Today, because of advances in the extraction of base metals from non-sulfide ores, these deposits have become particularly valuable and found an important economic status. Recently, much research has been done on them such as the research conducted by   -    . The Pb-Zn ore deposit Ahmadabad, located at 80 km North-East in the metallogenic Bahabad belt belonging to the Central Iran structural zone, is considered one of the important ore deposits because of high abnormality of its Mo element (Figure 1). The ore deposits of the said belt are in the form of a straband Vein, Veinlet, Space Filling and Karst in the carbonate hosting rock  . The relative enrichment of the carbonate hosting rock compared to base metals and also limitation of mineralization to this lithology can raise the hypothesis of the relationship between ore deposits and carbonate hosting rocks. The aim of this study is finding the existence and/or non existence of any significant genetic relationship between ore minerals and carbonate rocks. To achieve this aim, normalized patterns of REEs were used.
2. Study Methods
Petrography and mineralogy studies of 30 thin-polished sections were performed in the geology laboratory of Tarbiyat Modarres University. To find out the existence of a genetic relationship, Rare Earth Elements related to 8 samples of host and non-host carbonate units and minerals were analyzed in ALS lab through ICP-MS technology. Findings were processed and then studied.
3. Geology Setting
Ahmadabad ore deposit was placed in Posht-e-Badam block in Central Iran Zone. Lithologically, the rocks of this zone were composed of dolomitic limestone sedimentary sequence, clastic and evaporative belonging to Triassic and Jurassic periods. Dolomitic limestone and dolomites of Shotori and Nayband Formations are the most important units in this zone and host minerals in Posht-e-Badam block. Therefore, the possible genetic relationship between these units and minerals are investigated in this paper.
4. Lithology of Carbonates and Mineralogy
Carbonates of the area consist of limestone, limestone-dolomite and dolomites
Figure 1. The position of ore deposit Ahmadabad among Zn-Pb ore deposits of Triassic period in the metallogenic zone of Bahabad (adapted from  and relevant modifications).
units of Shotori Formation (TRSh1-4) and the limestone unit belonging to Nayband Formation (TRnb2) (Figure 2(a)).
The TRSh1 unit is composed of thin, grey layers of dolomite limestone. Microcrystalline mud forms the highest volume of this rock. Fractures due to tectonic performance are filled with sparitic crystals (Figure 2(b)). The TRSh2 unit is the substrate of the mineral-hosting rock. This dolomite-limestone unit is made of an average to thick layer, ecru or cream in color, and has an inhomogeneous tissue; a microbial activity can also be seen in it (Figure 2(c)). Brown mass dolomites form the lithology of TRSh3 unit of mineral. The unit has a progressive edge with its lower and upper layers. In a thin scale, microcrystallines are the main constituents closely followed by sparitic crystals (Figure 2(d)). The TRSh4 is youngest carbonate unit of Shotori formation. The upper edge of this unit leads to gypsum-marl layers of Nayband Formation. Mesocratic microcrystallines constitute the central part which are seen in some areas in form of round
Figure 2. (a) General view of carbonate units in the area and the mine position in relation to them in Ahmadabad area Thin section of (b) TRSh1 unit; (c) TRSh2 unit; (d) TRSh3 unit and (f) TRSh4 unit.
to oval ploids in different sizes. The unit, influenced by tectonic phases, has been severely fractured and filled by sparitic crystals (Figure 2(e)). The carbonate layer TRnb2 is cream in color and contains large quantities of brachia macrofossils. The sequence of dark and light layers is detectable in thin sections. The light parts are made of sparitics and the black parts are made of microcrystallines (Figure 2(f)).
Pb, Zn, Sr and Mo Non-sulfide minerals are the most important minerals of Ahmadabad mine ores made due to weathering and conversion of primary sulfide minerals. Examples of the latter include galena, sphalerite and pyrite which have been crushed due to tectonic phases leading to formation of non-sulfide minerals. Calamine minerals (Hemimorphite and Hydrozensite) (Figure 3(a)),
Figure 3. (a) Calamine non-sulfide mass ore deposit: Hydrozensite and Hemimorphite (Ore1) (b) Red non-sulfide mass ore deposit (Wulfenite-Cerussite-Celestine-Fe Oxide and Fe Hydroxide (Ore2) in Ahmadabad ore deposit.
Celestine, Cerussite and I (Figure 3(b)) are the most important non-sulfide minerals of the ore deposit.
5.1. Geochimestry of Rare Earth Elements in Carbonate Units
Samples of all carbonate units were normalized in relation to North American shale (NASC)  , upper continental crust  and chondrite C1  . The rare earth elements distribution diagram obtained in relation to North American shale and upper continental crust indicates depletion of all rare earth elements with respect to these two standards; so that all units in both distribution patterns are placed under axis 1. This depletion for carbonate stratigraphic units takes
place in the range of between to times the upper continental crust. The
highest depletion belongs to ThSh2 unit and the lowest is related to TRnb2 unit.
The average content of rare earth elements in minerals is times the upper
continental crust. Samples of carbonate units in the area show the highest depletion compared to North American shale and this takes place in the range be-
tween to times the NASC. Figure 4 indicates that all samples of carbo-
nate rocks have a uniform distribution pattern compared to North American shale and the upper continental crust. Also the depletion of light and rare earth elements is lower than that of heavy ones and all LREE patterns towards HREE show a downward trend. All samples have increased in relation to Eu and Tm elements and decreased with respect to Yb. Among stratigraphic units of the area, the distribution pattern of rare earth elements in TRSh2 unit (substrate of the host layer) is the closest and the most similar to minerals. The same distribution trend can also be seen in the normalized pattern in relation to North American shale. Distribution of such elements, contrary to the two previous patterns, indicates an enrichment of LREE elements in carbonate units, so that all units except the TRSh2 unit are placed above 1. This enrichment in the TRSh2 unit includes only four elements (Pr, Ce, La, and Nd). The normalized pattern in relation to chondrite indicates the decreasing trend of rare earth elements from
LREE towards HREE in all units and mineral samples. The relation reveals
the rise and enrichment of light rare earth elements to heavy ones. This relation was separately calculated for carbonate units. The values obtained vary from 51 times in TRnb2 unit to 11 times in TRSh4 unit. The average value in carbonate units is equal to 14.24 (TRSh2: 12.5, TRSh1: 17.36, TRSh3: 15.94, TRSh4: 11.17 times); this shows the relative high enrichment of LREEs compared to HREEs. The ratio for minerals is 14/63 in average and very close to average value of all carbonates.
Comparison of distribution patterns between minerals and rocks in the area represents undeniable similarities between these materials and carbonate rocks.
Figure 4. (a) Normalized pattern of rare earth elements of Ahmadabad carbonate units in relation to North American shale standard, (b) compared to upper continental crust and (c) compared to Chondrite C1.
Among these, the greatest similarity is related to TRSh2 limestone-dolomite which is the substrate of host unit (TRSh3) (Figure 4).
5.2. Comparison of Geochemistry of Rare Earth Elements in Ores and Carbonate Rocks
After determining the genetic relationship of Ahmadabad ore deposit with carbonate units to better show this relationship, each carbonate unit was separately investigated with minerals. These units were normalized in relation to upper continental crust  . Ores (Ore1 & Ore2)-TRSh1 unit (Figure 5(a)), Ores-
Figure 5. Comparison diagram of rare earth elements in Zn-enriched ores (calamine) (ore1) and Pb-enriched ores (cerussite) (Ore2) with carbonate units; (a) TRSh1 unit; (b) TRSh2 unit C) TRSh3 unit.
TRSh2 (Figure 5(b)), Ores-TRSh3 (Figure 5(c)), Ores-TRSh4 (Figure 6(a)) and Ores-TRSh4 (Figure 6(a)) and Ores-Ores-TRnb2 (Figure 6(b)). As diagrams indicate, mineral samples are very similar to all kinds of carbonate samples and the similarity of TRSh2 unit was the highest (Figure 5(b)). Diagrams (Figure 5 and Figure 6), show the significant decrease of potassium in comparison to carbonate rocks. This decrease corresponds to the amount of clay minerals in carbonate rocks and minerals. This reduction is clearly shown as a severe depletion of potassium in the diagrams relating to minerals.
Ahmadabad non-sulfide Pb-Zn ore deposit belongs to metallogenic area Bahabad in the Central Itan structural zone. This mineralization is non-sulfide and the most important minerals include galena, sphalerite and pyrite that, after
Figure 6. Comparison diagram of rare earth elements in Zn-enriched ores (calamine) (ore1) and Pb-enriched ores (cerussite) with carbonate units; (a) TRSh4 unit and (b) TRnb2 unit.
supergene processes, have become non-sulfide Pb-Zn minerals and Mo. The normalized patterns show that, with respect to distribution of rare earth elements, minerals are the most similar to TRSh2 unit among carbonate units. The results show that ore creating fluids and host rocks belong to a joint basin and all are formed under similar condition.
1) It is suggested to use SEM-EDS method to recognize the combination of carbonates types in ore deposit. Through this method, it is possible to examine amount of replacement of ZnO in carbonate rocks. Besides showing different types of carbonate rocks, the current results can determine effects of metal-rich fluids on these rocks.
2) In order to accurately determine of minerals types used QPA method.