Si, Al, Cr, Ti, alkali, and alkaline metals.
The clay dominated separates showed a Si/Al ratio of 2.3-2.4 and elevated contents of Fe, with minor quantities of Mn, Cr, Ti, Ba, and Ca. The mean contents of Na, Mg, and K were 3.2%, 2.4%, and 1.9%, respectively. The Cl content was also increased, mostly by interstitial halite crystallization, reaching from 1.5% to 2.0%. The REE positively correlated (>0.9) with total clay minerals content (0.5), and with detrital minerals, such as quartz or feldspar. Ce showed slightly anomalous behavior, i.e., lower positive correlations with metals and other REE (0.6 to 0.7). REE did not correlate with Fe and Mn, and showed a negative relation with halite and amorphous silica content (0.5 to 0.7, respectively). The C and N also showed negative correlations with REE, but was positively related to S.

Horizon B
Similar to with horizon A, the grain size composition of horizon B was strongly related to the quantity of fine silt and clay fractions (0.86-0.93). REE content was essentially positively correlated with fine fractions, clay minerals, barite, and metals such as Fe, Mn, P, Ba, and S. Ce showed positive correlation only with P (0.66), Zn, Pb, As, Sn, Rb and Sc. Similar behavior occurred with Sc, which was more strongly related to U and Th, than Ce. Fe and Mn were positively correlated (0.94) and also showed positive relations with other metals (0.6 to 0.9) ( Figure S1). Anomalous behavior (lack or low correlations) was indicated with Ag, Sn, Rb, Sc, and Ce. Correlations between Ni, Cu, and Co were high (0.9>). Mn and Fe showed strong positive correlation with Sr, Ba, and S (around 0.6 to 0.9). Metals such as Ni, Cu, Co, Zn, Pb, As, Mo, Cd, Tl, Sr, and Ba showed positive relations with each other, i.e., usually around 0.7 to 0.9, but did not show positive correlations with Rb, Ag, Sn, and Cr. Th and U contents showed positive correlations with P, Zn, Pb, As, and Sn (0.5-0.7), as well as with REE (0.4-0.5). Biogenic elements such as C and N indicated strong negative correlations with fine fractions, metals, and REE (−0.5 to −0.9). Different behavior was displayed by S, which showed positive relations with fine fractions and most metals, including REE.
Compared to active layer, correlations between minerals and selected elements were clearly visible. The feldspar content was positively related to clay minerals (especially smectite) and barite (0.6-0.9). Barite was positively correlated with REE. Kaolinite and illite did not show any special relations with REE and metal contents, apart from P, Rb, Sc, Ce, Th, and U. Biogenic amorphous silica was positively correlated with coarser fractions, biogenic elements (C and N), and halite. Opaline silica showed strong negative relations with almost all metals.

Horizon C
The correlations between selected metals and minerals in horizon C were comparable to those in horizon B, but more uniform and distinctive. The REE were positively correlated with fine fractions (0.6-0.7). Correlations of metals (excluding Cr) with coarse fractions were significantly more negative, compared with the two higher horizons. Almost all metals showed positive relations with Fe and Mn. Additionally, P, S, and REE showed strong positive correlations with most strategic metals, except for Ag, Sn, and Cr. The REE correlation with S was also weaker in comparison with horizon B (0.26-0.33). P and most metals (apart from As, Ag, Sn, Rb and Th) were well correlated with each other (>0.8). P was strictly related to fine fractions, while correlating negatively with Cr, C, and S. Ba and Sr showed similar behavior. The contents of Th and U also showed positive relations with Ag, As, Sn, Rb, as well as with fine fractions, especially fine silt and clay. C and N indicated negative correlations with all metals, and correlated positively only to coarser fractions.
For minerals, barite was positively correlated to other metals and REE (0.8-0.9); however, a lower coefficient was observed in the case of Ce (0.7). Feldspars were positively correlated to clays, especially smectite and illite, and additionally to REE.
According to the comparison of grouped LREE-MREE-HREE correlation coefficients in horizon A, there was a general tendency for correlation increase between HREE and coarse fractions, as well as P contents. The REE content seemed to better correlate with Mn than Fe. In horizon B, the relation of REE with P was less significant, and appeared to be more uniform in each subgroup. The REE showed stronger relations with Fe than Mn. In horizon C, the picture is quite similar; however, a slight increase of correlation coefficient between REE, P, Ba, and clays was observed. The full correlation coefficients matrices for each sampling horizon are presented in Figure S1.

Principal Components Analysis (PCA)
The FA and PCA analyses indicated a dominance of two factors (components), which covered 63%, 76%, and 84% of the total analyzed sample variability in horizons A, B, and C, respectively. The influence of factor 1 increased gradually in horizons B and C (64% and 69%, respectively). The value of factor 2 was quite uniform for all horizons, but showed an increase from the top to the bottom sections of the sediments. Other minor factors were also uniform in all horizons ( Figure 14). The PCA loadings showed a strong fractionation of REE and selected metals in horizon A. Most other variables were dispersed on the PCA loading plot (Figure 15), indicating low correlations. REE and metals such as Sn, Rb, Ag, and Th showed negative correspondence with Mn, Fe, amorphous silica, halite, C, N, and clay fraction, when compared with other metals (i.e., Ni, Cu, or Co). These patterns may suggest an external REE source, controlled mostly by biogenic input, coarser fractions (mostly silt), and relations with polymetallic nodule formation mechanisms. Critical metals showed weak positive relations to coarse fractions, illite, and quartz content, which also suggest dominance of external factors (hydrogenic or hydrothermal input). Variables in horizon B showed different behavior and grouping of REE, or several other metals. The REE, apart from Ce and Sc, were positively correlated with other metals such as Fe and Mn, as well as clay minerals (especially smectite) or barite, which suggests diagenetic remobilization. The relation was negative with amorphous silica content, biogenic elements (C, N, and P), silt, and sand fractions. Ce, U, and Th are grouped in a second small cluster, suggesting some different oxidative behavior, or a relationship with biogenic phosphates input and dissolution. The visible grouping of variables and the unification of factors are related to more pronounced fractionation in comparison with horizon A.
Variables in horizon C showed behavior similar to horizon B, and even more apparent REE and metal groupings, which may be related to Fe and Mn immobilization, barite formation, or to decomposition of phosphates. The relations were also positive with some external components, such as plagioclase or pyroxene contents, suggesting additional external influences. Fractionation model in horizon C may be strongly shaped by a diagenetic transformation of clay minerals, burial degradation of allogenic components, or barite formation, mostly in regime of extensive S and P suboxic consumption.
The anomalous Ce positions in the plot may be related to different oxidation properties of Ce 3+ . Even such an autonomous metal as Ag (besides Cr) is fractionated in horizon C, indicating a strong relationship with the transformation processes that occur in sediments.

Spatial Variability
The sedimentological, geochemical, and mineralogical data presented on the maps show distinctive spatial features ( Figure S2).
The mean grain size of siliceous clayey silts shows generally highest variability in the E-W direction, and lowest in N-S. The sediments show patchy-like type of zonality. The spots of coarser material were located in the central part of the study area, and in case of horizon A, also in the NE part of the polygon. The finest sediments were located mostly in the outer parts of IOM H11, especially western and eastern portions of the region. The pattern was generally the same in all horizons; however, at greater depths, it was most uniform in horizon C.
The total content of Cu, Ni, and Co showed spatial features other than grain size. The data generally trended NW-SE, with the lowest variability being observed in the SW-NE direction. The metal contents were more evenly distributed in the active layer in comparison with horizons B and C, and did not show any specific trend. In the active layer, the highest concentrations were observed in the SW and NE parts of the polygon. The lowest values occurred in the central study area.
Compared to the active layer A, horizon B showed the lowest content of metals in the NW and SE of polygon. The zone of intermediate metal contents was oriented N-S, with a few spots of increased content in the NE area. The mean contents of metals in horizon B were generally lower compared to the active layer, but higher than in horizon C.
The total metal content in horizon C generally trended NW-SE. The lowest contents occurred in the central and SE parts of the polygon, increasing towards NW with a few concentrations of higher metal contents being observed in NW area. The total metal contents in horizon C were lower in comparison with horizons A and B.
The REE distribution maps show good spatial convergence with grain size and SiO 2am /clay minerals ratio, especially in horizons B and C. The REE data trends were similar in horizons B and C. The highest variability occurred in the NW-SE direction. The elevated contents of REE in the active layer occurred in NW and N parts of the polygon. Horizon B and C showed similar distributional patterns, and the intermediate REE content zonation was oriented N-S, which mostly covered the central part of the polygon. Elevated contents of REE occurred in some concentrations located near the eastern border (horizon B) and western part of the region (horizon C) of IOM H11 polygon.
The maps of amorphous silica/clay minerals contents show the influences related to diagenetic burial dissolution of silica and transformation to clay minerals. The highest ratios of both variables show NW-SE trending in all horizons, with the lowest ratios in the eastern and western parts of the polygon.
The lithological profiles presented in Figure 16 show vertical changes of the grain size composition, mineralogy, and geochemistry of individual horizons A, B, and C (Figures 16-18). Three general models of vertical variability were observed: (i) the content of REE, Fe, Al, Ba, and clays was intermediate and increased with depth, while the amount of Si, Mn, Ni (and other metals), and coarse grain fraction decreased or was uniform in all profiles ( Figure 16); (ii) the content of REE, Fe, Mn, Al, Ni (and other metals), and Ba was lowest among all samples, while coarse fraction content was the highest in horizon A, and the Si (and amorphous silica) content increased with depth, or was quite uniform (similar to clay minerals) ( Figure 17); (iii) the contents of REE, Fe, Mn, Ni, and Ba were highest in all sample populations and associated mostly with horizon B, while Al, Si, and clay contents increased with depth or were quite uniform within the profile (Figure 18).

Discussion
The sediment distribution and composition in CCFZ depends on several environmental factors, including: • moderate biological productivity of surface waters (higher in the eastern area and lower in the west); • bathymetry and distinctive linear topography of the seafloor; • low sedimentation rates; • depth of CCD ranges from 4000 to 4500 m, which determines CaCO 3 contents <10%; • early diagenesis processes affecting neoformation and transformation of clay minerals; • tectonic, volcanic and seismic activity [43].
Surface sediments from the IOM H11 area show significant spatial relationships to the accumulation of REE and other strategic metals. The main process that influences scavenging of rare earths is the early diagenetic remobilization of metals and neoformation of diagenetic clay minerals. Acquisition of REE is related to sorption and immobilization mechanisms during the transition from oxic to suboxic conditions. The formation of Mn-(Fe) oxyhydroxides as micronodules and clay minerals, mostly Fe-rich smectite, determine the bonding of REE and metals, such as Ni, Cu, or Co. Other processes of different REE fractionation patterns include: (i) the presence of allogenic biogenic phosphates, mostly CFA, in the form of teeth and skeletal remnants of fish, which may determine low Ce an indicated in selected samples; (ii) admixtures of detrital material, such as feldspars or pyroxenes, which may explain the higher metal contents in some sample locations, or increased contents of HREE; (iii) the presence of micronodules or nodule remnants, which usually show greater quantities of REE and other metals, in comparison with sediments.
The data of mean grain size and total Cu, Ni, and Co contents showed low spatial correlation in the active layer (horizon A). The highest metal contents correlated with finest fractions, especially in SW and E of study area. The spatial relations between SiO 2am clay minerals were not so clearly apparent; however, the lowest ratios, related to increasing clay contents, corresponded positively with the highest metal contents in the active layer. Some anomalous spots, including sample stations 2262 or 2292, showed the presence of higher micronodule quantities, which are visible in grain size data, as medium or fine sand subfractions.
The zonation of REE and metal contents in horizons B and C were similar, which may constitute evidence of the same fractionation trends. The lowest contents of REE were observed in the central and S part of polygon, excluding only few stations, such as 2264 or 2295, where increased REE contents also occurred within sediments with intermediate or elevated amounts of Cu, Ni, and Co. These patterns indicate REE fractionation between coarser fractions of sediments, to suggest that low contents of biogenic silica are needed to accumulate REE. These processes may correspond with early diagenetic remobilization of metals in horizon B, or REE and metal scavenging controlled by clay minerals adsorption. Described remobilization patterns may be strongly conditioned by biogeochemical processes within the sediment column, related to burial and reduction of sulphates and organic carbon degradation, likely controlled in some cases by bacterial processes, denitrification, and finally, the dissolution of biogenic phosphates, mostly CFA [87].
The distribution patterns of total metal content and REE were similar in horizons B and C, but were different in the active layer. The highest contents of REE occurred in the NW part of the polygon, accompanied by elevated contents of Cu, Ni, and Co. The strong evidence of diagenetic fractionation of metals and REE corresponds well with fine silt and clay subfractions, which dominated in the NW part of polygon. The pattern of diagenetic REE uptake is particularly apparent in horizons B and C, when compared using the REE distribution map with SiO 2am /clay ratio. The increased influence between metals accumulation (including REE) and clay fraction contents, or lesser contents of silica, is especially apparent when horizon C is compared with A. Horizon B is a transition between A and C, where the described parameters were in the middle, suggesting some stability or gradual change of diagenetic processes in the uppermost 30 cm of sediment column.
A comparison of grain size data showed that quantities of clay minerals, biogenic silica contents, and REE distributional patterns, as well as the early diagenetic immobilization of metals such as REE, Ni, Cu, Co, or Zn, could also be related to the presence of micronodules. In the lower sediment depths, the feldspars content showed a positive relationship with clay minerals, especially illite and smectite, which may be an indicator of burial alteration and plagioclase decomposition processes [88]. REE related to feldspars or other allogenic debris components may be an additional source of Y or HREE, mostly in the deeper parts of sediment column. Additionally, in horizon C (or even deeper), the role of P, S, and Ba in the acquisition and fractionation of REE increased.
The observed REE ratios are important indicators of hydrogenic, hydrothermal, and biogenic processes. The Ce/La ratio is an indicator of the relationship between hydrogenic (>2) and hydrothermal (<2) impact upon sediments [9]. In that study, Ce/La ratio ranged from 0.9 to 2.07 ( Figure 19), with only seven samples reaching or exceeding a value of 2, accompanied with positive Eu an . These suggest a strong positive relationship between sediments and hydrothermal conditions. Pelagic sediments are usually Ce depleted and show a negative Ce an , while polymetallic nodules usually indicate strong positive Ce an [6]. This factor, as well as enrichment of MREE compared to LREE and HREE, is typical for sediments formed away from terrigenous sources at relatively slow sedimentation rates [4]. The REE fractionation in oceanic waters was reflected in the mineralogical and geochemical composition of bottom sediments. The REE content and positive Ce an usually increases in sedimentary processes, with a higher contribution of reactive iron and manganese. Increase of bone debris content in pelagic clays, as a result of low sedimentation rates, leads to the inversion of REE composition. The depletion of Ce and LREE becomes stronger, mainly because bone debris accumulates considerable amounts of REE dissolved in oceanic water, probably without any noticeable fractionation. Pelagic clay with high bone debris content represents the terminal member in the series of sediment types formed during the oceanic material fractionation [4]. Negative Ce an were related to the different oxidation potential of Ce and were associated strong relation with Mn-Fe oxyhydroxides, which are the main oxidizing agent [56].
Oliver and Boyet [89] suggested that Ce an , as well as the enrichment of HREE relative to LREE, could be masked due to elevated contents of terrigenous material. This situation is particularly true, as regards the clay minerals and fine grain quartz, often depleted together with REE [90,91]. Bau and Dulski [92] proposed a binary diagram, which provides a test of whether the calculated negative Ce an was real, or masked by positive La an (Figure 20). Low Gd an , apparent in a few samples, was likely related to inorganic speciation, as well the positive Eu an , which is usually connected with hydrothermal input [56]. The issue of normalizing the REE results to individual rock standards was broadly discussed by [6]. The most commonly used standards are the North American Shale Composite (NASC), Post Archean Australian Shale (PAAS), Upper Continental Crust (UCC), World Shale Average (WSA), and chondrites; however, depending on the author, the values may differ. A less commonly used rock standard is clay from the Russian Platform [93].
A comparison of the REE distributions in the selected samples of horizon B normalized to different rock standards is presented in Figure 21. These samples were selected to show the most representative values (maximum and minimum REE contents, including LREE and HREE, or LREE/HREE).
There are several differences in normalized values, and in the shape of spider diagrams. The PAAS-normalized values were higher than WSA (the difference ranges from 4% for Ce to 58% in Tb), and spider diagrams are more flattened (Figure 21a). Positive Eu an was higher (9.8%) when PAAS-normalized, but slight Tb an and Tm an are present on the WSA-normalized spider diagrams. In both cases, the distributions were enriched with MREE, in comparison to LREE. The NASC-normalized REE distribution diagram was similar to the UCC-normalized one; however, for all samples, positive Dy an are apparent on NASC-normalized diagrams (Figure 21b).  [69] and WSA [70], (b) NASC [71] and UCC [72], and (c) PAAS and chondrite [73].
The most significant differences in values and shapes of spider diagrams are apparent with chondrites-normalized REE distribution (Figure 21c). The values were higher than other standards by two orders of magnitude, and the spider diagram trends are reversed, i.e., distributions are enriched with LREE, in comparison with MREE and HREE. The Ce an were similar to other standards; however, only chondrite-normalized REE distributions showed slightly negative Eu an , i.e., in the range of 0.78 to 0.92. The above comparison indicates the accuracy of the rock standard used to normalize the results of the analyzed sediment samples.
Observed negative Ce an usually represent variability of oxic conditions into a sedimentary environment and in the water column, but in this particular case, the changes were caused mostly by authigenic phosphate and authigenic Fe-rich smectite formation, being the effect of early diagenesis. The reaction between Fe oxyhydroxides and biogenic opal, by which the Fe-smectite can be formed, suggests an early diagenetic process, which is in equilibrium with seawater REE [94]. Of particular note, the PCA indicated an increase of Ce geochemical independence with depth, especially apparent in horizon C, which may have been caused by the different oxidation behavior of Ce, compared to other REE. Ce showed similar trends to U or Sc, and did not correlate with metals, such as Ni, Cu, or Co. This shows that the accumulation tempo of these metals and REE differed significantly due to oxix-suboxic changes in the sediment column, caused mainly by early diagenetic processes.
The high quantity of Fe-smectite may indicate the primary presence of pyroclastic material, such as volcanic glass, and effect of halmyrolysis. This mineral may also have a detrital origin, but the quantity in the analyzed samples (6.6-32.8% of all mineral phases), the occurrence of volcanic glass previously found by [60], and the distance from land are suggestive of authigenic origin [95].
Since the depth of sampling sites ranged from 4333 to 4443 m, which is below CCD, the cause of increased calcite content in some samples (up to 9.2%) is not clear. There could be two reasons for calcite enrichment of these sediments: (i) as per quoted CCD depths in CCFZ [42], some sample stations in the eastern part of studied area may have been above or within the CCD interval (for example sample 2297 25-30, which contained the highest quantity of calcite, sampled from a depth of 4333 m); (ii) the carbonate-rich sediments could occur below CCD due to slumping. An increased concentration of calcite in the sediments below CCD was found also in the southern part of BGR Claim Area adjacent to IOM H11, explored by the Federal Institute for Geosciences and Natural Resources of Germany [96].
Local heterogeneity of geochemical parameters is related to small scale local variability of depositional environment parameters, such as topography, biological productivity, hydrothermal effects, dissolution of nodules, or redox zonation [97]. In some parts, the elevated metal contents in CCFZ may also be related to buried hydrothermal microchimneys [98].
Apart from this, admixtures of REE may be related to weathered basaltic material from the Hawaiian area seafloor [99]. The elevated REE concentrations can also be attributed to desorption from resuspended sediments and pore water released into the overlying water column [100].
Increased CaCO 3 concentrations (maximum values at 19-28 cm bsf) can also be associated with abundant and well-preserved foraminifers, and may be correlated with the last glacial maximum (approx. 26,500-19,000 years ago) [101], when the increased productivity zone was located more to the north. At that time, the CCD interval was lower, associated with higher sedimentation rate and supply of carbonate material to the sediments. After the location of the increased productivity zone moved further south and the CCD became more shallow, probably not all carbonate components were fully dissolved [96].
The presence of phillipsite-Na occurred in two samples (2269 25-32 and 3016 10-15). Phillipsite, which is a zeolite, is commonly found in pelagic sediments, mainly as an authigenic mineral, forming zeolitic clays (>5% of zeolites), and results mostly as halmyrolysis of volcanoclastic material in a oxidizing environment, mostly in locations with slow accumulation rate. Phillipsite is considered by some authors as a main host mineral for REE in marine sediments [102]. In fact, the two aforementioned samples showed an increased REE content (544 ppm and 436 ppm, respectively); however, REE hosting phillipsite has not been proven. Sa et al. [21], who studied sediments from the Central Pacific, showed that REE are mostly concentrated in bioapatite (fish teeth and bones), and concluded that the main factors in REE enrichment include low sedimentation rate, decrease of mean grain size, and increase of quantity of biogenic apatite. The increase of REE in presence of CPA was probably caused not only by substitution, but also by adsorption (compare [87] or [103]). The REE enrichment processes may also have been generated by strong adsorption capacities of clays and Mn-Fe microparticles, or widespread oxic conditions [103]. Additionally, the positive correlation between P and Ce in horizon B suggests acquisition by hydrogenic processes [104].
The high contents of Ba were directly related to the increased contents of barite found in several samples analyzed. Additionally, high contents of REE were confirmed in samples with distinctive barite enrichment. As indicated [99,105,106], barite in deep-sea sediments is proxy of hydrothermal solutions, precipitation of water column, or authigenic product of pore waters. The barite in the studied area was mostly diagenetic, formed by burial diagenesis, and was characterized by relatively large size (up to 100 µm) and coffin-like tabular-shaped crystals. As an indicator of early diagenesis, barite may be related also to organic matter productivity in surface waters, and the presence of higher contents of biogenic silica, which may be transformed during burial processes [107].
Barite remains stable under oxidizing conditions, but becomes demineralized when reducing conditions are present [105,108,109].
A comparison of obtained Ba concentrations with the results of similar studies carried out in the central part of the CCFZ [95], as well as sediments collected from the Government of the Republic of Korea Claim Area [42], confirmed the distinctive enrichment in Ba. The barium contents in nine sediment samples analyzed by former researchers [95] ranged from 3884 to 12,997 ppm, with an average of 6154 ppm, while the average Ba concentration in later studies [42] was 6508 ppm. The observed enrichment of REE in samples below the active layer can be attributed both to crystallographic constraints of substitution, or to solution complexing of REE in the precipitating medium. The alkalinity usually increased with depth and sediment redox potential, which could cause significant complexing and depletion with HREE [110,111]. The LREE/HREE fractionation in sediments from IOM claim area is directly expressed by increased correlation coefficients between Ba, barite, and REE, observed in horizons B and C.
Metal resources, including REE, found in the horizon A sediments in H11 exploration block, were calculated by earlier studies [76]. The total inferred quantities of Cu, Ni, and Co were estimated to be 140,000 Mg, of which Cu is dominant (94,000 Mg) over Ni and Co (36,000 Mg and 14,000 Mg, respectively). The gross tonnage of Cu-Ni-Co ore grading is comparable to only small hydrothermal sulfide deposits and some land-based sedimentary ores. The above value equals only 14-15% of the estimated total resources found in polymetallic nodules from the same polygon [57].
According to bulk sediments geochemistry, REE have slightly greater economic value than Ni, Cu, and Co, with total REE resources estimated to be 58,000 Mg, which may be comparable with some REE placer deposits and low-grade land-based vein resources. The individual Ce, Y, Nd, and La resources are as high as 13,600 Mg, 12,600 Mg, 10,200 Mg and 8200 Mg, respectively [76]. The individual contents of REE and some selected metals (Ni or Co) were higher when compared, e.g., with hydrothermally affected carbonate sediments [22], but definitely lower (except for REE) than in typical metalliferous sediments forming in hydrothermally active seafloor zones [112].
As observed by Volz et al. [87], the redox zonation which affects metal accumulation in CCFZ is determined by the differences in surface water productivity, mostly organic flux to the seafloor, low sediment accumulation rate, and the oxidation of pore-water Mn 2+ at burial depth. Diagenetic modeling have indicated that due to low sedimentation rates, labile fractions of organic carbon are limited to the upper 20 cm of sediment column, where organic carbon degradation is dominated by aerobic respiration. The Mn 4+ reduction and denitrification are not so important, and consume less than 2% of the refractory organic matter.

Summary
(1) The presented data indicate that early diagenetic fractionation of REE and metals, such as Ni, Cu, or Co, occurred in oxic-suboxic conditions and with the presence of increased content of clay minerals. The changes of metal concentration observed in the siliceous clayey silts are comparable with other data from CCFZ, and suggest a strong influence of the degradation of organic matter during burial diagenesis.
(2) An ICP-MS analysis showed that the total ΣREE contents varied from 200 ppm to 577 ppm, with a mean of 285 ppm, which is generally low. The highest ΣREE content was observed in horizon C (>25 cm).
(3) The mean content of light rare earth elements (ΣLREE) was 182 ppm, while the total of heavy rare earth elements (ΣHREE) was 33 ppm. The LREE/HREE ratio was uniform in all horizons, varying from 0.62 to 0.64.
(4) The PAAS-normalized REE distributions were similar for each horizon and showed negative Ce an , weak positive Eu an , small positive Y an expressed by Y SN /H SN ratio >1, and also an apparent enrichment of MREE, compared to LREE. The Ce/La ratios indicated strong dominance of hydrothermal REE influx in all horizons. Greater hydrogenic acquisition of REE was observed only in horizon B.
(7) Clay minerals were dominated by illite and smectite (or mixed I/S), which formed mostly due to burial diagenesis. Clays greatly affect REE processes and metals acquisition. The elevated contents of HREE may be related to some admixtures of allogenic debris components, or the formation of diagenetic micronodules. Other signatures of elevated REE contents were diagenetic barite and zeolites. (8) The early oxic-suboxic diagenetic degradation of biogenic silica and bio-geochemical consumption of CNS and P during burial processes reflected better fractionation of critical metals and REE in the deeper parts of sediments, compared to active layer (horizon A). The mean C:N:S:P ratio decreased with depth, and varied from 5.4:0.2:6.6 in horizon A, 5.0:0.2:0.8 in horizon B, and 7.4:0.2:0.6 in horizon C. (9) The rate of metal accumulation in sediments (i.e., Cu, Ni or Co) differed significantly, compared to REE (apart from Ce and Sc) and U, which was caused by early diagenetic fractionation in oxic-suboxic conditions, and due to the presence of increased contents of clay minerals and barite. Ce, Sc, and U were indicators of metal acquisition fluctuations, mainly due to increased oxidation potential.
(10) The analyzed sediments from IOM H11 polymetallic nodules field generally contained low concentrations of REE and metals, such as Ni, Cu, or Co. Since the sediments were not significantly enriched in REE and other metals, the location shall not be considered a promising resource of REE in the near future; however, individual horizons may indicate increased contents of metals, expressed by increased contents of clays and diagenetic products (micronodules, barite, or zeolites). Proper geological prospection of CCFZ should include also this kind of data, which may be useful for future exploratory decision-making.
Supplementary Materials: The following are available online at http://www.mdpi.com/2075-163X/10/4/320/s1, Figure S1: Correlation matrix of sediment horizons A, B and C; Figure S2: Simplified maps of selected lithological parameters of individual horizons A, B and C; Table S1: Grain size data of analyzed sediments into individual sampling horizons A, B and C; Table S2: Geochemical data of sampling horizons A, B and C; Table S3: The SEM-EDX geochemical data of selected mineral components.