Ni-Co Mineralization in the Intex Laterite Deposit, Mindoro, Philippines

: The Intex laterite deposit in Mindoro, Philippines is derived from the weathering of the ultramaﬁc rocks under a tropical climate. This study investigates the several types of serpentines and the e ﬀ ect of the degree of chemical weathering of ultramaﬁc rocks and laterites on the enrichment of Ni in the deposit. The ﬁve types of serpentines are di ﬀ erentiated based on their textural features and Raman spectral data. Type I, type II, type III, and type IV serpentines contain a low amount of NiO (average 0.15 wt%), and their formation is linked to the previous exhumation of the ultramaﬁc body. Conversely, type V serpentines show the highest NiO contents (average 1.42 wt%) and have the composition of serpentine-like garnierites, indicating a supergene origin. In the limonite horizon, goethite is the main ore mineral and shows high NiO contents of up to 1.68 wt%, whereas the Mn-oxyhydroxides (i.e., asbolane and lithiophorite–asbolane intermediate) display substantial amounts of CoO (up to 11.3 wt%) and NiO (up to 15.6 wt%). The Ultramaﬁc Index of Alteration (UMIA) and Index of Lateritization (IOL) are used to characterize the di ﬀ erent stages of weathering of rocks and laterites. The calculated index values correspond to a less advanced stage of weathering of the Intex laterites compared with the Berong laterites. The Berong deposit is a Ni-Co laterite deposit in the Philippines, which is formed from the weathering of the serpentinized peridotite. The less extreme degree of weathering of the Intex laterites indicates less advanced leaching, and thereby the re-distribution of Ni, Si, and Mg from the limonite towards the saprolite horizon may have resulted in the poor precipitation of talc-like (kerolite-pimelite) and sepiolite-like (sepiolite-falcondoite) phases in the studied saprolite horizon. Nickel in the Intex deposit has undergone supergene enrichment similar to other humid tropical laterite deposits.


Introduction
Nickel laterite deposits are formed from chemical weathering of ultramafic rocks and contain a significant amount of Ni, and to some extent, Co and Sc [1][2][3][4]. Most Ni laterite deposits occur in the present humid tropics, and tectonically active collision zones, including New Caledonia, Indonesia, the Philippines, and Cuba, but some are situated in cratonic areas in Australia, Brazil, and West In northwestern Mindoro, the basement rocks are composed of metamorphic rocks and minor amounts of ophiolitic fragments of the Mangyan ophiolitic complex, which are designated as the Halcon Metamorphics [32,33]. The Halcon Metamorphics consist mainly of chlorite, graphite schist, quartz mica with phyllite, slate and amphibolites. This metamorphic complex was initially a mélange, which was subjected to regional metamorphism after the Cretaceous period [32]. In northwestern Mindoro, the basement rocks are composed of metamorphic rocks and minor amounts of ophiolitic fragments of the Mangyan ophiolitic complex, which are designated as the Halcon Metamorphics [32,33]. The Halcon Metamorphics consist mainly of chlorite, graphite schist, quartz mica with phyllite, slate and amphibolites. This metamorphic complex was initially a mélange, which was subjected to regional metamorphism after the Cretaceous period [32].
The Intex exploration project area lies in the Mangyan Ophiolitic Complex in the north-central part of the island, which is 40 km south of Calapan. A total of three laterite profiles, namely BB2515, PG1500, and BB2406, were selected for this study (Figure 1c). These profiles were chosen based on the availability of complete horizons (saprolite and limonite) and the location of the laterite profiles (topmost ridges). The Intex's concession area covers approximately 113 km 2 with an elevation that ranges from 135 m in the northeast section to 1460 m near the southwest section ( Figure 2).  The laterite profiles observed in the drill cores are divided from bottom to top into: (i) serpentinized ultramafic rocks, (ii) the saprolite horizon, and (iii) the limonite horizon. The bulk Fe concentration, texture and mineralogy of the rock and laterite were used to distinguish each horizon. The thickness of the laterite ranges 13-16 m. The ultramafic rocks in the studied cores are characterized by mm-wide serpentine veins. In this study, lherzolite (BB2515 core), clinopyroxenite (PG1500 core), and harzburgite-dunite bedrock (BB2406 core) are examined (Figure 3a-c).
concentration, texture and mineralogy of the rock and laterite were used to distinguish each horizon. The thickness of the laterite ranges 13-16 m. The ultramafic rocks in the studied cores are characterized by mm-wide serpentine veins. In this study, lherzolite (BB2515 core), clinopyroxenite (PG1500 core), and harzburgite-dunite bedrock (BB2406 core) are examined (Figure 3a-c).
Overlying the serpentinized bedrock is the saprolite horizon, which is generally yellow-brown, and porous. The saprolite horizon is well developed in all studied cores with thickness ranging from 3 to 8 m. This horizon contains a combination of earthy materials and coarse-grained to gravel-sized rock remnants (Figure 3d). Residual silica and Mn-oxyhydroxides often occur as coatings on the surface of moderately weathered rocks. The saprolite horizon derived from clinopyroxenite (PG1500) is marked by a thick layer of residual silica.
Approximately from 3 to 4.5 m of the limonite horizon is developed above the saprolite horizon. Irregular patches of residual silica are occasionally found on the upper section of the limonite horizon ( Figure 3e). Figure 3f displays an example of dark-orange-colored and friable limonite. Figure 3. Photos of (a) serpentinized lherzolite (BB2515 core), (b) harzburgite-dunite (BB2406 core), and (c) clinopyroxenite (PG1500 core), (d) earthy material including pebble-sized rock remnants (e) silica-bearing limonite sample from the limonite horizon, and (f) dark orange highly weathered materials.

Sampling and Analytical Methods
Samples from the bedrock, saprolite and limonite horizons were collected from the three drill cores mentioned above. These samples were air-dried at 20-30 °C for two weeks, then were quartered and powdered using mortar and pestle.
The pH measurements of 26 representative samples were conducted. Twenty grams of powdered sample and 20 mL of distilled water were transferred to a 50 mL container and were mixed. The mixed solution was constantly stirred for 30 minutes. The pH meter was calibrated using pH 4, 7, and 10 standard solutions under 20-25 °C temperature conditions. The pH meter was then dipped Figure 3. Photos of (a) serpentinized lherzolite (BB2515 core), (b) harzburgite-dunite (BB2406 core), and (c) clinopyroxenite (PG1500 core), (d) earthy material including pebble-sized rock remnants (e) silica-bearing limonite sample from the limonite horizon, and (f) dark orange highly weathered materials.
Overlying the serpentinized bedrock is the saprolite horizon, which is generally yellow-brown, and porous. The saprolite horizon is well developed in all studied cores with thickness ranging from 3 to 8 m. This horizon contains a combination of earthy materials and coarse-grained to gravel-sized rock remnants (Figure 3d). Residual silica and Mn-oxyhydroxides often occur as coatings on the surface of moderately weathered rocks. The saprolite horizon derived from clinopyroxenite (PG1500) is marked by a thick layer of residual silica.
Approximately from 3 to 4.5 m of the limonite horizon is developed above the saprolite horizon. Irregular patches of residual silica are occasionally found on the upper section of the limonite horizon ( Figure 3e). Figure 3f displays an example of dark-orange-colored and friable limonite.

Sampling and Analytical Methods
Samples from the bedrock, saprolite and limonite horizons were collected from the three drill cores mentioned above. These samples were air-dried at 20-30 • C for two weeks, then were quartered and powdered using mortar and pestle.
The pH measurements of 26 representative samples were conducted. Twenty grams of powdered sample and 20 mL of distilled water were transferred to a 50 mL container and were mixed. The mixed solution was constantly stirred for 30 minutes. The pH meter was calibrated using pH 4, 7, and 10 standard solutions under 20-25 • C temperature conditions. The pH meter was then dipped into the solution, and the sample pH to the nearest 0.01 pH unit was recorded. Lastly, the electrode was rinsed with tap water followed by distilled water.
Twenty polished thin sections and polished samples were prepared. The modal proportions of olivine, orthopyroxene, clinopyroxene, talc, and serpentine in the bedrock were determined by the point-counting method under an optical microscope. A total of 2500 points were covered for each polished thin section. The saprolite and limonite samples were impregnated with petropoxy resin prior to sectioning and polishing.
The bulk mineralogy of the samples was analyzed using X-ray Powder Diffraction (XRPD). The MultiFlex XRPD (Rigaku, Tokyo, Japan) with Cu Kα radiation source was operated at 30 kV, 10 mA, step size of 0.02 • and a scan step of 20 • per minute. The XRPD machine is available at the Graduate School of International Resource Sciences, Akita University, Japan. Mineral identification was accomplished using the COD reference database of MATCH! software-based on 'figure-of-merit" values and visual inspection relative to the experimental diffraction pattern.
The polymorphs of serpentine were distinguished using an inVia Raman microscope (Renishaw, Gloucestershire, United Kingdom) of Akita University. This instrument is equipped with a 100 mW 532 nm frequency-doubled Nd: YAG laser and a CCD detector. A total of 1800 lines/mm grating was used to disperse the signal onto the CCD detector. Before the analysis of polished thin sections, the analyzer was calibrated using the Si-Au standard. A range of from ten to fifty percent laser power was used, and the minerals were observed under a 50× objective lens. Both the spectra from low wavenumbers (100-500 cm −1 ) and high wavenumbers (3600-4000 cm −1 ) were collected for mineral identification. The background fluorescence and noise were removed using the WiRE TM software (Renishaw, Gloucestershire, United Kingdom). The Raman signatures of the serpentine polymorphs of this study were compared to the previous results [20,37,38].
The whole-rock composition of representative samples was obtained by X-ray Fluorescence (XRF) spectrometer (Rigaku ZSX Primus III+, Tokyo, Japan). Forty powdered samples were oven-dried at 105 • C in an oven for over 30 minutes. The mixture of 0.5 g sample and di-lithium tetraborate was fused at 1250 • C in a Pt crucible using a high-frequency fusion instrument (HERZOG HAG-M-HF, Germany). Then this mixture was cooled on a Pt disk, and the fused glass beads were analyzed using the XRF spectrometer. A 50 kV voltage and a current of 50 mA was used. Two calibration curves were prepared using a different set of OREAS reference standards for SiO 2 , Al 2 O 3 , P 2 O 5 , TiO 2 , Cr 2 O 3 , MnO, Fe 2 O 3 , Co 2 O 3 , and NiO, whereas GSJ standards for Na 2 O, MgO, K 2 O, and CaO. Five international standards, including JP-A (peridotite), JB-1b (basalt), JG-3 (granodiorite), OREAS 401 (Fe ore), OREAS 180 and OREAS 184 (Ni laterite ore) were used to evaluate the accuracy of the analytical results. The loss-on-ignition (LOI) of each representative sample was obtained. Both XRF and LOI were done at GSJ, AIST in Tsukuba. was calculated using Bragg's equation (nλ = 2dsinθ), where n is a positive integer (first order Bragg diffraction peak), and lambda λ is the wavelength of the incident wave. Serpentine, olivine, pyroxene are the dominant minerals in the bedrock with a trace amount of chromite ( Figure 4). The strong reflection at 7.25 Å and weaker reflections at 4.60 and 3.60 Å are characteristics of serpentine. In the saprolite horizon, serpentine is the major mineral, whereas chromite, goethite, talc, quartz, actinolite, relict olivine, and pyroxene occur as accessory constituents (Figure 4). The minor peaks at 3.12 and 8.40 Å belong to actinolite (Figure 5a). The limonite horizon consists mainly of goethite. Hematite, talc, chromite, magnetite, asbolane, and quartz occur in minor to trace amounts. XRPD analysis of the limonite samples shows the occurrence of talc of which reflections are at 9.36 Å (d 001 ), 4.67 Å (d 002 ) and 3.12 Å (d 003 ) (Figure 5a). The 9.44 Å and 4.74 Å peaks belong to asbolane (Figure 5b).

XRPD Analysis
Minerals 2020, 10, x FOR PEER REVIEW 7 of 33 strong reflection at 7.25 Å and weaker reflections at 4.60 and 3.60 Å are characteristics of serpentine.
A network of serpentine cuts the primary minerals in all the studied bedrock. The serpentine veins contain discontinuous strings of magnetite ( Figure 6a). The peridotite bedrock from BB2515 and BB2406 cores are characterized by three types of serpentine veins including mesh-textured type I and type II veins and the interlocking-textured type III veins. Fine-to coarse-grained magnetite outlines the core of type II veins, whereas the rim is free from magnetite ( Figure 6a). The type III veins are wider, generally hundreds of micrometers to a millimeter in width. Talc has a characteristically high birefringence under cross-polarized light. Figure 6b shows that fine-grained talc replaces type III serpentines. Microscopic observations show that talc is more dominant in lherzolite in contrast to harzburgite-dunite bedrock. Chromite occurs in various shapes and sizes but is typically subhedral in form (Figure 6b).
A network of serpentine cuts the primary minerals in all the studied bedrock. The serpentine veins contain discontinuous strings of magnetite ( Figure 6a). The peridotite bedrock from BB2515 and BB2406 cores are characterized by three types of serpentine veins including mesh-textured type I and type II veins and the interlocking-textured type III veins. Fine-to coarse-grained magnetite outlines the core of type II veins, whereas the rim is free from magnetite ( Figure 6a). The type III veins are wider, generally hundreds of micrometers to a millimeter in width. Talc has a characteristically high birefringence under cross-polarized light. Figure 6b shows that fine-grained talc replaces type III serpentines. Microscopic observations show that talc is more dominant in lherzolite in contrast to harzburgite-dunite bedrock. Chromite occurs in various shapes and sizes but is typically subhedral in form ( Figure 6b).
Three types of serpentine veins are identified in the saprock derived from lherzolite bedrock ( Figure 6c). The textural features of these veins are analogous to the previous veins identified in the bedrock. Type I veins contain disseminated magnetite and pseudomorph the former primary olivine and pyroxene. Type II veins have distinct magnetite rich core and cut through type I veins. Type III veins are characterized by interlocking texture (Figure 6c). Similarly, the saprock derived from harzburgite-dunite bedrock shows type I to type III serpentine veins, and these are subsequently cut by yellow-orange, discontinuous type IV veins, which are often associated with magnetite ( Figure 6d). The saprock developed above clinopyroxenite is marked by type I and type V veins. Type I veins are characterized by interpenetrating texture (Figure 6e) and are cut by type V serpentine veins (Figure 6f). Hematite is widely distributed within type V veins (Figure 6f). Minerals 2020, 10, x FOR PEER REVIEW 9 of 33 Figure 6. Photomicrographs of (a,b) type I, II and III serpentine veins cutting primary olivine, pyroxene, chromite, and Fe-oxide in lherzolite (BB2515 core); serpentine veins in the saprock developed above (c) lherzolite (BB2515 core), (d) harzburgite-dunite (BB2406 core), and (e,f) clinopyroxenite (PG1500 core). Ol-olivine, Px-pyroxene, Srp-serpentine, Tlc-talc, Chrchromite, Gth-goethite.
Three types of serpentine veins are identified in the saprock derived from lherzolite bedrock ( Figure 6c). The textural features of these veins are analogous to the previous veins identified in the bedrock. Type I veins contain disseminated magnetite and pseudomorph the former primary olivine and pyroxene. Type II veins have distinct magnetite rich core and cut through type I veins. Type III veins are characterized by interlocking texture (Figure 6c). Similarly, the saprock derived from harzburgite-dunite bedrock shows type I to type III serpentine veins, and these are subsequently cut by yellow-orange, discontinuous type IV veins, which are often associated with magnetite ( Figure  6d). The saprock developed above clinopyroxenite is marked by type I and type V veins. Type I veins are characterized by interpenetrating texture (Figure 6e) and are cut by type V serpentine veins ( Figure 6f). Hematite is widely distributed within type V veins (Figure 6f).  . Photomicrographs of (a,b) type I, II and III serpentine veins cutting primary olivine, pyroxene, chromite, and Fe-oxide in lherzolite (BB2515 core); serpentine veins in the saprock developed above (c) lherzolite (BB2515 core), (d) harzburgite-dunite (BB2406 core), and (e,f) clinopyroxenite (PG1500 core). Ol-olivine, Px-pyroxene, Srp-serpentine, Tlc-talc, Chr-chromite, Gth-goethite. The saprolite horizon developed above lherzolite and harzburgite-dunite is characterized by the frequent presence of type I, type II-rim, type II-core, and type III serpentines with the addition of type IV serpentines ( Figure 8). The main peaks of type I serpentines are positioned at 228, 383, and 688 cm −1 . The extra reflections at 827 and 857 cm −1 correspond to the relict phase of olivine. The high-frequency domains reveal sharp peaks at 3679, 3682, 3683 and 3684 cm −1 . Both the low-frequency and high-frequency domains of type I to type IV serpentines in the saprock derived from harzburgite-dunite match the signature of lizardite. However, the Raman peaks of type I in the saprock derived from clinopyroxenite belong to antigorite. Here, the low-frequency domains show intense peaks at 230, 375, and 684 cm −1 , whereas, in the high-frequency domain, the strong peak is at 3667 cm −1 (Figure 9). Conversely, the Raman bands of type V serpentines in the saprock developed above clinopyroxenite are identified as chrysotile ( Figure 9). The Raman signatures of lizardite (3679-3684 cm −1 ) are differentiated from antigorite (3667 cm −1 ) and chrysotile (3694 cm −1 ) based on the strong peaks in the high-frequency domain. The saprolite horizon developed above lherzolite and harzburgite-dunite is characterized by the frequent presence of type I, type II-rim, type II-core, and type III serpentines with the addition of type IV serpentines ( Figure 8). The main peaks of type I serpentines are positioned at 228, 383, and 688 cm -1 . The extra reflections at 827 and 857 cm -1 correspond to the relict phase of olivine. The highfrequency domains reveal sharp peaks at 3679, 3682, 3683 and 3684 cm -1 . Both the low-frequency and high-frequency domains of type I to type IV serpentines in the saprock derived from harzburgitedunite match the signature of lizardite. However, the Raman peaks of type I in the saprock derived from clinopyroxenite belong to antigorite. Here, the low-frequency domains show intense peaks at 230, 375, and 684 cm -1 , whereas, in the high-frequency domain, the strong peak is at 3667 cm -1 ( Figure  9). Conversely, the Raman bands of type V serpentines in the saprock developed above clinopyroxenite are identified as chrysotile ( Figure 9). The Raman signatures of lizardite (3679-3684 cm -1 ) are differentiated from antigorite (3667 cm -1 ) and chrysotile (3694 cm -1 ) based on the strong peaks in the high-frequency domain.   . Raman signatures of type I, type II, type III and type IV vein serpentines identified in the saprock derived from harzburgite-dunite (BB2406 core). Red dashed lines indicate the Raman bands from previous work [21].

Mineral Chemistry
The bedrock samples show that the highest NiO concentration is measured in primary olivine (average 0.37 wt%; 0.01 apfu Ni) with a considerable amount of FeO (average 8.42 wt%) (Figure 10a). Orthopyroxene and clinopyroxene are marked by relatively high FeO concentrations (average 5.56 wt%, average 1.78 wt%) ( Table 1). Talc commonly occurs as fine aggregates in the bedrock and it contains a substantial amount of FeO (average 1.75 wt%) and Al2O3 (average 1.24 wt%), but with low NiO concentration (average 0.07 wt%). The average structural formula of talc is Mg2.93Si3.89 O10(OH)2.

Mineral Chemistry
The bedrock samples show that the highest NiO concentration is measured in primary olivine (average 0.37 wt%; 0.01 apfu Ni) with a considerable amount of FeO (average 8.42 wt%) (Figure 10a). Orthopyroxene and clinopyroxene are marked by relatively high FeO concentrations (average 5.56 wt%, average 1.78 wt%) ( Table 1). Talc commonly occurs as fine aggregates in the bedrock and it contains a substantial amount of FeO (average 1.75 wt%) and Al 2 O 3 (average 1.24 wt%), but with low NiO concentration (average 0.07 wt%). The average structural formula of talc is Mg 2.93 Si 3.89 O 10 (OH) 2 .  In the saprock developed above lherzolite and harzburgite-dunite, the FeO content of type I, type II-rim and type II-core serpentines (average 5.62 wt%, average 7.01 wt%, average 7.75 wt%) continuously increases (Tables 3 and 4). The FeO concentration of type III serpentines (average 6.42 wt%) drops in the saprock. However, the amount of FeO in type IV serpentines (average 9.65 wt%) increases again and finally decreases in type V serpentines (average 5.47 wt%). Figure 11a,b show that the Fe/(Fe + Mg + Ni) ratio increases from type I to type II serpentines and decreases in type III serpentines, but rises again in type IV serpentines. Finally, the Fe/(Fe + Mg + Ni) ratio declines in type V serpentines (Figure 11c). The MgO concentration from type I to type II serpentines (average 32.2 wt%, average 33.68 wt%, average 33.09 wt%) increases, and subsequently decreases in type III and type IV serpentines (average 31.06 wt%, average 29.84 wt%). A similar trend is observed in Mg/(Mg + Fe + Ni) ratio from type I to type II serpentines, however, there is a significant decrease in the Mg/(Mg + Fe + Ni) ratio of type III and type IV serpentines (Figure 11b). The saprock samples derived from lherzolite and harzburgite-dunite contain a low amount of NiO in type I serpentines (average 0.31 wt%), type II-rim (average 0.25 wt%), type II-core (average 0.26 wt%), type III serpentines (average 0.07 wt%) and type IV serpentines (average 0.11 wt%). A significant amount of NiO is The FeO content of type I, type II-rim and type II-core serpentines (average 6.30 wt%, average 5.85 wt%, average 8.17 wt%) is higher compared with type III serpentines (average 5.13 wt%) in the lherzolite and harzburgite-dunite bedrock ( Table 2). The MgO concentration of type I and type II-rim serpentines (average 37.56 wt%, average 38.37 wt%) is higher than type II-core and type III serpentines (average 36.48 wt%, average 36.26 wt%) in either bedrock. The sudden decrease in the Mg/(Mg + Fe + Ni) ratio from type II-rim to type II-core and type III serpentines is clearly shown in Figure 10a. The NiO contents of type I and type II serpentines in the bedrock are similar (average 0.22 wt%, 0.009 apfu), but type III serpentines are distinctively lower (0.06 wt%, 0.002 apfu) ( Table 2). The Ni/(Ni + Mg + Fe) ratio from type I to type III serpentines decreases in the bedrock (Figure 10a,b). In the saprock developed above lherzolite and harzburgite-dunite, the FeO content of type I, type II-rim and type II-core serpentines (average 5.62 wt%, average 7.01 wt%, average 7.75 wt%) continuously increases (Tables 3 and 4). The FeO concentration of type III serpentines (average 6.42 wt%) drops in the saprock. However, the amount of FeO in type IV serpentines (average 9.65 wt%) increases again and finally decreases in type V serpentines (average 5.47 wt%). Figure 11a,b show that the Fe/(Fe + Mg + Ni) ratio increases from type I to type II serpentines and decreases in type III serpentines, but rises again in type IV serpentines. Finally, the Fe/(Fe + Mg + Ni) ratio declines in type V serpentines (Figure 11c). The MgO concentration from type I to type II serpentines (average 32.2 wt%, average 33.68 wt%, average 33.09 wt%) increases, and subsequently decreases in type III and type IV serpentines (average 31.06 wt%, average 29.84 wt%). A similar trend is observed in Mg/(Mg + Fe + Ni) ratio from type I to type II serpentines, however, there is a significant decrease in the Mg/(Mg + Fe + Ni) ratio of type III and type IV serpentines (Figure 11b). The saprock samples derived from lherzolite and harzburgite-dunite contain a low amount of NiO in type I serpentines (average 0.31 wt%), type II-rim (average 0.25 wt%), type II-core (average 0.26 wt%), type III serpentines (average 0.07 wt%) and type IV serpentines (average 0.11 wt%). A significant amount of NiO is observed in type V serpentines (average 1.42 wt%), particularly in the saprock derived from clinopyroxenite. Among the different types of serpentine in the saprock, a high Ni/(Ni + Mg + Fe) ratio is observed in type V serpentines (Figure 11c). The chemical composition of type V serpentines observed in the saprock plot near the serpentine-like garnierite of the Si-Mg(+Fe)-Ni ternary diagram ( Figure 12). The average O/T ratio (Mg + Fe + Ni)/Si) of type V serpentines is 0.94, which is less than the ideal value (O/T = 1.5) of the serpentine group minerals.    Goethite contains a significant amount of Al2O3 (average 6.63 wt%), NiO (average 0.77 wt%), MnO (average 1.09wt%) and CoO (average 0.27 wt%) ( Table 5). In Figure 13a

pH, Petrographic and Whole-Rock Geochemical Analysis
Figures 15-17 illustrate the relative amount of olivine, variations in pH and elements in representative bedrock, saprolite, and limonite samples. The pH of these samples is between 6.14 and 8.75. A pH gradient displays the shift from alkaline condition (pH 8.75) in the bedrock to neutral condition (pH 7.32) in the saprolite horizon to mildly acidic conditions (pH 6.14) in the limonite horizon.

pH, Petrographic and Whole-Rock Geochemical Analysis
Figures 15-17 illustrate the relative amount of olivine, variations in pH and elements in representative bedrock, saprolite, and limonite samples. The pH of these samples is between 6.14 and 8.75. A pH gradient displays the shift from alkaline condition (pH 8.75) in the bedrock to neutral condition (pH 7.32) in the saprolite horizon to mildly acidic conditions (pH 6.14) in the limonite horizon.

pH, Petrographic and Whole-Rock Geochemical Analysis
Figures 15-17 illustrate the relative amount of olivine, variations in pH and elements in representative bedrock, saprolite, and limonite samples. The pH of these samples is between 6.14 and 8.75. A pH gradient displays the shift from alkaline condition (pH 8.75) in the bedrock to neutral condition (pH 7.32) in the saprolite horizon to mildly acidic conditions (pH 6.14) in the limonite horizon.    The saprolite horizon is marked by a high NiO concentration, which reaches up to 2.15 wt%. The bedrock shows low CoO and MnO contents (0.01 wt%, 0.07 wt%), whereas significant amounts of these elements are found in the limonite horizon (up to 0.19 wt%, 1.15 wt%). The concentrations of TiO 2 , K 2 O, CaO, and P 2 O 5 in the bedrock are either low or below the detection limits. Conversely, the limonite horizon contains a considerable amount of TiO 2 and CaO (up to 0.35 wt%, 1.15 wt%).

Mineralogical Evolution of the Laterite Profiles
The NiO concentration of olivine (0.37 wt%), orthopyroxene (0.07 wt%), clinopyroxene (0.04 wt%), and talc (0.07 wt%) ( Table 1) indicate that olivine is the major source of Ni in the saprolite and limonite horizons. The initial serpentinization of peridotite and pyroxenite results in the formation of type I serpentines. Continuous serpentinization leads to the formation of type II-rim serpentine veins, which is followed by type II-core and later by type III veins in the studied bedrock ( Figure 18). This sequence is identical in the bedrock and saprock, suggesting a similar generation of serpentinization.

Mineralogical Evolution of the Laterite Profiles
The NiO concentration of olivine (0.37 wt%), orthopyroxene (0.07 wt%), clinopyroxene (0.04 wt%), and talc (0.07 wt%) ( Table 1) indicate that olivine is the major source of Ni in the saprolite and limonite horizons. The initial serpentinization of peridotite and pyroxenite results in the formation of type I serpentines. Continuous serpentinization leads to the formation of type II-rim serpentine veins, which is followed by type II-core and later by type III veins in the studied bedrock ( Figure 18). This sequence is identical in the bedrock and saprock, suggesting a similar generation of serpentinization. The Raman characterization of type I, type II, and type III serpentines in the lherzolite and harzburgite-mdunite identified the types as lizardite, whereas type I serpentines in the clinopyroxenite were identified as antigorite. The serpentine variety can be explained by the difference in the pressure and temperature conditions to which they were subjected. Lizardite and chrysotile form predominantly in a low-temperature (<300 °C)-pressure condition, whereas antigorite forms in a high-temperature (>320 °C)-pressure condition [40,41]. Type I to type III serpentines found in the ultramafic bedrock are of hydrothermal origin, which is formed before its settlement and exposure on the surface. Although we have not confirmed the replacement texture of lizardite by antigorite, the formation of lizardite in type I veins can be explained by the reaction of olivine and water (Equation (1)), in addition to the development of magnetite after the breakdown of brucite (Equation (2)) and serpentine (Equation (3) The Raman characterization of type I, type II, and type III serpentines in the lherzolite and harzburgite-mdunite identified the types as lizardite, whereas type I serpentines in the clinopyroxenite were identified as antigorite. The serpentine variety can be explained by the difference in the pressure and temperature conditions to which they were subjected. Lizardite and chrysotile form predominantly in a low-temperature (<300 • C)-pressure condition, whereas antigorite forms in a high-temperature (>320 • C)-pressure condition [40,41]. Type I to type III serpentines found in the ultramafic bedrock are of hydrothermal origin, which is formed before its settlement and exposure on the surface. Although we have not confirmed the replacement texture of lizardite by antigorite, the formation of lizardite in type I veins can be explained by the reaction of olivine and water (Equation (1)), in addition to the development of magnetite after the breakdown of brucite (Equation (2)) and serpentine (Equation (3) Further reaction of silica-rich fluid with brucite leads to the formation of type II lizardite. The absence of brucite in the samples may be attributed to the dissolution of brucite during the initial stages of serpentinization. The iron from the rim of type II serpentines is consumed to precipitate magnetite in the core of type II lizardite. The depletion of Ni and Mg in type II-core suggests the removal of these elements from the core of type II lizardite. The transformation from mesh-textured type I and type II veins to the interlocking textured type III veins is due to the change in the temperature or the composition of the fluid, which leads to the recrystallization of serpentines [45].
The NiO content of type III lizardite in the bedrock is lower than type I and type II lizardite indicating a local redistribution of the element in the serpentines. It is possible that this element was transported with the serpentinizing fluid and homogenizes in the late-stage type serpentines. Type IV serpentines in the saprock are typically associated with magnetite and contain low amount of NiO (average 0.11 wt%). Earlier work reported that magnetite is formed between 200 and 300 • C during serpentinization [46]. The composition of type IV serpentines and conditions related to its formation, suggest that these serpentines are also formed prior to the exhumation of the ultramafic body. In contrast, type V serpentines show the highest NiO content (average 1.42 wt%). These serpentines are comparable to serpentine-like phases reported by previous works, which are more likely to be formed at low-temperature conditions [11,20,47].
During progressive weathering, Ni is leached from the limonite horizon and then transported downwards to the saprolite horizon. The leached Ni is accommodated in type V serpentines owing to the increased amount of Ni in these serpentines [15,48]. Therefore, the composition of type V serpentines indicates that it precipitated last in the paragenetic sequence. Despite type V serpentines only occuring in the saprock derived from clinopyroxenite, we posit that the enrichment of Ni in the saprolite horizon above lherzolite and harzburgite-dunite is contributed to by other minerals including goethite and talc.
Observations under the microscope show that pyroxene crystals are not only altered to serpentine but also talc. The hydration of orthopyroxene-bearing rock primarily produces talc and can be explained by the reaction below [44].
The replacement of serpentine by talc is common in the studied bedrock. The prolonged interaction of serpentine with fluid leads to the development of talc. Since carbonates (e.g., magnesite) were not detected in the samples, this observation implies that carbonatization is not responsible for the formation of talc. Thus, talc formation (Equation (5)) is possible if the silica activity of the fluid is increased or if the water activity is decreased [49].
Talc is typically fine-grained in the bedrock samples. Based on XRPD data, talc is also present in the saprolite and limonite samples. The accumulation of talc in the weathered horizon is most likely due to residual enrichment under the supergene process. In this horizon, the pH is between 6.14 and 6.82, indicating this is the right condition for the stability of talc. A number of studies have reported that talc could form under near-neutral conditions [2,9] and is stable under low-temperature conditions [50].
A minor amount of goethite is present in the saprolite horizon with pH ranges from 7.53 to 8.13. However, at pH values between 6.24 and 6.46, there is an increased amount of goethite in the limonite horizon. Goethite is the main host of Ni in the limonite horizon, which contains a significant amount of NiO of up to 1.68 wt%. Hematite is also found in this horizon, with more hematite being formed when the pH is above pH 6.46. This is consistent with the fact that hematite is more stable at a pH closer to neutral, which is in contrast to goethite. The transformation of goethite to hematite depends mainly on temperature, the composition of goethite and the physico-chemical parameters of the solution [51,52].
Asbolane and lithiophorite-asbolane intermediate are the typical Co-bearing Mn-oxyhydroxides in the laterites from the Intex deposit in Mindoro, Philippines. Based on the XRF results, the trends of Co and Mn are similar throughout the three profiles, suggesting the strong association of Co with Mn oxyhydroxides minerals. The occurrence of these minerals is linked to the oxidation of other Mn-oxyhydroxide minerals such as buserite, cryptomelane, birnessite, hollandite, and todorokite [53,54]. However, we currently do not have definitive evidence in which primary minerals affect the formation of asbolane and lithiophorite-asbolane intermediate.
The mineral chemistry data show that both minerals contain significant amounts of CoO (up to 11.3 wt%) and NiO (up to 15.6 wt%). The sorption of Ni by Mn oxyhydroxides depends on structural and physicochemical parameters [55], and the presence of Al in the solution at a pH above 6 [56]. In this study, asbolane was found in abundance in the limonite horizon with a pH value above 7.29, whereas a lithiophorite-asbolane intermediate was found around pH 6.32. The results suggest that lithiophorite-asbolane intermediates form at approximately around pH 6 and asbolane is precipitated at higher pH (pH above 7). Asbolane shows a lower Co/Ni ratio (0.32) in contrast to the lithiophorite-asbolane intermediate, which has a higher Co/Ni ratio of 3.35. Taking into account the difference in pH and Co/Ni ratio of these minerals, these results, therefore, show that under slightly acidic conditions (pH 6), Co is more closely associated with a lithiophorite-asbolane intermediate.
The limonite horizon exhibits abundant silica, mainly consisting of quartz, particularly in the limonite derived from clinopyroxenite. Since pyroxenes have 15% more SiO 2 than olivine, this indicates a higher amount of silica present in pyroxene-dominated rocks. The precipitation of silica is generally attributed to the poorly drained environment. Under these environmental conditions, silica may not be fully leached, resulting in its accumulation in the upper horizon [2].

Degree of Weathering on Ultramafic Rocks and Laterites
Two weathering indexes, namely the Ultramafic Index of Alteration (UMIA) [13,57] and the Index of Lateritization (IOL) [57,58] are utilized to determine the degree of chemical weathering of ultramafic rocks and laterites in the Intex deposit. Then, the index values of this study are compared with the results from Berong deposit in Palawan, Philippines. Similarly, the Berong laterite ores are a product of the intensive weathering of ultramafic rocks under humid tropical conditions [59].
The Berong deposit in Palawan, Philippines is also divided from bottom to top into: (i) bedrock, (ii) saprolite and (iii) limonite horizon. The different horizons are classified based on Fe concentration, texture and mineralogy of the rock and laterite samples [59]. Both the studied samples from Berong and Intex deposits were acquired from topmost ridges and on uneroded areas. The bedrock in the Berong deposit is mainly peridotite (i.e., harzbugite and dunite). The summer rainfall in these two deposits is between 900 and 1800 mm [2]. The major differences between the two deposits are the ore minerals in the saprolite, bulk Ni concentration in the saprolite horizon and thickness of the weathered horizons. The saprolite horizon of the Berong deposit shows higher Ni contents of up to 6.11 wt%, and the main ore minerals are talc-like (kerolite-pimelite) and sepiolite-like (sepiolite-falcondoite) phases. The profiles in the Berong deposit have thinner saprolite (2 to 5 m) and thicker limonite (3-15 m).
The UMIA values are calculated using the equation below and are expressed in molar ratios [55]. The UMIA values of the bedrock samples from Intex deposit range from 3 to 5, the saprolite UMIA = 100 × ((Al 2 O 3 + Fe 2 O 3(T) )/(SiO 2 + MgO + Al 2 O 3 + Fe 2 O 3(T) )) (6) from 3 to 14, and the limonite from 16 to 82. The low UMIA values of the bedrock and saprolite indicate that these are not intensely altered. In Figure 19a, the bedrock and saprolite have high amounts of MgO and SiO 2 . However, as weathering progresses, Mg and Si are leached from the bedrock and saprolite, resulting in an increased Fe 2 O 3 . The sample acquired from the transition boundary between the saprolite and limonite horizons exhibits a relatively high UMIA value of 29 compared to the bedrock and saprolite (Figure 19a). On the other hand, the limonite is characterized by higher UMIA values (more than 50), which plot near the apex of Al 2 O 3 and Fe 2 O 3 . This observation is consistent with the fact that limonite from the Intex deposit contains high amounts of Fe 2 O 3, which indicates an abundance of Fe-oxyhydroxides (e.g., goethite and hematite).
Minerals 2020, 10, x FOR PEER REVIEW 28 of 33 is consistent with the fact that limonite from the Intex deposit contains high amounts of Fe2O3, which indicates an abundance of Fe-oxyhydroxides (e.g., goethite and hematite). The UMIA values of the bedrock and saprolite from Intex deposit are comparable to that of the Berong deposit in Palawan, Philippines. Based on Figure 19a, the two deposits have a similar weathering trend. However, the limonite samples from the Berong deposit show the highest UMIA values, suggesting that these samples are strongly altered.
The different stages of advanced chemical weathering are not sufficiently quantified if only UMIA is utilized. To supplement these results, IOL is applied. This index is a quantitative approach to determine the stages of advanced chemical weathering (weakly, moderately, and strongly), and is typically expressed in wt% [53]. IOL = 100 × ((Al2O3 + Fe2O3(T)) / (SiO2 + Al2O3 + Fe2O3(T))) The IOL values of the bedrock are in the range of 14 to 19, and the saprolite up to 17. However, the limonite from Intex deposit exhibits higher IOL values, reaching up to 94 (Figure 19b). Earlier studies reported that unweathered ultramafic rocks have IOL values of less than 40 [46]. Even though the IOL values of the saprolite are low, weak weathering was observed under the microscope. Conversely, the sample from the transition boundary has a higher IOL value (46), corresponding to the point in the middle section of the SiO2-Al2O3-Fe2O3 (SAF) ternary diagram, which indicates a significant loss of silica ( Figure 19b). As lateritization progresses, more silica is leached, resulting in the relative enrichment of Fe. Samples from the saprolite and limonite horizons show an apparent increase in Ni (Figure 19c).
The calculated IOL values of the Intex profiles correspond to a less advanced stage of weathering or moderately to strongly "laterized" profiles, which leads to the development of thicker saprolite (3-8 m) and thinner limonite (3-4.5 m). In contrast, the profiles in the Berong deposit experienced a more advanced stage of weathering or strongly "laterized" profiles and subsequently yielded thinner saprolite (2-5 m) and thicker limonite (3-15 m). Concerning the Ni contents between the two deposits, the Intex deposit exhibit lower bulk Ni in the saprolite (up to 1.69 wt%) and limonite (up to 0.79 wt%) compared with the Berong deposit (up to 6.11 wt%; up to 0.90 wt%) (Figure 19c). Thus, the difference in Ni concentration between the Intex and Berong deposits may be the result of different degrees of The UMIA values of the bedrock and saprolite from Intex deposit are comparable to that of the Berong deposit in Palawan, Philippines. Based on Figure 19a, the two deposits have a similar weathering trend. However, the limonite samples from the Berong deposit show the highest UMIA values, suggesting that these samples are strongly altered.
The different stages of advanced chemical weathering are not sufficiently quantified if only UMIA is utilized. To supplement these results, IOL is applied. This index is a quantitative approach to determine the stages of advanced chemical weathering (weakly, moderately, and strongly), and is typically expressed in wt% [53].
The IOL values of the bedrock are in the range of 14 to 19, and the saprolite up to 17. However, the limonite from Intex deposit exhibits higher IOL values, reaching up to 94 (Figure 19b). Earlier studies reported that unweathered ultramafic rocks have IOL values of less than 40 [46]. Even though the IOL values of the saprolite are low, weak weathering was observed under the microscope. Conversely, the sample from the transition boundary has a higher IOL value (46), corresponding to the point in the middle section of the SiO 2 -Al 2 O 3 -Fe 2 O 3 (SAF) ternary diagram, which indicates a significant loss of silica ( Figure 19b). As lateritization progresses, more silica is leached, resulting in the relative enrichment of Fe. Samples from the saprolite and limonite horizons show an apparent increase in Ni (Figure 19c).
The calculated IOL values of the Intex profiles correspond to a less advanced stage of weathering or moderately to strongly "laterized" profiles, which leads to the development of thicker saprolite (3-8 m) and thinner limonite (3-4.5 m). In contrast, the profiles in the Berong deposit experienced a more advanced stage of weathering or strongly "laterized" profiles and subsequently yielded thinner saprolite (2-5 m) and thicker limonite (3-15 m). Concerning the Ni contents between the two deposits, the Intex deposit exhibit lower bulk Ni in the saprolite (up to 1.69 wt%) and limonite (up to 0.79 wt%) compared with the Berong deposit (up to 6.11 wt%; up to 0.90 wt%) (Figure 19c). Thus, the difference in Ni concentration between the Intex and Berong deposits may be the result of different degrees of weathering of the laterites.
Since the limonite from the Intex deposit experienced a less advanced degree of weathering, this affected the leaching and re-mobilization of Ni from the limonite horizon towards the saprolite horizon. The weathering solution is not supersaturated with Ni, Si, and Mg, which may have resulted in the poor precipitation of talc-like (kerolite-pimelite) or sepiolite-like (sepiolite-falcondoite) phases in the studied saprolite horizon. Nevertheless, the combined mineralogical and geochemical data suggest that Ni in the Intex deposit has undergone supergene enrichment similar to other humid tropical laterite deposits in New Caledonia, the Caribbean, and northeastern Australia [3,11,13,17].

Conclusions
The weathering of the serpentinized ultramafic rocks resulted in the formation of the Intex laterite deposit. In the bedrock, olivine is the main source of ore in the saprolite and limonite horizons. The early stages of serpentinization lead to the development of type I, type II, type III, and type IV serpentines. The results of this study show that these serpentines are of hydrothermal origin. The late-stage type V serpentines cut the early-stage type I to type IV serpentines. Type V serpentines are the serpentine-like garnierites and display the highest amount of NiO (average 1.42 wt%).
The UMIA and IOL values of the Intex laterites are in agreement with the less advanced stage of weathering compared with Berong laterites. The difference in bulk Ni concentration between the Intex and Berong deposits may be the result of different degrees of weathering of the laterites. The less extreme degree of weathering of Intex profiles indicates less advanced leaching, and thus the re-distribution of Ni, Si, and Mg from the limonite towards the saprolite horizon may have resulted in the poor precipitation of talc-like (kerolite-pimelite) and sepiolite-like (sepiolite-falcondoite) phases in the studied saprolite horizon.
Supergene enrichment of Ni occurred in the Intex laterite deposit, which is comparable to the Ni laterite deposits in New Caledonia, the Caribbean, and northeastern Australia. The main difference between the Intex deposit and other tropical laterite deposits is the composition of garnierites. In this study, garnierites consist mainly of serpentine-like minerals, whereas talc-like and sepiolite-like phases are often found in other laterite deposits. Another similarity of the studied deposit with other classic deposits is the occurrence of goethite and Mn-oxyhydroxides (i.e., asbolane and lithiophorite-asbolane intermediate) in the limonite horizon. Nickel is mainly hosted by goethite, and Mn-oxyhydroxides contain significant amounts of CoO (up to 11.3 wt%) and NiO (up to 15.6 wt%).
Author Contributions: C.A.J.T. acquired the samples, performed the analyses, prepared, and revised the manuscript. Y.W. supervised, visualized and contributed significantly to interpret the data and review the manuscript. K.S. supervised and assisted in performing the XRF and EPMA analyses. T.E. supervised and helped obtain good quality Raman data. C.A. acquired the resources needed for the fieldwork. C.F. helped conceptualize the research which resulted in the preparation of the manuscript. All authors have read and agreed to the published version of the manuscript.
Funding: This research received no external funding.