Pegmatites are coarse to very coarse-grained igneous rocks. Indeed, most pegmatites have granitic composition. Pegmatite hosts variety of minerals along with common minerals such as, lithium aluminosilicates (spodumene, petalite, lithium), tourmaline, garnets, beryl, pollucite; phosphates (monazite, amblygonite, lithiophyllite, topaz); oxides (cassiterite, columbite-tantalite, rutile, uranitite, zircon, corundum) . Pegmatite contains elements such as Li, Rb, Cs, Be, Ga, Sc, Y, REE, Sn, Nb, Ta, U, Th, Zr and Hf. Apart from these rare minerals, industrial minerals and gemstones are valuable in pegmatite . Granite-pegmatites are sources of rare metals and REEs (RMRE), which is commercially exploitable and economically viable  - .
Granitic pegmatites represent very unusual magmas, which constitute considerable reservoirs of rare elements  . However, the genesis and mineralization of Li-Cs-Ta (LCT) pegmatites  are still being debated. Processes leading to the genesis of pegmatite are defined at two distinct geological scales: 1) a crustal scale where the pegmatite-forming melt is produced; and 2) the scale of the pegmatite body, where internal physico-chemical processes lead to localized concentrations of rare elements such as Li, Be, Cs, and Ta. Most LCT-type pegmatites are interpreted as the product of extreme granitic fractionation. Such a magmatic process is defined by fractional crystallization leading to an increase of rare elements and fluxes in the residual melt with increasing distance from the consolidating parental granitic source (see    , and references cited therein).
In India, pegmatites are of Precambrian age and occur in different geological domains    and contain rare metal (Sn, Ta, Be and Li) bearing minerals, such as cassiterite, columbite, tantalite, beryl, lepidolite, amblygonite   , pollucite . These pegmatite belts are localised in metamorphic terrains and are genetically related to various granitic bodies    . Micas are phyllosilicates with the simplified formula IM2-3 □1-2T4O10A2, where I is commonly Cs, K, Na, NH4, Rb, Ba, Ca; M is usually Li, Fe (Fe3+ or Fe2+), Mg, Mn (Mn3+ or Mn2+), Zn, Al, Cr, V, Ti & □ represents a vacancy; T is usually Be, Al, B, Fe3+, Si, and A is usually Cl, F, OH, O (oxy-micas), and S . Lepidolite (or lithium mica) K (Li, Al,  □)3(Si, Al)4O10(F, OH)2 is known for its pink and purple colours and is one of the major sources of the rare alkali metals rubidium and cesium. Ferromagnesian micas are significant mafic minerals in intermediate and basic igneous rocks whereas Li-bearing micas predominate in peraluminous leucogranites, associated pegmatites and ore deposits . Micas are useful as monitors of the physicochemical environment, in which they grew, as well as indicators of the metallogenetic potential of their host rock (e.g.     ). Li-bearing micas may be abundant in evolved late-stage granites, associated pegmatites, and ore deposits in metasomatic rocks    .
Lepidolite occurrence from the area was first reported by  and carried out detailed investigation and traced lepidolite bearing boulders over a 120 m × 30 m zone . Subsequently, preliminary work carried out at Chakrasila and adjoining area through collection of geochemical samples and drilling   . The work for W, Sn & REE in Ckakrasila area has been attended and indicated lepidolite occurrence in pegmatite with higher concentration of Rb and Y . The purpose of this paper is geochemistry and genesis of lepidolite and non-lepidolite pegmatites.
2. Geological Background
The Assam Meghalaya Gneissic Complex (AMGC) is the north eastern extension of Indian Shield and is separated from the main mass of Peninsular India by Tertiary sediments of Ganges Brahmaputra and Cretaceous Rajmahal volcanics. The Shillong plateau composed of AMGC is considered as the detached portion of Eastern Ghats Mobile belt  or Chotanagpur Gneissic Complex  (Figure 1, after   ). The plateau is E-W striking horst block elevated about 600 - 1800 m above the Bangladesh plains. The plateau comprises the Neoarchean-Proterozoic to Early Paleozoic (2.6 - 0.5 Ga) basement gneissic rocks     , the Paleo Mesoproterozoic NE-SW trending intracratonic Shillong basin constituting metasedimentary supracrustal rocks of the Shillong Group   . Shillong Group has undergone green schist facies of metamorphism . Proterozoic-Early Paleozoic (881 - 479 Ma) equigranular to porphyritic coarse grained granite-granodiorites plutons (Mylliem granites and its equivalents) intruding the basement gneisses and the Shillong Group of rocks   - . Basic volcanics of Sylhet /Mikir traps of Cretaceous age occurs as concordant to discordant bodies within the Shillong group of rocks. The plateau is bounded and dissected by various fault systems E-W and N-S to the major earthquakes in the region. To North the plateau is bounded by Oldham fault  and to south it is flanked by Dauki fault  also considered as the extension of Son Narmada Fault. Advanced studies incorporated with chemical dating suggests that in the global scenario AMGC can be probably a leading edge during oblique collision between India with Austarlo Antartica during Pan-African final amalgamation and the Pan-African suture passing through Prydz Bay in Antarctica continued to the Shilling plateau which passes in between Sonapahar and Garo-Goalpara Hills regions of the Shillong plateau .
The study area is the part of Assam Meghalaya Gneissic Complex (AMGC)/Precambrian Gneissic Complex in the Dhubri district, Assam. In Assam, the rocks of AMGC are the north western extension of the Proterozoic rocks of Meghalaya Plateau or Shillong plateau  . The Precambrian rocks
Figure 1. Regional geological map of Assam Megahlaya Gneissic Complex (AMGC) showing location of Chakrasila area (after,   ). (A) Geological map of Chakrasila area with lepidolite pegmatite .
of AMGC are dominated by granulite to amphibolite facies of rocks interlayered with Banded Iron Formations (BIF), amphibolites, talc-actinolite schist and pyroxenites . Gneissic complex occupies a large part of the central Assam and few isolated inselbergs cutting out of the Quaternary plains of western Brahmaputra Basins. The Gneissic Complex comprises of biotite-bearing quartzo-feldspathic gneiss, schist, biotite-hornblende gneisses, migmatitic granitoid intruded by younger acidic (granite, aplite, pegmatite) and basic (metadolerite, epidiorite, amphibolite) intrusive rocks (Figure 1(A), after  ).
3. Field Occurrence and Petrography
In the field, mineralogically pegmatites are composed of 1) quartz-feldspar; 2) quartz-feldspar-tourmaline-biotite-muscovite; 3) quartz-feldspar-biotite-muscovite and 4) quartz-feldspar-lepidolite. The detail work on lepidolite pegmatite and non-lepidolite pegmatite is discussed below.
1) Lepidolite pegmatite:
Lepidolite occurred as flakes within pegmatite veins, which is intruded in biotite gneiss and amphibolite in the northern tip of Dhir Bill (at Chakrasila). Amphibolite and actinolite tremolite schist are associated rocks in the area and are in the form of small bodies and boulders on Chakrasila hillock. In situ lepidolite/pegmatite veins as exposed in the area, only large blocks and boulders of lepidolite rocks scattered over the surface (Figure 2(A) and Figure 2(B)). The
Figure 2. Field photographs of lepidolite pegmatite showing (A) pink lepidolite flakes, (B) small boulder with lepidolite flakes and fractures on surface, (C) Hand specimen of purple to violet lepidolite, (D) & (E) Photomicrograph showing clusters of lepidolite showing fanning and deformation along with quartz. Field photographs of non-lepidolite pegmatite displaying (F) zoning with quartz core and fracturing, (G) Contact between lepidolite pegmatite and non-lepidolite pegmatite, (H) & (I) Graphic intergrowth texture and zircon inclusion in biotite.
large blocks and boulders of lepidolite bearing pegmatite spread over the surface for a length of 200 m with a width of 120 - 130 m. It occurs in the form of fragmented boulder rather than continuous body/exposure. At places these boulders are traversed by quartz veins of 30 - 40 cm length and width of 2 - 4 cm. The lepidolite predominantly pink to purplish-violet and in the form of fine to coarse flakes, radiating clusters with subordinate quartz, feldspar and muscovite (Figure 2(C)). From the nature of concentration of blocks and boulders of lepidolite pegmatite over gently sloping ground it seems that they are in situ. Pegmatite is medium to coarse grained and is composed of lepidolite, quartz, alkali feldspar, muscovite and opaque minerals. It is massive, hard and compact.
In petrography, pegmatite is medium to coarse grained and is composed of lepidolite, quartz, alkali feldspar, muscovite and opaque minerals. Lepidolite is in the form of tabular to platy, laths to euhedral crystals, medium to coarse grained and is showing well developed parallel twinning (Figure 2(D)). It occurs in the form of phenocrysts and small grains as ground mass. The lepidolite is medium to fine grained and has layering in some parts and showing unidirectional cleavage and has equigranular structure. In some portion the rock is almost monomineralic in which lepidolite mineral varies from 90% to 95%. It contains inclusion of quartz, which are mostly subhedral to anhedral while. K-feldspar is subhedral and medium to fine grained (Figure 2(E)). In some parts, lepidolite flakes and clusters are deformed and showing kinking along with deformed quartz. Radiating crystals show fanning with wavy margins and deformed crystals reflects pinch and swelling along with ribbon shaped quartz.
2) Non-lepidolite pegmatite:
Non-lepidolite pegmatite (hereafter pegmatite) occurs as small to large veins and boulders. It ranges from 10 to 20 m in length and 20 to 50 m in width. Pegmatite is dominated in southern part and boulders of pegmatite also notice from hill top, central part, eastern and western flank of the mapped area. Pegmatite is coarse grained and composed of pink K-feldspar + quartz + biotite ± muscovite ± magnetite and garnet. It mainly NW-SE parallels to the foliation of the granite gneiss. This pegmatite is zoned (Figure 2(F)). The boarder part is comprised of K-feldspar and muscovite on either side and coarse quartz crystals at the core part. It is also showing intrusive contact with lepidolite pegmatite (Figure 2(G)).
In thin section, it is medium to coarse grained and consist of quartz, K-feldspar and plagioclase, biotite and muscovite (Figure 2(H)). Garnet, zircon and opaque minerals occur as accessory mineral. The quartz grains are mostly subhedral to anhedral with deformation and shows wavy extinction and at places play undulose extinction. Biotite and muscovite is lath shaped and is present as very thin flakes (Figure 2(I)). Biotite is dark brown to dark yellowish and shows pleochroic halos surrounding the zircon grain (Figure 2(J)). K-feldspar is subhedral and more dominant over plagioclase-feldspar. At some places, microcline with cross hatched twinning is observed. Plagioclase feldspars occur as subhedral grains with polysynthetic twinning. Some overgrowth texture also noticed, K-feldspar growths over plagioclase-feldspar and shows perthite texture. Beside that plagioclase alters to sericite. In some places K-feldspar is replaced by plagioclase feldspar and muscovite.
4. Sampling Methods and Analytical Techniques
An area of 50 Sq.km. has been covered by large scale mapping on 1:10,000 and an area of 1 sq.km by detailed mapping on 1:5000 in and around Chakrasila hill. Samples from lepidolite bearing and non-lepidoilite pegmatites were collected systematically for petrological, mineralogical and geochemical studies. The thin section was prepared at Petrology Division, GSI, NER, Shillong and GSI, CR, Nagpur. The petrographic studies and photomicrographs of pegmatites was carried out at SU: Assam, NER, Guwahati using Nikon 600 Pol microscope with camera attachment and Leica DMRXP Pol microscope with Leica DMC 4500 camera and software attachment. Bulk pegmatite samples, collected from both the lepidolite bearing and non-lepidoilite pegmatites were analyzed for major, trace and REE by XRF and ICP-MS at Chemical Division, GSI, Shillong and Kolkata following standard analytical procedures. The X-ray diffraction phase analysis of lepidolite (separated flakes) has been carried out by using PANalytical XRD (EMPYREAN Diffractometer system) at mineral Physics Division, GSI, Central Region, Nagpur. The general conditions were 40 mA, 45 kV at temperature of 25˚C with Cu tube (anode material). Lepidolite is the major mineral phase in the form of muscovite (as lithium is not determined) and Kaliophilite in trace amount. The result of XRD analytical data is given in Table 1 and X-ray diffractograms in Figure 3.
5. Geochemistry of the Pegmatites
1) Major oxide Geochemistry
In lepidolite pegmatite SiO2 is high ranging from 51.43 to 77.07 wt% (except one sample having 49.93 wt% might be due to contamination of mafic phase or error in sample collection). High Al2O3 varies from 12.13 to 28.65 wt%, low to high K2O upto 8.99 wt%, Na2O from 0.19 to 2.74 wt%. Low amount of CaO ranging from 0.01 to 1.12 wt% (except one sample 10.82 wt%) and P2O5 from 0.01 to 9.59 wt% (high in one sample). Low amount of MnO varying from 0.01 to 1.25 wt%, MgO from 0.01 to1.91 wt% (except 5.92% MgO in one sample) and
Table 1. X-ray phase analytical result of lepidolite.
Figure 3. X-ray diffractogram of lepidolite.
Table 2. Major oxide data of lepidolite pegmatites (samples of L-series) and non-lepidolite pegmatite (samples of P-series).
Table 3. Trace element data of lepidolite pegmatites (samples of L-series) and non-lepidolite pegmatite (samples of P-series).
TiO2 is varying from 0.03 to 0.76 wt%. Fe2O3T is varying from 0.08 to 9 wt% and one sample have high amount 13.98 wt%.
Pegmatite shows high amount of SiO2 ranging from 68.45 to 78.64 wt% (except one sample having 98.72 wt% quartz rich sample). High Al2O3 varies from 9.89 to 17.04 wt%, high K2O upto 12.37 wt% and high Na2O from 1.12 to 5.23 wt%. Low CaO ranging from 0.08 to 4.58 wt% (except one sample 10.82 wt%) and P2O5 from 0.01 to 10.56 wt%. Low MnO and MgO vary from 0.01 to 0.05 wt% and 0.01 to 0.53 wt% respectively. Fe2O3T is varying from 0.14 to 3.09 wt%.
These high amounts of major elements such as SiO2, Al2O3, K2O and Na2O with low amount of CaO, MnO, MgO and TiO2 are indicative of the importance of fractional crystallization in their petrogenesis. Fairly high amount of P2O5 and Fe2O3T could be related to crystallization of minerals, such as apatite, titanite, and biotite from magma in early stages of its evolution.
a) Classification of pegmatites:
On SiO2 vs Na2O + K2O TAS diagram of , the compositions of samples plotted closed to the field of alkali granite and granite with sub-alkaline to alkaline nature (Figure 4(A)). The SiO2 vs K2O binary diagram (after,  ) indicates calc-alkaline to high calc-alkaline characters for majority samples. Whereas, some samples plotted in tholeiitic field and few lepidolite samples in soshonitic field (Figure 4(B)). The molar Al2O3/(CaO + Na2O + K2O) versus molar Al2O3/ (Na2O + K2O) (A/CNK vs A/NK) diagram   reflect the per-aluminous character of both the pegmatites (Figure 4(C)). In SiO2 vs Na2O+K2O-CaO (MALI) diagram of  samples plot in the field of calcic and calc-alkalic field. The overlapping field of I-type, A-type and S-type are from , where studied samples indicate both S-type and I-type magmatic characters (Figure 4(D)). Reference  have proposed a new classiﬁcation scheme to separate calc-alkaline granites from A-type granites and oxidised A-type granites from reduced A-type granites. In the CaO/(FeOt + MgO + TiO2) vs. CaO + Al2O3 and CaO/(FeOt + MgO + TiO2) vs. Al2O3 diagrams (Figure 4(E) and Figure 4(F)), the data falls in the A-type, calc-alkaline granite fields and some samples away from the calc-alkaline field. In the FeOt/(FeOt + MgO) vs. Al2O3 and FeOt/(FeOt + MgO) vs. Al2O3/(K2O/Na2O) diagrams (Figure 4(G) and Figure 4(H)), most of the samples plot near to oxidised A-type field and some towards the reduced A-type field. Few samples fall in the ﬁeld of calc-alkaline granite field.
On the basis of Alumina Saturation Index (ASI), these pegmatites resemble Lithium-Cesium-Tantalum (LCT) family of pegmatites (e.g.,   ). Their A/NK values are in the range of 1.50 - 3.52 (except two samples having 7.6 & 145.05) for lepidolite pegmatite. However, non-lepidolite pegmatite has values
Figure 4. Geochemical diagrams displaying (A) SiO2 vs Na2O + K2O TAS classification diagram of pegmatites. Both the pegmatite’s indicates alkali granite to granite affinity (after,  ), (B) The SiO2 vs K2O binary diagram indicates calc-alkaline to high calc-alkaline characters (after,  ). Some non-lepidolite pegmatite samples indicate tholeiitic field and three samples of lepidolite pegmatite plot in the shoshonitic field, (C) A/CNK vs A/NK diagram reflects the per-aluminous character of both the pegmatite’s  , (D) In SiO2 vs Na2O + K2O-CaO diagram of , samples plot in the field of calcic to alkali-calcic field for both the pegmatites. The field of I-type, A-type and S-type are from , (E) & (F) In the CaO/(FeOt + MgO + TiO2) vs. CaO + Al2O3 and CaO/(FeOt + MgO + TiO2) vs. Al2O3 diagrams the data falls in the A-type, calc-alkaline granite fields and some samples away from the calc-alkaline field (after,  ), (G) & (H) In the FeOt/(FeOt + MgO) vs. Al2O3 and FeOt/(FeOt + MgO) vs. Al2O3/(K2O/Na2O) diagrams, most of the samples plot near to oxidised A-type field and some towards the reduced A-type field and differing from calc-alkaline field. However, clustering of samples is also witnessed near to oxidised A-type field (after,  ).
ranges from of 0.50 - 9.37. The A/CNK values are in the range of 1.406 - 3.506 (except two samples have 1.032 & 138.143) for lepidolite pegmatite. The non-lepidolite pegmatite has A/CNK values are in the range of 0.333 - 8.630. Most pegmatites with the LCT signature have compositional affinity with S-type granites . These types of pegmatites are usually related to S-type granites of orogenic environments (i.e., subduction zones or continental collision zones)     .
2) Trace and immobile element geochemistry
In lepidolite pegmatite, trace element Ba varies from 50 to 821 ppm, Ga from 26 to 163 ppm and Rb from 239 to 393 ppm (three samples have 12,409, 13,138 & 15,537 ppm Rb content). Sr from 6 to 130 ppm, Y ranging from 21 to 939 ppm, Zn from 10 to 676 ppm. In non lepidolite pegmatite, trace element Ba varies from 50 to 1241 ppm, Ga from 5 to 41 ppm and Rb from 3 to 1268 ppm. Sr from 5 to 186 ppm, Y ranging from 5 to 91 ppm, Pb from 12 to 319 ppm.
a) Tectonic discriminations and fractional crystallization:
Trace element compositions of the studied rocks are presented, briefly. An increase in the amounts of Rb can be correlated with late stage crystallization of K-feldspar and biotite, and decrease in Sr contents can be due to fractional crystallization of plagioclase. Barium content is commonly used as indicator of the evolution in granites and pegmatites, which decreases with increasing crystal fractionation  , and the decrease in content of Ba is marked. High amount of Ba (50 - 821 ppm) is due to the presence of minerals, such as K-feldspar and biotite. Rubidium contents in the pegmatites vary from 239 to 393 ppm and Sr contents from 6 to 130 ppm. With increasing concentrations of K, the Rb contents of the rocks increase, as well. The increasing concentration of Ba, Sr and Cs values, are also observed in samples due to their similar geochemical behavior. These chemical characteristics indicate that the studied pegmatites are highly evolved varieties of granitoids of the region. As a rare alkali metal Rb is enriched in K-bearing minerals during progress of pegmatite crystallization , the ratio of K/Rb is indicative of the general fractionation.
A hybridization index of CaO + MgO + FeOT is useful in quantifying deviations from leucogranitic melt compositions (see  ). Rb vs. Sr and Rb vs. Ba plots showing variable degrees of fractionation within the simple-type and hybridized pegmatites and granites; the trend for normal granites is plotted for comparison. The pegmatites are strongly to moderately evolved, as demonstrated by Rb-Ba-Sr trends that vary between signatures of a normal and a moderately fractionated granitic pegmatite . The majority of the pegmatites plots away the normal granite trend. Ratios of K/Rb vs. Cs (see  ) are good proxies to evaluate the K-Rb and K-Cs substitution in potassium feldspar and micas within the bulk samples. The granites differ from the granitic pegmatites by having significantly lower Rb, but comparable Cs contents. The studied samples follow a simple type pegmatite fractionation pathway on the K2O/Rb vs. Rb plots. The trends are very steep, increasing sharply in Rb. The pegmatites clearly lie on a deeper K2O/Rb vs. Rb path.
b) The pegmatite protoliths (source rock) characteristics:
A few samples contain progressively less Sr and Ba and more Rb as a result of fractionation. High amounts of Rb in the studied pegmatites, indicate that these samples are placed in the category of strongly differentiated granites in the ternary Rb-Ba-Sr plot . Other samples are moderately evolved chemically. On the basis of diagram from  studied pegmatites plot mainly in S-type granites fields and few samples plot in I-type field indicate involvement S-type granite as major source along with I-type granite as minor constituents. Therefore, both the studied pegmatites could be an evolved variety of granitic rocks that originated from the same magma.
The Rb vs Sr and Rb vs Ba (ppm) diagrams showing variable degrees of fractionation, the studied samples plotted above the normal granite field (Figure 5(A) and Figure 5(B)). The trend of normal granite field is after . Three samples have more than 10,000 ppm Rb and not plotted in the diagram, which indicate more fractionation of Rb, Sr and Ba in both the pegmatites. Rb vs K2O/Rb (ppm) diagram (after,  ) evaluate the K–Rb fractionation in simple-type and complex-type (hybridized) pegmatites. The analysed data plot near the arrow of simple type pegmatite and few samples scattered around hybrid pegmatite (Figure 5(C)). The trace element Zr vs TiO2 diagram  indicate mainly S-type granitic source for both the pegmatites and few samples of plots in I-type field (Figure 5(D)). In triangular CaO-Al2O3-Na2O-K2O-Fe2O3T + MgO diagram (after,  ) indicate mainly S-type field and I-type field for some samples (Figure 5(E)) and Zr vs Nb/Ta (ppm) diagram (after,  ) indicate enrichment and fractionation of Nb (Figure 5(F)). The Nb/Ta ratios for pegmatites range between 0.31 and 30.93 in lepidolite pegmatite and between 4.11 and 61.98. Nb/Ta vs. Ta and Nb/Ta vs. K2O/Rb plots show variations in Nb/Ta indicate fractionation between simple-type pegmatites vs. hybridized pegmatites; the arrows indicate the direction of a more evolved (i.e. fractionated) melt undergoing hybridization. In Nb/Ta vs Ta samples plot in lower end of hybridization arrow and few towards the arrow head (Figure 5(G)) and Nb/Ta vs K2O/Rb diagram samples plot around hybridization arrow indicate more fractionation of Ta and Rb in lepidolite pegmatite (Figure 5(H)). Variations in Nb/Ta and Zr/Hf also infer a moderate to high degree of fractionation in the pegmatite melts. Similarly, the immobile elemental magmatic aﬃnity plot of  in Yb vs Th (ppm) diagram data indicate calc-alkaline affinity (Figure 5(I)) and in Yb vs La (ppm) samples plot in the tholeiitic to transitional field and samples of lepidolite pegmatite
Figure 5. (A) Rb vs Sr & (B) Rb vs Ba (ppm) diagrams the studied samples plotted above the normal granite field showing variable degrees of fractionation of pegmatites, (C) Rb vs K2O/Rb (ppm) diagram, the analysed data plot near the arrow of simple type pegmatite and few samples scattered around hybrid pegmatite (after,  ), (D) The trace element Zr vs TiO2 diagram indicate mainly S-type granitic source for both the pegmatites (after,  ), (E) In triangular CaO-Al2O3-Na2O-K2O-Fe2O3T + MgO diagram indicate mainly S-type field and I-type field for some samples (after,  ), (F) Zr vs Nb/Ta (ppm) diagram indicate enrichment and fractionation of Nb (after,  ), (G) In Nb/Ta vs Ta samples plot in lower end of hybridization arrow and few towards the arrow head, (H) Nb/Ta vs K2O/Rb diagram samples plot around hybridization arrow indicate more fractionation of Ta and Rb in lepidolite pegmatite, (I) Yb vs Th (ppm) diagram data indicate calc-alkaline affinity in immobile elemental magmatic aﬃnity plot , (J) Yb vs La (ppm) samples plot in the tholeiitic to transitional field and samples of lepidolite pegmatite in transitional to calc-alkaline field, (K) Ternary Hf-Rb/30-Ta*3 diagram reflects mainly within plate tectonic field, and for some samples all other fields  and (L) Ba-Rb-Sr ternary diagram represent normal to strongly differentiated trend of granite/pegmatite (after,  ). Symbols are same as used in Figure 4.
in transitional to calc-alkaline field (Figure 5(J)). Ternary Hf-Rb/30-Ta*3 diagram  samples reflect within plate and volcanic arc tectonic fields, and for some samples all other fields (Figure 5(K)) and Ba-Rb-Sr ternary diagram (after,  ) represent normal to strongly differentiated trend of granite/pegmatite with few samples as anomalous granite (Figure 5(L)).
3) Rare Earth Element geochemistry
The Rare Earth Element (REE) data of both the pegmatites is presented in Table 4. The REE spider and multi-element spider variation diagrams were plotted using these data.
Rare Earth Element is relatively low to moderate. LREE i.e. La ranging from 1 to 20.76 ppm, Ce from 2 to 59.51 ppm and Nd from 0.88 to 27.53 ppm. HREE i.e. Gd from 0.50 to 4.73 ppm, Tb from 0.50 to 0.83 ppm, Dy from 0.50 to 4.40 ppm, Ho from 0.50 to 0.65 ppm, and Er from 0.50 to 1.59 ppm. The REE spider
Table 4. Rare Earth Element data of lepidolite pegmatites (samples of L-series) and non-lepidolite pegmatite (samples of P-series).
diagram (Figure 6(A) & Figure 6(B)) and multi element spider diagram (Figure 6(C) & Figure 6(D)) after  represented following observations. The chondrite-normalized spider diagram indicates slightly enriched LREE pattern (La, Ce, Pr, Nd, Pm, Sm, Eu), than HREE (Gd, Tb, Dy, Er, Tm, Yb, Lu) in lepidolite pegmatite. However, there is enrichment of MREE (Eu, Gd, Tb, Dy, Er) and HREE in non-lepidolite pegmatite. LREE enrichment correlates with monazite and allanite, which host the LREE in these rocks . There is negative and positive Europium anomaly for some samples in both the pegmatites, which indicate fluctuation in the crystallization of plagioclase in the source region or presence of plagioclase in minor amount in the magma. Pronounced negative anomalies such as Ce, Nd, Gd, Dy, Er and Yb indicate absence of posphatic minerals in the magma. Whereas, strong positive anomalies such as Pr, Pm, Tb, Ho and Tm indicate garnet and amphibole in the source region. On chondrite-normalized multi-element diagrams , high field strength elements (HFSE), such as Zr and Nb show negative anomalies. These anomalies may result from the preservation of such elements in residual phases when magmas have been generated in a subduction zone by partial melting of source rocks (see  ). Positive anomaly of Rb in multi-elements spider diagram may have resulted from late stage crystallization of muscovite and K-feldspar from magma. Barium, and Sr negative anomalies can be due to their co-substitution in plagioclase, which crystallizes at early stages.
On the whole, enrichment in some LILE, such as K, Rb, and Th and depletion
Figure 6. (A) & (B) The REE spider diagram for lepidolite pegmatite and non-lepidolite pegmatite (after,  ), (C) & (D) Multi element primitive mantle spider diagram for lepidolite pegmatite and non-lepidolite pegmatite (after,  ).
in some HFSE, such as Nb, Ti, Zr, and Y, and HREE can be related to melting and fractionation processes in the region  . According to the LCT (Li-Cs-Ta) family of pegmatites contains high concentrations of Rb, Cs, Be, Ta, Nb, and Sn, as well as elevated levels of fluxing components (Li, P, F, and B). Accordingly, the studied lepidolite pegmatites have high concentration of Rb (up to 393 ppm; three samples have 12,409, 13,138 & 15,537 ppm), Ta (up to 269.86 ppm), Nb (up to 83 ppm), and Sn (312.85 ppm). High amounts  of HFSE elements, such as Th (up to 102 ppm), U (up to 11.26 ppm), and Zr (up to 259 ppm) are may be due to occurrence of some minerals, such as Th-silicate, U-silicate, U-oxides, and zircon in pegmatites. Accordingly, the studied non lepidolite pegmatites have high concentration of Rb (up to 1268 ppm), Nb (up to 46 ppm), HFSE element such as Th (up to 42 ppm), U (up to 93.36 ppm), and Zr (up to 493 ppm) are might be due to occurrence of some minerals, such as Th-silicate, U-silicate, U-oxides, and zircon in pegmatites. These above REE studies emphasize the highly fractionated nature of both these pegmatites from the granitic source.
On the basis of field characters, pegmatites are intrusive as small to large veins in the biotite gneiss and amphibolite with lepidolite as important mineral. Geochemically, they are calc-alkaline to high calc-alkaline and per-aluminous in characters. On the basis of Alumina Saturation Index (ASI), these pegmatites are resembling to Lithium-Cesium-Tantalum (LCT) family of pegmatites. Most pegmatites with the LCT signature have compositional affinity with S-type granites of orogenic environments (i.e., subduction zones or continental collision zones). Trace element compositions (Rb, Sr, Ba) indicate crystal fractionations, variable degrees of fractionation and highly evolved nature of pegmatites from the granitic source. The different tectonic discrimination diagrams indicate S-type and I-type melt for pegmatite derivations. High amounts of Rb in the studied pegmatites, indicate that these samples are placed in the category of strongly differentiated granites in the ternary Rb-Ba-Sr plot. Therefore, both the studied pegmatites could be an evolved variety of granitic rocks that originated from the same magma. The REE is relatively low to moderate and slightly enriched LREE pattern in lepidolite pegmatite. However, there is enrichment of MREE and HREE in non-lepidolite pegmatite.
The authors are grateful to the DDG & RMH-II, GSI, NER Shillong is for his kind guidance and encouragement during the field work. RRM collected the samples during his field visits with the help of project officers and he indebted to them for their help in the field. Due acknowledgment is given to the Geological Survey of India for providing all facilities. The Petrology Division and Mineral Physics Division, GSI, CR is acknowledged for their kind help for lab studies. The authors also acknowledge anonymous reviewers for their constructive and thoughtful comments, which helps for improving the manuscript’s quality.
 Cerny, P. (1991) Rare-Element Granite Pegmatites. Part I: Anatomy and Internal Evolution of Pegmatite Deposits. Part II: Regional to Global Relationships and Petrogenesis. Geoscience Canada, 18, 49-81.
 Taylor, R.P. and Strong, D.F. (1985) Recent Advances in the Geology of Granite-Related Mineral Deposits: Proceedings of the CIM Conference on Granite-Related Mineral Deposits. Canadian Institute of Mining and Metallurgy, Vol. 39, 1-445.
 Norton, J.J. and Redden, J.A. (1990) Relations of Zoned Pegmatites to Other Pegmatites, Granite, and Metamorphic Rocks in the Southern Black Hills, South Dakota. American Mineralogist, 75, 631-655.
 Wise, M.A. and Brown, C.D. (2010) Mineral Chemistry, Petrology and Geochemistry of the Sebago Granite Pegmatite System, Southern Maine, USA. Journal of Geosciences, 55, 3-26.
 Jahns, R.H. and Burnham, C.W. (1969) Experimental Studies of Pegmatite Genesis. I. A Model for the Derivation and Crystallization of Granitic Pegmatites. Economic Geology, 64, 843-864.
 Trueman, D.L. and Cerny, P. (1982) Exploration for Rare-Element Granitic Pegmatites. In: Cerny, P., Ed., Granitic Pegmatites in Science and Industry, Association of Canada Short Course Handbook, Mineral, Vol. 8, 463-494.
 Lamba, V.J.S. and Khanna, V.K. (1981) Characteristic Feature of Tin-Bearing Rare Metal Pegmatites of Konta Tahsil, Bastar District, M.P. Bulletin of the Indian Geologists Association, 14, 151-154.
 Babu, P.V.R., Pandey, B.K. and Dhana Raju, R. (1993) Rb-Sr Ages on the Granite and Pegmatitic Minerals from Bastar-Koraput Pegmatite Belt, Madhya Pradesh and Orissa, India. Journal of the Geological Society of India, 42, 33-38.
 Som, S.K., Bandyopadhyay, K.C., Basu, S.K., Santra, D.K. and Ghosh, R.N. (2002) Li-Cs-Rb Mineralization in Proterozoic Zoned Pegmatites of Beku, West Bengal. Journal of the Geological Society of India, 60, 493-503.
 Singh, Y., Pandit, P.S.C., Bagora, S. and Jain, P.K. (2017) Mineralogy, Geochemistry, and Genesis of Co-Genetic Granite-Pegmatite-Hosted Rare Metal and Rare Earth Deposits of the Kawadgaon Area, Bastar Craton, Central India. Journal of the Geological Society of India, 89, 113-228.
 Rieder, M., Cavazzini, G., D’yakonov, Yu.S., FrankKamenetskii, V.A., Gottardi, G., Guggenheim, S., Koval’, P.V., Muller, G., Neiva, A.M.R., Radoslovich, E.W., Robert, J.-L., Sassi, F.P., Takeda, H., Weiss, Z. and Wones, D.R. (1998) Nomenclature of the Micas. The Canadian Mineralogist, 36, 905-912.
 Tischendorf, G., Forster, H.J. and Gottesmann, B. (2001) Minor and Trace-Element Composition of Tri-Octahedral Micas: A Review. Mineralogical Magazine, 65, 249-276.
 Cerny, P. and Burt, D.M. (1984) Paragenesis, Crystallo-Chemical Characteristics and Geochemical Evolution of Micas in Granite Pegmatites. In: Bailey, S.W., Ed., Micas, Reviews in Mineralogy, Vol. 13, De Gruyter, Berlin, 257-297.
 Guidotti, C.V. (1984) Micas in Igneous Rocks. In: Bailey, S.W., Ed., Micas, Reviews in Mineralogy Vol. 13, Mineralogical Society of America, Washington DC, 357-467.
 Hewitt, D.A. and Wones, D.R. (1984) Experimental Phase Relations of Micas. In: Bailey, S.W., Ed., Micas, Reviews in Mineralogy Vol. 13, Mineralogical Society of America, Washington DC, 201-256.
 Speer, J.A. (1984) Micas in Igneous Rocks. In: Bailey, S.W., Ed., Micas, Reviews in Mineralogy Vol. 13, Mineralogical Society of America, Washington DC, 299-356.
 Henderson, C.M.B., Martin, J.S. and Mason, R.A. (1989) Compositional Relations in Li-Micas from S.W. England and France: An Ion- and Electron-Microprobe Study. Mineralogical Magazine, 53, 427-449.
 du Bray, E.A. (1994) Compositions of Micas in Peraluminous Granitoids of the Eastern Arabian Shield. Implications for Petrogenesis and Tectonic Setting of Highly Evolved, Rare Metal Enriched Granites. Contributions to Mineralogy and Petrology, 116, 381-397.
 Mohamed, F.H., Abdalla, H.M. and Helba, H. (1999) Chemistry of Micas in Rare-Metal Granitoids and Associated Rocks, Eastern Desert, Egypt. International Geology Review, 41, 932-948.
 Mishra, M.K. and Singh, B. (2017) Investigation for W, Sn & REE in the Chakrasila, Nadangiri and Bhumeswar in the Bongaigaon, Dhubri and Kokrajhar Districts, Assam. Geological Survey of India FS 2014-16.
 Khonglah, M.A., Khan, M.A., Karim, M.A., Kumar, A. and Choudhury, J. (2008) Geology and Structure of the Areas in and around Shillong, Meghalaya, North East India, Revisited. Proceedings of the National Seminar on Geology & Energy Resources of NE India: Progress & Perspectives Nagaland University Research Journal Special Pub.
 Srivastava, R.K. and Sinha, A.K. (2004) The Early Cretaceous Sung Valley Ultramafic-Mafic-Alkaline-Carbonatite Complex, Shillong Palateau, Northeastern India: Petrological and Genetic Significance. Mineralogy and Petrology, 80, 241-263.
 Kumar, S., et al. (2017) Contribution of Columbia and Gondwana Supercontinent Assembly- and Growth-Related Magmatism in the Evolution of the Meghalaya Plateau and the Mikir Hills, Northeast India: Constraints from U-Pb SHRIMP Zircon Geochronology and Geochemistry. Lithos, 277, 356-375.
 Chatterjee, N., Bhattacharya, A., Duarah, B.P. and Mazumdar, A.C. (2011) Late Cambrian Reworking of Paleo-Mesoproterozoic Granulites in Shillong-Meghalaya Gneissic Complex (Northeast India): Evidence from PT Pseudosection Analysis and Monazite Chronology and Implications for East Gondwana Assembly. The Journal of Geology, 119, 311-330.
 Chatterjee, N., Mazumdar, A.C., Bhattacharya, A. and Saikia, R.R. (2007) Mesoproterozoic Granulites of the Shillong-Meghalaya Plateau: Evidence of Westward Continuation of the Prydz Bay Pan-African Suture into Northeastern India. Precambrian Research, 152, 1-26.
 Ghosh, S., Fallick, A.E., Paul, D.K. and Potts, P.J. (2005) Geochemistry and Origin of Neoproterozoic Granitoids of Meghalaya, Northeast India: Implications for Linkage with Amalgamation of Gondwana Supercontinent. Gondwana Research, 8, 421-432.
 Yin, A., Dubey, C.S., Webb, A.A.G., Kelty, T.K., Grove, M., Gehrels, G.E. and Burgess, W.P. (2010) Geologic Correlation of the Himalayan Orogen and Indian Craton: Part 1. Structural Geology, U-Pb Zircon Geochronology, and Tectonic Evolution of the Shillong Plateau and Its Neighboring Regions in NE India. Geological Society of America Bulletin, 122, 336-359.
 Chimote, J.S., Pandey, B.K., Bagchi, A.K., Basu, A.N., Gupta, J.N. and Sarsawat, A.C. (1988) Rb-Sr Whole-Rock Isochron Age for the Myllium Granite, Khasi Hills, Meghalaya. Fourth National Symposium on Mass Spectrometry, Bangalore, EPs-9/1-9/4.
 Van Breeman, O., Bowes, D.R., Bhattacharjee, C.C. and Chowdhary, P.K. (1989) Late Proterozoic-Early Proterozoic Rb-Sr Whole Rock and Mineral Ages for Granite and Pegmatite, Goalpara, Assam, India. Journal of the Geological Society of India, 34, 89-92.
 Ghosh, S., Bhalla, J.K., Paul, D.K., Sarkar, A., Bishui, P.K. and Gupta, S.N. (1991) Geochronology and Geochemistry of Granite Plutons from East Khasi Hills, Meghalaya. Journal of the Geological Society of India, 37, 331-342.
 Ghosh, S., Chakraborty, S., Paul, D.K., Bhalla, J.K., Bishui, P.K. and Gupta, S.N. (1994) New Rb-Sr Isotopic Ages and Geochemistry of Granitoids from Meghalaya and Their Significance in Middle to Late Proterozoic Crustal Evolution. Indian Minerals, 48, 33-44.
 Peccerillo, A. and Taylor, S.R. (1976) Geochemistry of Eocene Calc-Alkaline Rocks from Kastamonu Area, Northern Turkey. Contributions to Mineralogy and Petrology, 58, 63-81.
 Frost, R.B., Barnes, C.G., Collins, W.J., Arculus, R.J., Ellis, D.J. and Frost, C.D. (2001) A Geochemical Classification for Granitic Rocks. Journal of Petrology, 42, 2033-2048.
 Landenberger, B. and Collins, W.J. (1996) Derivation of A-Type Granites from a Dehydrated Charnockitic Lower Crust: Evidence from the Chaelundi Complex, Eastern Australia. Journal of Petrology, 37, 145-170.
 Dall’Agnol, R. and de Oliveira, D.C. (2007) Oxidized, Magnetite Series, Rapakivi-Type Granites of Carajas, Brazil: Implications for Classification and Petrogenesis of A-Type Granites. Lithos, 93, 215-233.
 Cerny, P. (1992) Geochemical and Petrogenetic Features of Mineralization in Rare Element Granitic Pegmatites in the Light of Current Research. Applied Geochemistry, 7, 393-416.
 Martin, R.F. and Vito, C.D. (2005) The Patterns of Enrichment in Felsic Pegmatites Ultimately Depend on Tectonic Setting. The Canadian Mineralogist, 43, 2027-2048.
 Alfonso, P., Melgarejo, J.C., Yusta, I. and Velasco, F. (2003) Geochemistry of Feldspars and Muscovite in Granitic Pegmatite from the Capde Creusfield, Catalonia, Spain. The Canadian Mineralogist, 41, 103-116.
 Lentz, D. (1996) U, Mo, and REE Mineralization in Latetectonic Granitic Pegmatites, Southwestern Grenville Province. Ore Geology Reviews, 11, 197-227.
 Mckeough, M.A., Lentz, D.R., Mcfarlane, C.R. and Brown, J. (2013) Geology and Evolution of Pegmatite-Hosted U-Th ± REE-Y-Nb Mineralization, Kulyk, Eagle, and Karin Lakes Region, Wollaston Domain, Northern Saskatchewan, Canada: Examples of the Dual Role of Extreme Fractionation and Hybridization Processes. Journal of Geosciences, 58, 321-346.
 Watson, E.B. and Harrison, T.M. (1983) Zircon Saturation Revisited: Temperature and Composition Effects in a Variety of Crustal Magma Types. Earth and Planetary Science Letters, 64, 295-304.
 Ross, P.S. and Bédard, J.H. (2009) Magmatic Affinity of Modern and Ancient Subalkaline Volcanic Rocks Determined from Trace-Element Discriminant Diagrams. Canadian Journal of Earth Sciences, 46, 823-839.
 Harris, N.B.W., Pearce, J.A. and Tindle, A.G. (1986) Geochemical Characteristics of Collision-Zone Magmatism. Geological Society, London, Special Publications, 19, 67-81.
 Sun, S.S. and McDonough, W.F. (1989) Chemical and Isotopic Systematics of Oceanic Basalts: Implication for the Mantle Composition and Process. Geological Society London Special Publications, 42, 313-345.
 Foley, S.F. and Wheller, G.E. (1990) Parallels in the Origin of the Geochemical Signatures of Island Arc Volcanic and Continental Potassic Igneous Rocks: The Role of Residual Titanites. Chemical Geology, 85, 1-18.
 Peccerillo, A. and Taylor, S.R. (1976) Geochemistry of Eocene Calc-Alkaline Rocks from Kastamonu Area, Northern Turkey. Contributions to Mineralogy and Petrology, 58, 63-81.