The Bastar Craton occupies a key position in the Peninsular India, being located between three cratonic nuclei of India, the Dharwar Craton in the southwest, the Singhbhum Craton in the northeast, and the Bundelkhand Craton in the northwest. The southeastern and the northern margins of the craton are bordered by the Proterozoic orogenic belts constituting the Eastern Ghats Mobile Belt and the Central Indian Tectonic Zone (the Satpura Mobile Belt), respectively. Analysis of the tectonostratigraphic evolution of the craton indicates the formation of the craton during Paleoarchean Era (~3582 Ma). The Archean evolution of the craton is marked by the development of granite-greenstone belts containing chemogenic sediments (Banded Iron Formations) and gold mineralisation. High-grade gneisses and granulites were developed during three orogenic episodes in the terrane (~2700 Ma Bailadila orogeny, ~2900 Ma Bengpal orogeny and ~3400 Ma Sukma orogeny). The Paleoproterozoic evolution of the craton is gleaned from the record of siliciclastic, volcaniclastics and chemogenic precipitates (carbonates, Banded Manganese Formation, and Banded Iron Formation) on the northern margin of the craton, which were deposited during the Great Oxidation Event (GOE; 2500–2300 Ma) and Paleoproterozoic glaciation (2400–2300 Ma) as well as immediately after the GOE (2050–1850 Ma). Effects of orogenic activities in the adjacent mobile belts are marked by the metamorphic and magmatic activities affecting the rocks at the margin of the craton. The Satpura orogenic event on the northern margin of the craton led to the amalgamation of the Bastar Craton with the Bundelkhand Craton at ~2250 and ~2100 Ma, forming the major part of the Peninsular India. Orogenic collapse (extension) developed basins transverse to the orogenic trend, where clastic, volcaniclastic and chemogenic sediments (Khairagarh and Chilpi Groups) were deposited. The southeastern margin of the craton has records of migmatisation and granite emplacement during the Eastern Ghats orogeny at ~1700 Ma. A number of sedimentary basins, aligned along a line parallel to the Eastern Ghats Mobile Belt, were developed during the orogenic collapse of the Eastern Ghats. Later orogenic activities along the Eastern Ghats were responsible for the development of depositional hiatus/unconformity within these sedimentary basins of the craton. Mafic dykes of different generations (2400 Ma, 2100 Ma and 1890 Ma) cutting across the Archean basement complex provide suitable markers for paleomagnetic reconstructions of the craton. The Archean and early Paleoproterozoic rock assemblages and mineralisation patterns in the craton show a broad similarity with the Western Australian Craton, indicating near-neighbourhood positions of the two ancient cratonic blocks. Paleomagnetic studies have shown the separation of these two blocks at ~2000 Ma, with the development of a paleo-ocean which closed subsequently during the amalgamation of the Bastar Craton with the East Antarctic Shield to form the Eastern Ghats Mobile Belt in three phases at ~1700–1600 Ma, ~1050–950 Ma and ~500 Ma, with extensional phase between 1450 and 1100 Ma. The Bastar Craton preserves important clues regarding the evolution of the ocean and atmospheric conditions in the early Earth.

巴斯塔克拉通在印度半岛占有重要地位，位于印度三个克拉通核之间，西南为达尔瓦尔克拉通，东北为辛格布姆克拉通，西北为邦德尔坎德克拉通。克拉通东南缘和北缘分别与构成东高止山脉移动带和中印度构造带（萨特普拉移动带）的元古代造山带接壤。对克拉通构造地层演化的分析表明，克拉通形成于古太古代（~3582 Ma）。克拉通太古代演化的标志是包含化学成因沉积物（带状铁层）和金矿化的花岗岩-绿岩带的发展。高品位片麻岩和麻粒岩在地体的三个造山期（~2700 Ma Bailadila造山运动、~2900 Ma Bengpal造山运动和~3400 Ma Sukma造山运动）期间发育。克拉通的古元古代演化是从大氧化事件（GOE；2500 –2300 Ma) 和古元古代冰期 (2400–2300 Ma) 以及 GOE 之后 (2050–1850 Ma)。相邻移动带中造山活动的影响以影响克拉通边缘岩石的变质和岩浆活动为特征。克拉通北缘的萨特普拉造山事件导致巴斯塔克拉通与邦德尔坎德克拉通在~2250 和~2100 Ma 合并，形成了印度半岛的主要部分。造山带崩塌（延伸）发育成横切造山趋势的盆地，其中沉积了碎屑、火山碎屑和化学成因沉积物（Khairagarh 和 Chilpi 群）。克拉通东南缘在约 1700 Ma 的东高止山脉造山运动期间有混合作用和花岗岩侵位的记录。在东高止山脉造山崩塌期间，沿平行于东高止山脉流动带的一条线排列了许多沉积盆地。后来沿东高止山脉的造山活动造成了克拉通这些沉积盆地内沉积间断/不整合面的发展。跨越太古代基底复合体的不同世代（2400 Ma、2100 Ma 和 1890 Ma）的基性岩脉为克拉通的古地磁重建提供了合适的标记。克拉通中太古代和早古元古代的岩石组合和矿化模式与西澳大利亚克拉通具有广泛的相似性，表明这两个古克拉通地块的邻近位置。古地磁研究表明，这两个区块在约 2000 Ma 时分开，随着古海洋的发展，随后在巴斯塔克拉通与南极东部地盾合并形成东高止山脉移动带的过程中分三个阶段关闭。 1700-1600 Ma，~1050-950 Ma 和~500 Ma，伸展相在 1450-1100 Ma 之间。