China hosts a large proportion of global REE resources. This paper presents a preliminary review of the types and ore genesis of endogenic REE deposits in China. Three major types of REE deposits are identified, namely carbonatite-type, alkaline and alkali granite-type and hydrothermal-type deposits. The carbonatite-type deposits mainly include Bayan Obo in northern China, Maoniuping in southwestern China, Weishan in eastern China, and Miaoya in Central China, all of which are genetically related to carbonatite/carbonatite-alkaline complex. This type of deposit mainly contains economic light REE (LREE), which are mainly hosted in fluoro-carbonate and/or phosphate. Apart from LREE, some deposits may also show obvious enrichments in heavy REE (HREE), Nb, Th, and Sc. The above-mentioned carbonatite-type REE deposits were formed in different periods, including Meso-Proterozoic (Bayan Obo), Paleozoic (Miaoya), Mesozoic (Weishan) and Cenozoic (Maoniuping). They were generated in intra-continental extension (Bayan Obo, Miaoya, and Weishan) or post-collisional (Maoniuping) setting. The ore-related intrusions were mainly derived from very low degrees partial melting of the sub-continental lithosphere mantle (SCLM). Before the formation of carbonatite, the SCLM had been metasomatized by recycled crustal components, which elevated the contents of REE and other components (e.g., Nb, Ba, F, and P). The parental carbonatitic or CO2-rich silicate magmas have experienced intensive fractional crystallization or immiscibility of carbonate- and silicate-rich melts, which further improve the contents of REE in the later-stage magmas. A subset of REE minerals was crystallized in the magmatic evolution process, while a large proportion of REE were retained in the residual melts. Furthermore, the REE were transported out of the magma chamber by volatile-rich fluids (e.g., F−, SO42− and Cl−), and were deposited adjacent to the carbonatitic intrusions. The alkaline and alkali granite-type deposits mainly include Baerzhe and Saima in northeastern China, which have genetic associations with SiO2-saturated or -unsaturated alkaline intrusions, respectively. Compared with the carbonatite-type deposit, this type of deposits contains relatively high contents of HREE, which are mainly hosted in phosphate or silicate. Notably, this type of deposits may also contain economic Zr, Nb, and Ta. The above-mentioned deposits were formed in the Mesozoic under an intra-continental extensional setting. Similar to the carbonatite, the ore-related alkaline intrusions were derived from the sub-continental lithosphere mantle (SCLM), which had been metasomatized by REE- and volatile-bearing components. The parental silicate magmas have experienced intensive fractional crystallization during the evolution process. Many REE-, Nb-, and Zr-bearing minerals were crystallized in the later magmatic process. These minerals were later modified by magmatic-hydrothermal fluids, which lead to remobilization and further enrichment of REE, Zr and Nb. A few IOCG deposits also show obvious enrichment in LREE, which are represented by the Paleoproterozoic Yinachang and Lala deposits in southwestern China. Diverse minerals occur as REE hosts in this type of deposits, mainly including fluoro-carbonate, phosphate, and silicate. No spatially associated magmatic intrusions can be identified in the IOCG-type deposits, but available data indicate that REE enrichment was genetically related to some hidden magmatic intrusions. The intrusions were generated in a rift-setting and vary from mafic to felsic in composition. In this type of deposit, REEs were initially deposited in apatite and allanite. In the later stages, apatite and allanite were modified by multiples phases of fluids. During the fluid/mineral interaction processes, REEs were mobilized and reprecipitated in other REE minerals, including monazite, bastnaesite, xenotime, synchysite. Multiple stages of fluid/mineral interaction are important for the final enrichment of REE in this type of deposit. In the future, more studies are needed to accurately evaluate the resources of REE in China, to target more deposits that are relatively enriched in medium-heavy REE, and to provide guidance for the effective utilization of accompanied metals in the REE deposits.