CAJ | 학술논문

我国钼资源十分丰富，目前已发现钼矿床四百余个，它们具有成带分布的特点。本文在钼矿床地质特征基础上，系统总结了钼矿床和含钼矿床的成矿年代（依据辉钼矿Re-Os 年龄），结果显示我国钼矿床空间上可分为东秦岭-大别、兴-蒙、长江中下游、华南、青藏和天山-北山六大钼成矿带；成矿时代上，钼成矿作用分为古元古代（1882～1804Ma）、早古生代（480～420Ma）、晚古生代（412～260Ma）、中生代印支期（251～209Ma）、中生代燕山期（194～77Ma）和新生代（65～13Ma）等六个阶段，主要集中于中生代和新生代。元古宙形成的钼矿床分布于东秦岭-大别钼成矿带，古生代钼矿床主要分布于天山-北山钼成矿带，中生代钼矿床在中国东部广泛分布，新生代钼矿床全都分布于青藏钼成矿带。我国古元古代钼矿床（1882～1804Ma）形成于古陆块之间俯冲碰撞背景下的岛弧环境（东秦岭-大别）；早古生代钼矿床（480～420Ma）形成于不同构造单元由挤压向伸展转换的岛弧或陆缘弧环境（东秦岭-大别、兴-蒙和华南）；晚古生代钼矿床（412～260Ma）形成于古亚洲洋壳俯冲的岛弧环境（兴-蒙）；中生代印支期钼矿床（251～209Ma）形成于板块碰撞及后碰撞背景（东秦岭-大别、兴-蒙和天山-北山）或洋壳俯冲的背景（青藏）；燕山期钼矿床形成于古太平洋板块俯冲转向及其后伸展体制下岩石圈减薄拆沉环境（东秦岭-大别、兴-蒙、长江中下游和华南），燕山晚期钼矿床（85～77Ma）形成于碰撞后的伸展背景（青藏）；新生代（65～13Ma）钼矿床形成于印度板块与欧亚板块陆陆碰撞及其后的伸展背景（青藏）。我国钼成矿作用受到了环太平洋构造带（东秦岭-大别、兴-蒙、长江中下游和华南）、中亚造山带（天山-北山、兴-蒙）和特提斯构造带（青藏）三大构造体制的影响。我國鉬資源十分豐富，目前已髮現鉬礦床四百餘箇，它們具有成帶分佈的特點。本文在鉬礦床地質特徵基礎上，繫統總結瞭鉬礦床和含鉬礦床的成礦年代（依據輝鉬礦Re-Os 年齡），結果顯示我國鉬礦床空間上可分為東秦嶺-大彆、興-矇、長江中下遊、華南、青藏和天山-北山六大鉬成礦帶；成礦時代上，鉬成礦作用分為古元古代（1882～1804Ma）、早古生代（480～420Ma）、晚古生代（412～260Ma）、中生代印支期（251～209Ma）、中生代燕山期（194～77Ma）和新生代（65～13Ma）等六箇階段，主要集中于中生代和新生代。元古宙形成的鉬礦床分佈于東秦嶺-大彆鉬成礦帶，古生代鉬礦床主要分佈于天山-北山鉬成礦帶，中生代鉬礦床在中國東部廣汎分佈，新生代鉬礦床全都分佈于青藏鉬成礦帶。我國古元古代鉬礦床（1882～1804Ma）形成于古陸塊之間俯遲踫撞揹景下的島弧環境（東秦嶺-大彆）；早古生代鉬礦床（480～420Ma）形成于不同構造單元由擠壓嚮伸展轉換的島弧或陸緣弧環境（東秦嶺-大彆、興-矇和華南）；晚古生代鉬礦床（412～260Ma）形成于古亞洲洋殼俯遲的島弧環境（興-矇）；中生代印支期鉬礦床（251～209Ma）形成于闆塊踫撞及後踫撞揹景（東秦嶺-大彆、興-矇和天山-北山）或洋殼俯遲的揹景（青藏）；燕山期鉬礦床形成于古太平洋闆塊俯遲轉嚮及其後伸展體製下巖石圈減薄拆沉環境（東秦嶺-大彆、興-矇、長江中下遊和華南），燕山晚期鉬礦床（85～77Ma）形成于踫撞後的伸展揹景（青藏）；新生代（65～13Ma）鉬礦床形成于印度闆塊與歐亞闆塊陸陸踫撞及其後的伸展揹景（青藏）。我國鉬成礦作用受到瞭環太平洋構造帶（東秦嶺-大彆、興-矇、長江中下遊和華南）、中亞造山帶（天山-北山、興-矇）和特提斯構造帶（青藏）三大構造體製的影響。
아국목자원십분봉부，목전이발현목광상사백여개，타문구유성대분포적특점。본문재목광상지질특정기출상，계통총결료목광상화함목광상적성광년대（의거휘목광Re-Os 년령），결과현시아국목광상공간상가분위동진령-대별、흥-몽、장강중하유、화남、청장화천산-북산륙대목성광대；성광시대상，목성광작용분위고원고대（1882～1804Ma）、조고생대（480～420Ma）、만고생대（412～260Ma）、중생대인지기（251～209Ma）、중생대연산기（194～77Ma）화신생대（65～13Ma）등륙개계단，주요집중우중생대화신생대。원고주형성적목광상분포우동진령-대별목성광대，고생대목광상주요분포우천산-북산목성광대，중생대목광상재중국동부엄범분포，신생대목광상전도분포우청장목성광대。아국고원고대목광상（1882～1804Ma）형성우고륙괴지간부충팽당배경하적도호배경（동진령-대별）；조고생대목광상（480～420Ma）형성우불동구조단원유제압향신전전환적도호혹륙연호배경（동진령-대별、흥-몽화화남）；만고생대목광상（412～260Ma）형성우고아주양각부충적도호배경（흥-몽）；중생대인지기목광상（251～209Ma）형성우판괴팽당급후팽당배경（동진령-대별、흥-몽화천산-북산）혹양각부충적배경（청장）；연산기목광상형성우고태평양판괴부충전향급기후신전체제하암석권감박탁침배경（동진령-대별、흥-몽、장강중하유화화남），연산만기목광상（85～77Ma）형성우팽당후적신전배경（청장）；신생대（65～13Ma）목광상형성우인도판괴여구아판괴륙륙팽당급기후적신전배경（청장）。아국목성광작용수도료배태평양구조대（동진령-대별、흥-몽、장강중하유화화남）、중아조산대（천산-북산、흥-몽）화특제사구조대（청장）삼대구조체제적영향。
There are abundant of molybdenum resource in China.More than 400 molybdenum deposits have been explored,which are distributed within several metallogenic belts. After systematically summary of geological and geochronogical data (molybdenite Re-Os age )of the total molybdenum deposits in China from previous research,we divided the Mo deposits into six metallogenic belts,including East Qinling-Dabie district,Xing-Meng district,Middle-Lower of the Yangtze River district,South China district, Tibet Plateau district and Tianshan-Beishan district.Geochronolgical characteritics show that all the molybdenum deposits in China formed in Paleoproterozoic (1882~1804Ma),Eopaleozoic (480~420Ma), Neopaleozoic(412~251Ma),Mesozoic Indosinian (251~209Ma),Mesozoic Yanshanian (194~77Ma)and Cenozoic (65~13Ma),most of which were formed in Mesozoic and Cainozoic.The molybdenum deposits formed in Paleoproterozoic located in the East Qinling-Dabie district,the Paleozoic molybdenum deposits are mainly distributed in the Tianshan-Beishan district,the Mesozoic molybdenum deposits are widely distributed in eastern China, the Cenozoic deposits are all located in the Tibet Plateau district. Paleoproterozoic (1882 ~ 1804Ma ) molybdenum deposits formed in the island arc environment of subduction collision between the ancient landmasses (East Qinling-Dabie district );Eopaleozoic (480~420Ma)molybdenum deposits formed in the island arc or continental margin arc environment of transition from compression to extension (East Qinling-Dabie district,Xing-Meng district,South China district);Neopaleozoic(412~251Ma)molybdenum deposits formed in Paleo-Asian Ocean subduction island arc environment(Xing-Meng district,Tianshan-Beishan district);Indosinian (251 ~209Ma)molybdenum deposits formed in the collision and post-collision background (East Qinling-Dabie district,Xing-Meng district,Tianshan-Beishan district);Yanshanian (194~77Ma)molybdenum deposits formed in the Pacific plate subduction and lithospheric thinning delamination environment (East Qinling-Dabie district,Xing-Meng district,Middle-Lower of the Yangtze River district,South China district),and Late Yanshanian (85~77Ma)molybdenum deposits formed in the extension background of post-collosion (Tibet Plateau district);Cainozoic molybdenum deposits formed in the Indian and Eurasian plates continental collision and subsequent extending background (Tibet Plateau district ). Molybdenum mineralization in China are controlled by the three major tectonic regime:Pacific Rim Tectonic Belt (East Qinling-Dabie district, Xing-Meng district,Middle-Lower of the Yangtze River district,South China district),Central Asian Orogenic Belt (Tianshan-Beishan district,Xing-Meng district)and Tethyan Tectonic Belt (Tibet Plateau district).