Iron deposits from Benxi area including Gongchangling, Nanfen and Waitoushan are the typical BIF-hosted deposits in Northeastern China, which hosted within the Neoarchean middle Anshan Group. Recent studies of the iron deposits from Benxi area have formed the consistent view that they belong to Algoma-type BIF, but have the controversy about the tectonic nature during Archean BIF formation period because of the multiple deformation and metamorphic processes. Some of scholar considered that BIF produced in mid-oceanic ridge and others thought that it produced in an island are or back-arc basin (Dai, Zhang, Wang, Liu, Cui, Zhu, & Xiang, 2012; Feng, Zhou, & Xiao, 2009; Liu, & Jin, 2010; Cui, Sun, Zhang, Gu, Zhou, & Sun, 2012; Zhang, Yang, Zhou, & Shi, 2013; Sun, Zhu, Tang, Zhang, & Han, 2014; Wang, Xia, Zhao, Fu, & Hou et al., 2013) [1]-[7]. In addition, the known reports on the Nanfen BIF is small while the detailed study on the Gongchangling and Waitoushan BIF-hosted iron deposits is carried out by many geologists.

In fact, despite extensive research on BIF around the world in the past few decades, many aspects of their origin including tectonic setting remain unresolved (Bekker, Slack, Planavsky, Krapez, Hofmann, Konhauser, & Rouxel, 2010) [8]. Alogma-type BIF are closely associated with volcanic activity (Gross, 1980) [9], and so geochemical features of their volcanic wall rocks are widely used to constrain the tectonic setting of BIF. Chlorite amphibolites are important metamorphic volcanic rock of the middle Anshan Group stratigraphy and are in contact with BIF in the Nanfen iron deposit.

In view of the close links between Algoma-type BIF and subjacent volcanism, this study has focused on establishing the nature and distribution of metamorphic volcanic rock within the middle Anshan Group of Nanfen iron deposit. We report and discuss in this paper the results of a geochemical study on chlorite amphibolites from the Nanfen iron deposit in detail, and also reveal its tectonic significance for the formation environment of the BIF in the study area.

The Benxi iron producing area is located in Archean greenstone belts of the northeastern margin of China. The strata in this area included Archean Anshan Group, Proterozoic Liaohe Group, Neoproterozoic, Paleozoic, Mesozoic and Neozoic strata. Archean geological bodies are exposed in Gongchangling, Nanfen and Waitoushan area etc., and are mainly composed of about 30% iron-bearing rock series and 70% granitic rocks (Figure 1).

The Anshan Group strata are hosted between two phases of Archean granite, which have ages of about 3.0 Ga and about 2.45 Ga respectively, as “islands” (Zhai & Santosh, 2011; Zhou, 1994) [10] [11]. The iron-bearing rock series is restricted between these two phases of granite emplacement. BIFs in the Benxi area occur in the Archean middle Anshan Group which is mostly distributed from Benxi to Liaoyang area, and their formation age mainly concentrate between 2.50 - 2.55 Ga (Dai, Zhang, Wang, Liu, Cui, Zhu, & Xiang, 2012; Wan, Dong, Xie, Wang, Song, & Xu et al., 2012) [1] [12]. Lithologically the middle Anshan Group is made up mainly of amphibolites, amphibole-bearing gneiss and biotite leptynite, also interbedded with muscovite quartz schist, and chlorite quartz schist (Zhou, 1994) [11]. This iron-bearing rock series is characterized by multi-layers of iron ore, iron minerals dominated by oxide with minor silicate and a general close association with meta-basalt owing to greenschist-lower amphibolite facies metamorphism, which includes the Gongchangling, Nanfen and Waitoushan iron deposits, etc. (Zhou, 1994) [11].

At the Gongchangling iron ore deposit, the iron-bearing rock series can be divided into six units from bottom to top, which include the bottom amphibolite, bottom schist, lower iron ore (composed of the first layer of iron ore, the schist and the second layer of iron ore), biotite leptynite zone (interlayer with the third layer of iron ore), upper iron ore (composed of fourth layer of iron ore, lower plagioclase amphibolite, the fifth layer of iron ore, upper plagioclase amphibolites and the sixth layer of iron ore) and siliceous rocks (Wang, Xia, Zhao, Fu, & Hou, 2013; Sun, Zhu, Tang, Zhang, Luo, & Han, 2014; Zhou, 1994) [6] [7] [11]. Among them, the main ore types include the low-grade magnetite quartzite, high-grade magnetite quartzite and some of low-grade martite ore. At the Waitoushan iron deposit, the iron-bearing rock series is mainly composed of a suite of plagioclase amphibolites, magnetite quartzite, actinolite quartz schist, actinolite quartzite, and garnet biotite actinolite schist. The iron ore body can be divided into three layers of magnetitie quartzite, which are mainly hosted by plagioclase amphibolitic rocks (Dai, Zhang, Wang, Liu, Cui, Zhu, & Xiang, 2012) [1].

Nanfen iron deposit is in super large scale with simple ore body shape and evenly distributed useful components. This consist of three roughly paralleled ore bodies trending to NW-SE and dipping to the SW at 40˚ - 50˚, which occurs as bedded or stratoid structure interbedded with the chlorite schists and chlorite amphibolites (Figure 1). Their ore-preserving roof wall rock is mica quartz schist and their ore-preserving floor wall rock is chlorite amphibolite and others. The mainly ore mineral is magnetite quartz (Zhou, 1994) [11].

It is clear from the above-mentioned geological analysis that the metamorphic volcanic rocks are hosted by many petrographic varieties of amphibolites (i.e. mainly the plagioclase amphibolites in Gongchangling and Waitoushan, the chlorite amphibolites in Nanfen), which share the same tectonic and metamorphic history. So it can be argued convincingly that amphibolites and iron ore are integral parts of the middle Anshan Group and were therefore formed during the same geological event. Clearly the thinking has changed regarding the provenance of the amphibolites in the middle Anshan Group and further work was regarded as being of utmost importance to better characterize the Benxi iron ore deposits.

Six samples of chlorite amphibolite were collected from the Nanfen iron deposit, covering the interval from the lower part of Fe₁ ore layer to Fe₃ ore layer. Two came from the lower part of the succession associated with the Fe₁ ore layer and other two between Fe₁ ore layer and Fe₂ ore layer, while the rest are from the interbeds between F₃ ore layer (Figure 1(c)). In outcrop the chlorite amphibolites of Nanfen iron deposit are generally celadon or green (Figure 2(a)) and possess a fine grained granoblastic texture as well as a massive structure. Mineral composition is dominated by hornblende and chlorite (Figure 2(b) & Figure 2(c)), minor minerals include epidote, quartz, plagioclase and biotite and others.

All samples were processed and analysed by the Australian Laboratory Services Chemx (Guangzhou) Co. Ltd. For the whole-rock major element analyses, ME-XRF06 assay is used (lithium tetra-metaborate fusion, followed by X-Ray Fluorescence Spectroscopy; detection range of each oxide −0.01% - 100%). Trace element analyses were performed by four-acid digestion (perchloric, nitric, hydrofluoric and hydrochloric), with the dried residue taken up in dilute hydrochloric acid and analysed by ICP-AES. Rare earth element analyses were performed by ME-ICP161 assay (ICP-MS on lithium metaborate fusion beads). The accuracy for the trace element and rare earth element results were both better than 10%RSD. The analytical results are listed in Table 1.

The studied chlorite amphibolites display small variations in major oxide compositions, with SiO₂ = 47.04 -

49.85 wt.%, MgO = 7.70 - 8.79 wt.%, Al₂O₃ = 14.29 - 15.97 wt.%, FeOt = 11.66 - 12.24 wt.%, CaO = 9.38 - 11.37 wt.%, Na₂O + K₂O = 0.66 - 2.10 wt.% and TiO₂ = 0.77 - 0.90 wt.% (Table 1), and are plot into the basalt fields in the diagram of SiO₂ versus K₂O + Na₂O (Figure 3(a)).

The chondrite-normalized REE patterns for chlorite amphibolites are shown in Figure 3(b). As shown in Figure 3(b), the total REE contents are relatively low and samples exhibits nearly flat patterns with (La/Yb)_CN = 0.98 - 1.26, (Gd/Yb)_CN = 0.94 - 1.23 and insignificant Eu and Ce anomaly (Eu/Eu* = 0.81 - 1.09; Ce/Ce* = 0.96 - 1.04).

On the primitive mantle-normalized spidergram (Figure 3(c)), the chlorite amphibolites are characterized by subparallel patterns with the weakly enrichment in LILE (e.g. Th, U and Pb) and depletion in HFSE (e.g. Nb-Ta, Zr-Hf, Ti and Y), where samples have (Nb/La)_N = 0.66 - 0.79, (Th/La)_N = 1.22 - 1.50 and (Hf/Sm)_N = 0.86 - 1.01 (Table 1).

The Nanfen basaltic samples have relatively high LOI, suggesting that these rocks might have undergone some degree of alteration. It is essential to determine the effects of alteration in Archean metamorphic volcanic rocks.

During alteration and metamorphism, the LILE such as Cs, Na, K, Rb, Ba, Ca and Sr are typically mobile. However, the some of major elements such as Al, Ti, Fe, the HFSE (Nb, Ta, Zr and Hf) and REE (except Eu) and others are poorly affected by alteration (Zhang, Wang, Fan, Zhang, & Yang, 2012) [13]. In fact, the REE and HFSE in Nanfen samples show coherent and subparallel concentration patterns, indicating that they still

preserve the signature of original trace element composition (Figure 3(b) & Figure 3(c)). However, some mobile elements such as Rb, Ba and Sr show variable concentrations, which appear to indicate that some LILE have been significantly affected by alteration. So, we used immobile elements to discover the nature of basaltic rocks and selected appropriate discrimination diagrams for protolith reconstruction.

In the Ti/100-Zr-3´Y diagram (Figure 4(a)), all of our samples plot into the overlapping area between MORB-like basalts and arc-like ones, indicating that Nanfen chlorite amphibolites not only have MORB-like compositional characteristics but also have island arc-like ones. Basaltic rocks that combine both the MORB- like characters and arc-like ones may be BABB. The FeOt/MgO-TiO₂ diagram (Figure 4(b)) and Y/15-La/10- Nb/8 diagram (Figure 4(c)) show that the protolith of Nanfen chlorite amphibolites are BABB. In addition, Nanfen samples have Nb/La = 0.69 - 0.82, Ba/La = 5.68 - 85.36, Sm/Nd = 0.33 - 0.36, Zr/Nb = 19.57 - 24.50 and Zr/Y = 2.74 - 3.29 (Table 1), similar to those observed in Okinawa Trough BABB (Nb/La > 0.6, Ba/La > 10, Sm/Nd < 0.3 and Zr/Nb » 18, Zr/Y » 2.9) (Zhang, Wang, Fan, Zhang, & Yang, 2012; Shinjo, 1998) [13] [16].

Most Algoma-type BIFs are part of greenstone belts that have been deformed, metamorphosed, and dismembered. This makes reconstruction of the basinal setting of such BIFs very difficult (Bekker, Slack, Planavsky, Krapez, Hofmann, Konhauser, & Rouxel, 2010) [8]. Recovering of tectonic environment of BIF may be possible through the basaltic volcanic sequences interlayered with Algoma-type BIF. The spatial and temporal association between the BIF and basaltic volcanic sequences indicates a genetic relationship between volcanic activity and BIF.

At present, the tectonic nature during Archean BIF formation period in Benxi area has been long disputed. Based on the geochemical charaters, Feng, Zhou, & Xiao (2009) and Liu, & Jin (2010) [2] [3] considered the protolith of the Gongchangling plagioclase amphibolites to be mid-ocean ridge tholeiite.

Dai, Zhang, Wang, Liu, Cui, Zhu, & Xiang (2012) [1] proposed tectonic environment of its BIF as back-arc basin according to analysis results that protolith of the Waitoushan plagioclase amphibolites is BABB. Through the study on plagioclase amphibolites of middle Anshan Group, Cui, Sun, Zhang, Gu, Zhou, & Sun (2012) [4] and Zhang, Yang, Zhou, & Shi (2013) [5] considered that Gongchangling plagioclase amphibolites had typically the characters of Archean arc basalts and Waitoushan plagioclase amphibolites formed within back-arc spreading environment, and also presented that BIFs of Benxi area produced within the mantle plume-arc tectonic system. Based on the material source analysis about the plagioclase amphibolites combined with biotite leptynites in Gongchangling, Wang, Xia, Zhao, Fu, & Hou (2013) [7] proposed tectonic environment for Gongchangling BIF to be the back-arc basin. Sun, Zhu, Tang, Zhang, Luo, & Han (2014) [6] considered that the protolith of the Gongchangling plagioclase amphibolites to be basic volcanic rock and also proposed that Gongchangling BIF produced within subduction-related arc environment.

As mentioned above, Nanfen chlorite amphibolites originated from back-arc basalts, which have the transitional characters from MORB to arc-like basalt because they are formed by the upwelling upper mantle beneath an ocean ridge system in a supra-subduction zone. At the initial stage of back-arc basin formation, the spreading

axis is located close to the island arc, and the contents of volcanic rocks are similar to the island arc ones. During the development of the back-arc basin, the distance between the island arc and the through increase gradually, and the content of volcanic rocks also become more similar to MORBs. Such a compositional feature is generally acknowledged to be unique to BABB (Ghazi, Moazzen, Rahgoshay, & Moghadam, 2012; Xu, Castillo, Chen, Niu, Yu, & Zhen, 2003; Pearce, & Stern, 2006) [20]-[22]. It is generally believed that HFSE depletions were caused by the immobility of HFSE in fluids derived from the dehydration of the subducting oceanic crust in a convergent margin (Ghazi, Moazzen, Rahgoshay, & Moghadam, 2012; Xu, Castillo, Chen, Niu, Yu, & Zhen, 2003; Pearce, & Stern, 2006; Zhang, Wang, Fan, Zhang, & Yang, 2012) [13] [20]-[22]. In fact, the elemental geochemical signatures for Nanfen chlorite amphibolites, including weakly enrichment in LILE and a depletion in HFSE as well as significant negative Nb-Ta, Zr-Hf, Ti and Y anomalies (Figure 3(c)), could be explained by the introduction of metasomatized melt/fluid released from the subducted slab. Especially, the depletion and differentiation of Nb and Ta are considered to be a result of the initial partitioning and subsequent equilibration between rutile and fluids or melts in a subducted slab (Münker, 1998) [23]. The Nanfen chlorite amphibolites have Nb/Ta ratios of 14.29 - 17.69, reflecting a mixing contribution to the matasomatized fluids and melts (Münker, 1998) [23]. In study area, the back-arc basins may have developed between the subduction zones and provided a favorable sedimentary environment for Algoma-type BIF. The hypothesis about the subduction-re- lated tectonic setting is consistent with the viewpoint of Sun, Zhu, Tang, Zhang, Luo, & Han (2014) [6] for formation environment of Benxi BIFs.

In summary, we suggest that the Nanfen BIF were formed in a subduction-related back-arc basin.

Protolith of chlorite amphibolites from Nanfen iron deposit is BABB.

Tectonic environment for Nanfen BIF is the subduction-related back-arc basin.

We thank the financial support by Research of High-grade Iron Ore Formation Mechanism and Prediction of China (2012CB416800), Research on Archean Geologic bodies Evolution and Metallization of Large Ore Deposit in North Margin of North China Craton (41372098) and Fundamental Research Funds for the Graduate Innovation State Education Ministry (N110601002).

Ende Wang,Changik Han,Jianming Xia,Sunggi Yun, (2015) Geochemistry and Tectonic Significance of Chlorite Amphibolite in Nanfen BIF, Benxi Area, Northeastern China. Journal of Geoscience and Environment Protection,03,54-61. doi: 10.4236/gep.2015.35007