岐阜県西部の美濃帯ジュラ紀メランジュ中に産する舟伏山岩体の東部でペルム系石灰岩（舟伏山層）の岩相層序と年代を検討した。舟伏山層は下部より，高有機質，暗灰～黒色の層状石灰岩で特徴づけられる下部層（層厚約400 m：シスウラリアン上部～グアダルピアン下部）, 紡錘虫，ウミユリ，Tubiphytesに富む灰白色，塊状の石灰岩が優勢な中部層（層厚約250 m：グアダルピアン下部～中部），紡錘虫とウミユリに富む灰色，塊状の石灰岩が主体をなす上部層（層厚50～70 m：上部グアダルピアン）からなる。下部層中部にはアラトコンカ科大型二枚貝，下部層上部にはサンゴが産出する。<n>本層下部層の大半はミクライト質基質をもったwackestoneとpackstoneからなり，最上部にスパライトセメントをもつgrainstoneを伴う。中部層はwackestoneとpackstoneが優勢であるが，grainstoneが数層準で挟まれる。また中部層には石灰質シアノバクテリアによる小規模なboundstoneがみられる。上部層はペロイド質のミクライト基質をもつwackestoneおよびlime-mudstoneが卓越するほか，少量のgrainstoneとpackstoneがみられる。下部層最上部と中部層下部は互いに指交関係にあり，岩相および生相が漸移的に変化する。<n>

This paper describes the lithostratigraphy and age of the Permian limestones in the eastern part of the Funabuseyama rock mass in the Mino Belt. The Permian limestone, defined as the Funabuseyama Formation, mainly comprises bioclastic limestones that are rich in diverse shallow-marine organic debris and minor microbial boundstone. The three members of the Funabuseyama Formation are 1) a lower member (approximately 400-m thickness) consisting of bedded, highly carbonaceous, dark gray to black limestones with frequent intercalation of alatochoncid bivalves and minor light gray limestone in the upper part of the member, 2) a middle member (approximately 250-m thickness), dominated by massive, light gray pack/wackestone rich in fusulinoideans, crinoids, and calci-microbes with intermittent peloidal grainstones and 3) an upper member (approximately 70-m thickness), with primarily of massive to thick-bedded, gray to dark gray pack/wackestones that are rich in fusulinoideans and crinoids. The lower member grades into the middle member with an interfingering relationship. Based on the fusulinoidean biostratigraphy the lower to middle part of the lower member, its upper part, middle and upper members are correlated with the Kungurian, upper Kungurian to lower Roadian, upper Roadian to Wordian and Capitanian, respectively.<n>The lack of coarse land-derived grains in the Funabuseyama Formation implies its deposition in an open-ocean setting. The prevalence of dasycladacean algae in the succession further indicates its deposition in a photic, shallow subtidal zone, probably associated with a Panthalassic seamount. The highly carbonaceous property of the lower member suggests its deposition in a quiet and stagnant depression within a lagoonal basin of the buildup. Conversely, the middle member was deposited on a well-circulated sand shoal to sand bar on the buildup, whereas the upper member formed in a quiet, however, less stagnant environment in a lagoonal flat.