Two types of rodingitization (static and dynamic) are observed in the rodingites of the ophiolite north of Nain. Two stages have been occurred in the formation of static rodingites. At the initial stage, epidote, prehnite and hydrogrossular have crystallized respectively at the expense of plagioclase, with the increase of Calcium content rodingite forming fluid. In the advanced stage, xonotlite at the expense of plagioclase, and Mg–chlorite, tremolite and secondary diopside, at the expense of pyroxene, have formed simultaneously with an increase of Si content of rodingite forming fluid. The high content of vein xonotlite, in the dynamic rodingites, shows that the CaO/SiO2 ratio in the fluid is first close to one, but with time, it reduces to less than one and prehnite and pectolite have crystallized. In the dynamic rodingites, due to the low variations of rock–forming fluids, the mineralogy of dynamic rodingites do not vary much. In contrast, the mineralogy of static rodingites display variation, indicating the changing in composition of rock–forming fluids.

In north of Anarak area, in the upper Proterozoic ophiolite, exist Massive and Vein type Rodingites. Vein type rodingites have fonned in two phases. Massive or Static rodingites have fonned during oceanic crust spreading and ophiolite fonnation, and Vein type or Dynamic rodingites have fonned during Anarak ophiolite emplacement and tectonic activities. Abundance order of minerals in massive rodingites is Garnet (Chromian- Andradite), Idocrase, Chlorite, Diopside, Prehnite and Epidote (decreasing). In the first phase of vein type rodingites, the abundance order of minerals is Diopside, Chlorite, Idocrase, and Garnet (Ti-Andradite), and in the second phase is Diopside, Chlorite and Garnet (Andradite). Petrography and geochemical study of minerals show that, during the fonnation of massive type rodingites, the activity of Calcium, Iron, and Chromium ions in fluids, and during the fonnation of first phase of vein type rodingites, the activity of Calcium, Silicon, Magnesium, Aluminum, Titanium, and OH- ions in fluids, have been increased. Geochemistry of second phase of vein type rodingites is similar to first phase, but because of absence of Idocrase, and low Titanium in Andradite structure, the activity of Iron, Titanium, and Aluminum ions, is lower than first phase. Generally the diversity of minerals in massive type rodingites is more than vein type rodingites.

Gabbroie dykes hostes in serpentinite of Dehshir-surk ophiolites have undergone hydrothermal alteration, well known as serpentinization. Serpentnization of primary minerals (Pyroxene, olivine) introuduces Ca+2 to hydrothermal fluids. These Ca-rich fluids are responsible for rodingitization of Gabbro dykes introuded in serpentinite basement.There are two distinct serpentinitization stages: dynamic and static. and it is concluded the rodingitization is a polygenic processse. The rare mineral pectolite [Na Ca2 Si3 O8 (OH)] is formed due to Na-metasomatism in the latest stage of hydrothermal processes.

Mineral paragenesis of rodingitized basic rocks of Iranian ophiolites are presented and metasomatic reactions between Ca+2 bearing aqueous fluids issued during serpentinization of host ultramafic rock – with magmatic minerals of basic rocks leading to present paragenesis of rodingites are discussed. It is concluded that Ca+2 rich aqueous fluid in equilibrium with serpentinite has high Ca+2 chemical potential to react with magmatic minerals of basic dykes resulting in lowering the free energy of system, appearance of a new mineral paragenesis and total or partial conversion of basic dykes to rodingites. A feedback mechanism is proposed to account for inter-relationship of serpentinization and rodingitization.

Two types of rodingitization (static and dynamic) are observed in the rodingites of the ophiolite in the North Of Nain. Two stages have occurred in the formation of static rodingites. In the initial stage, epidote, prehnite and hydrogrossular have crystallized respectively, at the expense of plagioclase, with the increase of calcium content rodingite forming fluid. In the advanced stage, xonotlite in the expense of plagioclase, and Mg chlorite, tremolite and secondary diopside, at the expense of pyroxene, have been formed simultaneously with an increase of Si content of rodingite forming fluid. During rodingitization, the Ca and OR content, have increased, whereas the amounts of K, Al and Na are reduced. Mn, Fe and Mg values are slightly reduced but Si remains constant.

Around Soleymanieh village in the NE of Sabzevar, there are a numerous gabbros and microgabbros dykes that have interruped Sabzevar's ophiolites. Most of these dykes turn from black to green, white, yellow and reddish. The surrounding ophiolites have highly altered to serpentine, too.The petrographic studies of discoloured dykes show that, olivine, clino- pyroxenes, orthopyroxenes and calcic plagioclases, (high energy level minerals) have been converted to: wolastonite, prehnite, chlorite, epidote, hydrogrossular, pectolite, and xenotlite (low energy level minerals).Furthermore: XRD, thermic analysis and micropropic studies confirme the mineralization studies and rodingite reactions recognized by polarized microscope. Assemblages minerals and textures show that this complex is a rodingite association. Generally, rodingite mechanism start with serpentinization of olivine and pyroxenes in harzburgites and lherzolites and release of Ca+2 from their structures. These Ca+2 cations can not be accommodated in serpentine crystal structure, therefore, they are concentrated in the fluid associated with serpentinization. Oversaturated fluids of calcium, and with low amount of CO2, under suitable condition, (presence of reactional rocks like gabbros) react with above meantioened rocks and form calcium rich minerals. These fluids will react with basic roch minerals especialy Plagioclasis and creat a host of roddingites minerals (Xenotlite, grossular, Pectolite and others). In Some cases, somme minerals, such as pectolite and xenotlite are replaced in the form of veins within rodingites.

The protolith of rodingitic dykes of Naien area are pegmatoidic gabbros, microgabbros, dolerites and fewer amphibolites. Textural features and thickness are effective parameters for rodingitization of these dykes. Slight thickness of microgabbro and pegmatoidic dykes have more undergone rodingitization and have passed the primary to advanced stages of static rodingitization (due to the presence of epidote, Prehnite and hydrogrossular, Mg-chlorite, tremolite and secondary diopside replacement minerals as well as dynamic rodingitization (Owing to the xonotlite, prehnite and pectolite vein mineral), while doleritic and amphibolitic dykes have only passed the primary stage of static rodingitization (due to the presence of epidote, Prehnite and hydrogrossular).

Jandaq ophiolite suites are covered by metamorphic rocks that are marbles and schists. This old ophiolitic association has passed different phases of serpentinization and metamorphism. In this rock association, gabbroic dikes cross cut the serpentinized mantle peridotites. Joints and cracks of brittle gabbroic dikes are filled by veins that are light in color. These veins are formed after metamorphism and serpentinization. These coarse grain rocks are free from deformation and foliation, and are formed by calcite, prehnite, epidote, clinopyroxene and chlorite. The most important mineralogical characteristic of these veins is existence and considerable amount of calcite, that is the evidence of high f CO2 in minerals bearing fluid. Vein enclosing gabbros, are metamorphosed in amphibolite facies (2.7 to 9 kbar pressure and 630 to 750 of C temperature), and then pass through a retrograde metamorphism in green schist facies.

The Surk ophiolitic melange, as a narrow belt, is located in western part of Yazd province, between the southwest of Central Iran and Urumieh-Dokhtar magmatic arc, along Naein-Dehshir-Baft fault. This ophiolitic melange consists of mantle peridotites, gabbro, diabasic dykes, quartz andesite, dacite, serpentinite, listwaenite, rodingite, chert and Upper Cretaceous limestones. Petrography and mineral chemistry of mantle peridotites reveal incongruent melting of orthopyroxenes, the formation of excess olivines, the high value of Cr# in spinels of harzburgite and dunite and the occurrence of pargasitic amphibole in lherzolites in the studied ophiolite. All of these evidences suggest melt/oceanic lithosphere reaction. The reactive melt originated from a subducted slab that decreases the melting temperature of the lithospheric mantle and leads to widespread ascending melt/wall rock reaction. The peridotites of this ophiolitic melange consist of harzburgite, dunite and lherzolite in decreasing order. The ophiolite is a harzburgite type ophiolite (HOT) showing characteristics of supra subduction zone ophiolites (back-arc basin).

Anarak ophiolite, belonging to Paleozoic, formed along with the tectonic evolution of the Paleo-Tethys Ocean, consisting of meta-peridotites of mantle and crust, cumulate rocks, massive gabbros, pillow lava, basic and ultrabasic dikes, rodingite and listwanite covered all by schist and marble units. The olistolithic patches of Anarak ophiolite have commonly exposed in Sebarz schist, within the sole of Chah-Gorbeh complex. Olistoliths composed of listwanite, meta-mafic, serpentinite and meta-peridotite olistoliths varying from centimeter to several hundred meters in size. The results of electron microprobe analyses show that the fundamental rock-forming minerals of the listwanitized olistoliths are chromian spinel and pyroxene, secondary minerals including calcite, garnet, tremolite, chlorite, magnetite and opaque minerals. Meta-mafic olistoliths composed of chromian spinel, sphene, epidote, chlorite and opaque minerals. Serpentinized olistoliths consist of chromian spinel, magnetite, tremolite, talc and chlorite. It also shows that the meta-peridotite olistoliths composed of chromian spinel, chrome-bearing magnetite, chlorite, calcite, garnet and antigorite. Based on the geochemical analyses, Cr# in the listwanite patches, meta-mafic, serpentinite and meta-peridotite olistoliths are 87. 40-97. 92, 49. 38-51. 89, 49. 22-60. 05 and 29. 76-55. 97 respectively with very low amount of TiO2. The different in chemical composition of minerals in the North Anarak complex shows different petrogenesis for ophiolitic olistoliths suggests characteristic of the MORB and/or supra-subduction zone.