Major and trace element composition of sediments provides clue to the tectonic setting, weathering, paleo-oxygenation condition during sedimentation and provenance. (Table 2) shows the major oxide analysis (whole-rock geochemical analysis) of sixteen Neogene mudrocks, summarizes the average major element oxide (wt. %) data for the samples being studied. Mean major elemental composition of the Neogene mudrocks is in reasonable correspondence to the average shale narrated by Wedepohl (1971) [27] , NASC (North American Shale Composite), [28] , UC (the upper crust, [11] ) with the exclusion of the low content of CaO (Table 3) but compared with PASS (Post-Archaean Shale, Taylor and McLennan, 1985 [11] ), the Neogene mudrocks are slight depleted in Al₂O₃ content. The CaO diminution of the Neogene mudrocks is linked to the scarceness of calcic minerals [12] .

The Neogene mudrocks samples show no clear difference in major chemical composition from younger to older. SiO₂ content of the Neogene mudrocks was found to be high (ranging from 58.10% to 62.60%, with an average 59.90%). The TiO₂ content varies from 0.88 to 1.10 wt.%, the Al₂O₃ content from 18.60 to 20.89 wt.%, and the Fe₂O₃ content ranges from 7.74 to 9.67 wt.%. The CaO content is low (0.93 to 3.18 wt.%; av. 1.84 wt.%). Lesserconcentrations have noticed for MnO, CaO TiO₂ and P₂O₅ (0.12%, 1.84%, 1.01%, and 0.17% respectively). The observed relative enrichment in Al₂O₃ and K₂O is linked with the raised up of

K-feldspar, mica and other clay minerals. Diminution of Na2O and CaO is ascribed to minor abundance of plagioclase feldspar. Lower CaO content also indicate no associated carbonates or dolomitization. The poorer feldspar concentration are possibly a result either of weathering processes or the feldspar depletingsource region [5] [12] [13] . Harker Diagrams illustrates the fluctuation in the major elements concentration of Mudrocks relative to SiO₂ [4] [5] . Plots of TiO₂, Al₂O₃, Fe₂O₃, K₂O, Na₂O, CaO, MnO, and MgO against SiO₂ concentration indicate negative linear patterns (Figure 2). The negative correlation of SiO₂ with most major and trace elements is owing to size sorting and quartz dilution all the way through the transportation of these sediments. Amount of SiO₂ is a pointer of richness of silicate minerals existing within the Mudrocks with quartz clearly functioning as the noticeable meaning in the exemplification.

Fe₂O₃ + MgO is also well correlated with Al₂O₃. The latter correlation implies that these oxides are associated with phyllosilicates, particularly in matrix chlorite [12] . X-ray diffraction patterns also disclose that Neogene mudrocks contain illite-chlorite rich clay minerals. The mudrocks silica to alumina ratio is high (3.11). The 3.11 silica-alumina ratio showed that that the mudrocks samples are highly siliceous. The average SiO₂ (59.90%) and Al₂O₃ (19.33%) chemical composition in mudrocks constituted about 79.23% of the samples total chemical composition. The other chemical impurities in mudrocks samples from the Sitakund anticline are Fe₂O₃ (8.72%) and TiO₂ (1.01%). The ranges of SiO₂/Al₂O₃ and Na₂O/K₂O values from 62.74 to 3.56 and 0.17 to 0.29, respectively, suggest that the studied samples represent relatively mature sediments. Variation of major elements is probably a result of sedimentary processes [5] . Sediments K₂O/ Al₂O₃ ratio can be used as an indicator of ancient sediments’ original composition. The K₂O/Al₂O₃ ratios for clay minerals and feldspars are different (0.0 to

0.3, 0.3 to 0.9, respectively) according to Cox [29] . The average K₂O/Al₂O₃ ratio for shale varies from 0.21 to 0.24. The K₂O/Al₂O₃, Shows that the ratio is closer to the lower clay mineral range limit in mudrocks samples.

In the study area, Neogene mudrocks show moderate-to-little discrepancy in concentration of trace elements (Table 4). This characteristic signifies shared provenance, weathering, and tectonic setting [5] [7] [13] .There is a Positive correlation of Al, Cs, Ba, Th, and U with K content denotes that concentrations of these elements are controlled by clay and mica contents (Table 5). Additionally, Zr/Sc and Zr/Hf ratios act as good pointers to observe zircon enrichment [8] [13] . In the studied samples, the high Zr/Hf (range of 20.28 - 47.17 with an average of 33.84) and Zr/Sc (range from 8.45 to 16.25) ratios are indicators of zirconenrichment. La/Sc ratio also proposes the rock maturity, usually differs from 3 to 9 [7] [12] . Analyzed mudrocks demonstrate small deviation in La/Sc ratio, which ranges from 1.92 to 3.43 (Table 6). V and Sc have a tendency to be associated with mafic content. Lower V and Sc contents in the mudrocks suggest that these samples were derived from V and Sc enriched source rocks [2] [3] [5] [12] .

Chondrite-normalized diagrams illustrate REE patterns in the studied samples (Figure 3). The average REE concentrations of all samples were compared to the Post-Archean average Australian Shale (PAAS), NASC (North American Shale Composite, Gromer et al., 1984 [28] ) and the Upper Continental Crust (UCC) concentration values (Taylor and McLennan 1985) [11] . In spite of the differences in the abundance, the samples show similar REE pattern as UC. The Neogene mudrocks show slight LREE enriched.

The geochemical signs of clastic sediments have been used to establish provenance characteristics [11] [19] [31] [32] . Most clastic rocks Al₂O₃/TiO₂ ratios are fundamentally used to deduce source rock composition, because Al₂O₃/TiO₂ ratios increase from 3 to 8 for mafic igneous rocks, from 8 to 21 for intermediate rocks and from 21 to 70 for felsic igneous rocks [33] . The Al₂O₃/TiO₂ oscillated from 17.62 to 22.36 in the Neogene mudrocks. Hence, in this study the Al₂O₃/ TiO₂ ratio propose felsic rocks as being probable source rocks for the analyzed samples including little intermediate sign in nature. Abundance of Cr and Ni in siliciclastic sediments was considered as a useful provenance tool. Low Cr concentration indicates felsic provenance, according to Wrafter and Graham (1989) [34] , and high Cr and Ni content is mainly found in ultramafic rock-derived sediment [19] . The Cr and Ni content in these mudrocks has found to be low, therefore signifying felsic provenance. The increase in the Cr and Ni abundance for passive margin mudrocks is due to the enrichment and adsorption of these elements with the increased phyllosilicate content. Garver et al. (1996) [35] suggested that elevated Cr (>150 ppm) and Ni (>100 ppm) and a ratio of Cr/Ni between 1.3 - 1.5 are diagnostic of ultramafic rocks in the source region. In comparison, Cr concentrations ranges from 112 to 120 ppm (average 171.31 ppm) mostly below 150 ppm and Ni concentrations ranges from 48.9 to 104 ppm (average 70.69 ppm) and Cr/Ni ratios range from 1.63 to 4.37, but mostly above 2.0. This comparison suggests that the existence of huge complexes of felsic source but some samples shows mafic/ultramafic rocks signature in the source region. Reduction in Rb/Sr and Ba/Sr is because of the loss of Sr and feldspar with cumulative weathering and recycling [2] . The concentrations of Rb (mean ~53.4 ppm), Sr (~105) and Sm (~7.45) of the Neogene mudrocks are similarto those of sedimentary suits of High Himalayan region [36] .

REE, Th and Sc are quite beneficialto infer crustal compositions. This is because of their distribution is not considerably influenced by diagenesis and metamorphism as well as is a lesser amount of effect by heavy mineral fractionation than that for some elements, i.e. Zr, Hf, and Sn [19] . REEs enrichment in sedimentary rock is a pointer to the source area determination. REE patterns represent the features of source rocks geochemical attributes, from which sediments are resulted and accumulate within the basin depositional center. fluctu- ation in the REE patterns remain constant, if they derive from a common source. On the other hand, REEs show variable patterns in sediments that originated from heterogeneous source rocks [11] [32] [37] [38] [39] . From the chondrite- normalized REE plot (Figure 3), average REE concentration in Neogene mudrocks samples reflects a pattern alike to PAAS and UCC. Enrichment of LREEs and concurrent with poor HREE concentration are evidence of a felsic igneous source [11] . Ratios such as Th/Sc, La/Sc, and Th/Co are significantly dissimilar in felsic and basic rocks and may limits on average provenance composition [29] [32] [40] (Table 7). The Th/Co, Th/Sc and La/Sc ratios for Neogene mudrocks from this study were compared to those of felsic and basic rock- derived sediment (fine fraction) upper continental crust (UCC) and after [32] [39] ; (Cullers et al. 1988) [41] (Table 8). These comparisons also specified that such ratios came within the range of felsic source rocks. As a consequence of their immobile characteristic, trace elements in sediments reflect source rock composition.

Zr, Nb, Hf, U, Th and Y are high field strength elements, which are preferentially partitioned into melts during crystallization. This mechanism results in these elements being enriched in felsic rather than mafic sources. In contrast, Co, Sc, and V are more concentrated in mafic than in felsic source rocks [11] [42] [43] . These elements are thought to reflect provenance compositions as a consequence of their generally immobile behavior [11] .

On Sc-Th scatter diagram (Figure 4), most of the Neogene mudrocks plot in the field of felsic composition although few samples inhabit a field that bears the characteristics of intermediate composition. The origin from the Indo-Burman Ranges could also be probable in part, e.g. Uddin and Lundberg (1998) [24] showed the evidence that ophiolitic detritus could be resulted from the suture zone of the Indo-Burman Ranges.

Generally, there are Four groups of provenance: mafic and less-intermediate igneous (P1), intermediate igneous (P2), felsic igneous (P3), and quartzose sediments of mature continental provenance (P4). To conclude provenance, Roser and Korsch (1988) [4] proposed unstandardized discriminant function scores of the samples (F1 and F2) for major elements [4] were schemed following the boundaries flanked by fields (P1-P4) (Figure 5).

Following equation used for discriminant functions:

Discriminant function 1= (−1.773.TiO₂) + (0.607.Al₂O₃) + (0.760.Fe₂O₃) + (−1.500.MgO) + (0.616.CaO) + (0.509.Na₂O) + (−1.224.K₂O) + (−9.090);

Discriminant function 2 = (0.445.TiO₂) + (0.070.Al₂O₃) + (−0.250.Fe₂O₃) + (−1.142.MgO) + (0.438.CaO) + (1.475.Na₂O) + (−1.426.K₂O) + (−6.861).

(P1 first-cycle basaltic and minor andesitic detritus, P2 dominantly andesitic materials, P3 acid plutonic and volcanic detritus, and P4 mature polycyclic quartzose detritus) Most of the Mudrocks from Sitakund anticline are located within the P4 field, which signifies a recycled mature polycyclic quartzose detritus.

The sediment repository preserved in the Bengal Basin is predominantly a huge delta complex fed by the coalesced Ganges and Brahmaputra rivers. It preserves (16 - 22 km) thick sequence of Cenozoic sediments [23] [44] [45] [46] from oldest to youngest, the Sylhet, Kopili, Bhuban, Bokabil, Tipam and DupiTila Formations, which show facies evolution from marine through deltaic to fluvial environments. The Cenozoic sedimentary succession of Bangladesh provides a storehouse of Himalayan erosion [47] . The enormous stack of inter-bedded sandstones and mudrocks could have been consequent from rapid erosion of quick rising Himalayas and Indo-Burman Ranges. The occurrence of granitic plutons, Mesozoic flysch deposits, ophiolite rocks, and Tertiary molasse sediments are usual in the Eastern Himalayan structural belt [48] . In the Indo-Burman Ranges, thick Eocene to Oligocene turbidite successions and Upper Miocene to Pleistocene molasses sediments [24] are the important rocks successions. In Hatia Trough and Chittagong Hill Tracts, the Neogene facies are exposed. Although the Hatia Trough currently remains a site of sediment deposition, the Chittagong Hill Tracts consist of sediments deposited in the Bengal Basin, and subsequently uplifted and incorporated into the accretionary prism during subduction of the Indian oceanic plate beneath the Burma platelet to the east [45] . The relative contributions of huge pile of sediments to the Bengal basin from the Himalaya, Burman margin and Indian craton and Shillong Plateau, are disputed [1] [46] [49] [50] [51] . The low temperature Ar-Ar ages of detrital white mica from the Neogene sandstones of Surma Group are diagnostic of the youngest cooling events which can be correlated with early cooling ages from High Himalayan Crystalline rocks [52] . On the basis of sand petrography and lithofacies maps, it is evident that the Miocene sediments were transported from the immediate east, comprising the Indo-Burman Ranges too and produce a vivid record of unroofing of the eastern Himalaya/Indo-Burman Ranges [1] [24] . Most probably Himalayan terrain, particularly Eastern Himalaya could be documented as the principal source area of the Neogene mudrocks from Sitakund anticline. Theflysch successions which is comprised of Recycled sediment material of the Indo-Burman Ranges could also be amalgamated with the sediments of Himalayan origin within the deltaic sediment suits.

Highly weathered granitic gneissic terrain and/or pre-existing sedimentary terrain could be the source of sediments [4] . Weathering that occurs in the hinterland is estimated as CIA. To determine the weathering history of sedimentary rocks, Nesbitt and Young (1982) [10] recommended the CIA value (Chemical Index of Alteration) by means of molecular proportion of some bulk elements. Progressive alteration of plagioclase and potassium feldspars to clay minerals examined by chemical index of alteration (CIA). Average concentrations of alkali and alkaline earth elements varies in the course of weathering with chemical alteration [9] [10] .

The following equation was used to determine CIA value:

Where CaO* stands for the amount of CaO united in the silicate phases.

(CaO* = CaO-10/3) [8] .

Lack of weathering in samples represented by low CIA values (50 or less) whereas high values (76 - 100) specify a greatly chemically weathered source region [10] [53] . CIA values for the Neogene mudrocks vary from 67.81 to 77.57 with an average 74.41 indicating significant weathering at the source areas. The obtained average CIA value (~75) is higher than that of the CIA value (50) of upper continental crust. The CIA values are also plotted in Al₂O₃ (CaO* + Na₂O) - K₂O (A-CN-K) diagram (Figure 6). In the A-CN-K diagram, values of the samples occupy near the Al₂O₃ portion, far from the line linking plagioclase and K-feldspar. The acquired CIA values are symptomatic of the weathered nature of some of the minerals incorporated in Mudrocks. The negative correlation between CIA and K₂O/Al₂O₃ recommends that clay fraction generally consists of K-bearing minerals. Intensely weathered soils tends to be enriched in TiO₂ due to its low solubility. However, our analysis shows that TiO₂ concentration declines with rising CIA values. The observation advocates that these sediments derived from a TiO₂ dwindling felsic source rocks [54] .

From the relation, Na₂O/K₂O <1, the mudrocks seem to be mature (Table 9). The Th/U ratio differs from 3.5 to 4.0 for most upper crust rocks [8] . Enrichment of U is commonly found in anoxic sediments. During weathering and sedimentary recycling under oxidizing conditions, insoluble U⁴⁺ ions are converted into soluble U⁶⁺ ions. Higher Th/U values are indicative of dissolution and loss of U during sedimentation [8] [11] . Low Th/U ratios indicate the enrichment of U in the sediments. In sedimentary rocks, Th scatters as a trace element in heavy minerals (e.g. zircon and monazite). U is not copious in coarse-grained inorganic sedimentary rocks (e.g. quartzite and arkose); the range generally is from 0.5 to 1.5 ppm but can increase with increasing clay minerals [55] . The Th/U ratio is a significant index for checking kaolinite content, which upsurges with elevated Th/U values. In sedimentary rocks, Th/U values greater than 4.0 may specify intense weathering in source areas or sediment recycling. The Th/U ratios in the Neogene mudrocks range from 4.87 to 8.16, with an average of 5.99, indicating the derivation of these sediments from the recycling of the crust. (Figure 7) shows a typical distribution similar to the average values of fine grained sedimentary rocks testified by Taylor and McLennan (1985) [8] and follows the normal weathering trend [11] .

It is most likely that the sources for the Neogene mudrocks were recycled sediments and have undergone significant weathering. Mudrocks containing plagioclase (~9%) [52] may indicate insignificant chemical weathering during sedimentation within the basin [56] , however the CIA values of mudrocks are indicative of the significant weathering in their source. The calculated CIA values for the Neogene mudrocks are very much similar to the CIA values of the Yamuna River System sediments in the Himalaya (~51 to 69; average ~60) [57] .

Trace elements and Major are crucial pointers for deducing tectonic setting. Bhatia (1985) [2] proposed that immobile trace elements (e.g. Zr, La, Nb, Th, Y, Sc) in mudrocks reserve the signs of tectonic setting and source rocks. He distinguished four major tectonic provenances (Oceanic island arc, continental island arc, active continental margin and passive margin) based on the Th, U, Nb, La, Cr, Ni concentrations and the ratio of Th/U and La/Sc. Based on Bhatia’s (1985) [2] idea, the trace elements of the samples recommend diverse tectonic setting varies from continental island arc to active continental margin to passive margin. The ratio of La/Sc and content of La and Nb concentrations can be roughly matched with the contents of an active margin setting. Definite trace elements connecting to tectonic settings of Bhatia (1985) [2] were not conclusive for all four tectonic settings proved by McCann (1991) [60] . In Accordance with the idea of Bhatia (1985) [2] , the active and passive continental margin Mudrocks are discriminated from other mudrocks by their significantly greater Nband Th. The active continental and passive margin Mudrocks are alike in most immobile trace elements, and can be differentiated from each other by higher Ni and Cr copiousness for the passive margin setting.

The increase in the Cr and Ni abundance for passive margin mudrocks is due to the enrichment and adsorption of these elements with the increased phyllosilicate content. The passive-margin comprised Atlantic-type rifted continental margins developed along the edges of the continent, remnant, ocean basins adjacent to collision orogens, and inactive or extinct convergent margins. Intra- cratonic and rift-bounded grabens (e.g. the Benue trough) were formed on a thick continental crust which are included in the passive-margin type tectonic setting. La-Th-Sc, Th-Sc-Zr/10, and Th-Co-Zr/10 are important ternary plots for determining tectonic setting although a La-Th-Sc plot cannot discriminate between active and passive continental margins; Th-Co-Zr/10 and Th-Sc-Zr/10 can differentiate these settings (Figure 8). These ternary plots can generally discriminate between the following tectonic settings: oceanic island arc (A), continental island arc (B), active continental margin (C), and passive margin (D) [5] [7] . The Th-Co-Zr/10 and Th-Sc-Zr/10 diagrams conclude that the analyzed mudrocks be owned by an active continental margin tectonic setting with high Zr/Th ratios. Another discrimination diagram was proposed by Roser and Korsch (1986) [3] , using K₂O/Na₂O against SiO₂. Intermediate values of K₂O/Na₂O and SiO₂ indicate a change from PM, ARC to ACM. Intermediate K₂O/Na₂O and SiO₂ values indicate active continental margin tectonic environment of deposition for the analyzed Neogene mudrocks (Figure 9).

In this study, geochemical data were used to elucidate paleodepositional environments for Neogene mudrocks. Differing degrees of trace and REE element enrichment may reflect differences in depositional environment during accumulation. In the past, trace-element ratios such as Ni/Co, V/Cr and V/(V + Ni) have been used to evaluate the paleoredox conditions by various workers [16] [61] [62] . Dypvik (1984) [63] and Dill (1986) [64] have also used the Ni/Co ratio as a redox indicator. Jones and Manning (1994) suggested that Ni/Co ratios <5 inferred oxic conditions, 5 - 7 dysoxic conditions and >7 suboxic to anoxic con- ditions. In the present study, Neogene mudrocks have moderate Ni/Co ratio ranges from 2.51 to 6.75 indicating poor oxic to dysoxic condition. Vanadium, which is generally found in sediments deposited in reducing environments, may be bound to organic matter by the incorporation of V4+ into porphyrins [62] . V also may occur when adsorbed onto clay minerals, an association that probably results following its burial [65] .

Cr is thought to be associated only with the detrital faction (Dill 1986) [64] and is not influenced by redox conditions, thus high V/Cr values (>2) are thought to indicate anoxic conditions. According to Jones and Manning 1994 [16] , V/Cr ratios <2 infer oxic conditions, 2 - 4.25 indicate dysoxic conditions and >4.25 infer suboxic to anoxic conditions; in addition, V/(V + Ni) ratios greater than 0.84 suggest euxinic conditions, 0.54 - 0.82 represent anoxic conditions and 0.46 - 0.60 represent dysoxic conditions. In the present study, the V/Cr ratios of all samples (Neogene mudrocks) varies between 0.45 and 1.00, which imply that these Mudrocks were deposited in an oxic depositional environment.

Cu/Zn and (Cu + Mo)/Zn ratios have been put forward by Hallberg (1976) [66] as redox parameters. According to Hallberg (1976) [66] , high Cu/Zn ratios indicate reducing depositional conditions, while low Cu/Zn ratios suggest oxidizing conditions; he showed that high values should indicate more reducing conditions in the depositional basins than lower values, which may indicate more oxidizing conditions. Thus, the low Cu/Zn ratios for Neogene mudrocks (~0.46 - 0.98), respectively (Table 10) indicate that the Mudrocks were deposited under oxidizing conditions. The U/Th ratio may be used as a redox indicator with U/Th ratio being higher in organic-rich mudstones [16] .

Low contents of U are generally found in sediments deposited in oxygenated conditions in marine environment, whereas high U contents are found in sediments from the oxygen minimum zone [61] [67] thus, the U/Th ratio may be used as a redox indicator [16] . U/Th ratios below 1.25 suggest oxic conditions of deposition, whereas values above 1.25 indicate suboxic and anoxic conditions [17] . In this study, the samples have low U/Th ratios (~0.12 - 0.53) indicating that samples were deposited in an oxic environment. It is suggested that thresholds established for paleoredox indicators in these studies should not be applied strictly, but that relative differences in these indicators collectively can infer variations in the degree of anoxia.