Divergent genetic models have been proposed for clastic dominant (CD-type) massive sulfide Zn-Pb mineralization in the Proterozoic Carpentaria Zn Province. Due to varying degrees of tectonic overprint, it has been difficult to accurately constrain structural and paragenetic timing aspects of the CD-type genetic model, and the most basic timing constraints (syngenetic vs. epigenetic, synextension vs. syninversion) remain debated. The recently discovered Teena Zn-Pb deposit is hosted by an exceptionally well preserved subbasin that permits relative timing relationships to be well defined. Using a combination of geophysical, structural, sedimentological, and petrographic datasets, a new model for subbasin development and syndiagenetic hydrothermal replacement mineralization is developed for the Teena mineral system.At Teena, sulfide mineralization was deposited from lateral fluid flow beneath an impermeable seal several hundred meters below the paleosurface and maximum flood surface, after formation of fine-grained diagenetic pyrite (py1) and dolomite nodules. Sulfide mineralization resulted from syndiagenetic carbonate replacement and pore space cementation where thermochemical sulfate reduction took place. The sulfide mineralization is therefore partly cospatial but not cogenetic with its thick pyritic hanging wall, and its lateral alteration footprint is much smaller than predicted by sedimentary exhalative (SEDEX) models. An additional zone of low-grade Zn-Pb mineralization in the footwall W-Fold Shale Member represents a different style of mineralization not previously reported for Carpentaria CD-type Zn deposits: it is associated with strata-bound lenses of hydrothermal dolomite (HTD) that formed by both replacement and carbonate dissolution and infill, which yielded diverse cavity-infill textures that include coarse-bladed dolomite fans cemented by interstitial sphalerite, dolomite, and quartz. Volumetrically minor Zn mineralization is also present in a fault conduit hydrothermal breccia and in hanging-wall synorogenic vein sets derived by hydrothermal leaching and remobilization of Zn from the underlying mineralized zones.Whereas both the Teena and nearby McArthur River Zn-Pb deposits are located along the northern margin of the 3^rd-order Hot Spring-Emu subbasin, they formed in separate 4^th-order subbasins in association with local extensional growth faults. Growth fault movement in the Teena subbasin was initiated during deposition of the W-Fold Shale Member and persisted episodically until a weak structural disconformity associated with sedimentary facies regression developed in the Upper HYC unit. Shifting patterns in depocenter location, sedimentary facies development, mineralization, and alteration zonation are attributed to progressive growth and linkage of segments of a regionally anomalous ENE-trending, synsedimentary fault zone. Similar patterns of extensional subbasin development were repeated in other Zn-mineralized subbasins throughout the River supersequence across the northern Carpentaria Zn Province, and formed in response to a short-lived episode of north-northwest–south-southeast regional extension around ca 1640 ± 5 Ma, triggered by far-field subduction events.

中文翻译：

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Teena Zn-Pb 矿床（澳大利亚麦克阿瑟盆地）。第一部分：与动态子盆地演化相关的同成岩贱金属硫化物成矿

已经为元古界 Carpentaria Zn 省的碎屑显性（CD 型）块状硫化物 Zn-Pb 矿化提出了不同的遗传模型。由于不同程度的构造叠印，很难准确地约束 CD 型遗传模型的结构和共生时间方面，并且最基本的时间限制（同基因与表观遗传、同延与同反）仍然存在争议。最近发现的Teena Zn-Pb 矿床位于一个保存完好的子盆地中，可以很好地定义相对时间关系。结合地球物理、构造、沉积学和岩石学数据集，为蒂纳矿物系统开发了一种新的子盆地开发和同成岩热液替代成矿模型。在形成细粒成岩黄铁矿 (py1) 和白云岩结核之后，硫化物矿化是在古地表和最大洪水面以下数百米的不透水封层下的侧向流体流沉积的。硫化物矿化是由同成岩碳酸盐置换和孔隙空间胶结引起的，其中发生了热化学硫酸盐还原。因此，硫化物矿化与其厚黄铁矿挂壁部分共生，但不是共生的，其横向蚀变足迹远小于沉积喷出物 (SEDEX) 模型预测的。下盘 W 褶皱页岩成员中的另一个低品位 Zn-Pb 矿化带代表了一种不同的矿化类型，以前没有报道过 Carpentaria CD 型锌矿床：它与由置换和碳酸盐溶解和填充形成的热液白云岩 (HTD) 地层束缚透镜体相关，产生了不同的腔体填充结构，包括由间隙闪锌矿、白云岩和石英胶结的粗叶片白云岩扇。体积较小的 Zn 矿化也存在于断层管道热液角砾岩和由下伏矿化带的热液浸出和再动员 Zn 衍生的上壁同生脉组中。 而蒂纳河和附近的麦克阿瑟河锌铅矿床位于3的北缘 和石英。体积较小的 Zn 矿化也存在于断层管道热液角砾岩和由下伏矿化带的热液浸出和 Zn 再迁移衍生的上壁同生脉组中。而蒂纳河和附近的麦克阿瑟河锌铅矿床位于3的北缘 和石英。体积较小的 Zn 矿化也存在于断层管道热液角砾岩和由下伏矿化带的热液浸出和再动员 Zn 衍生的上壁同生脉组中。 而蒂纳河和附近的麦克阿瑟河锌铅矿床位于3的北缘^rd阶温泉-鸸鹋子盆地，它们分别形成于^第4^次与局部伸展生长断层相关的阶次盆地。蒂纳亚盆地的生长断层运动是在 W 褶皱页岩段沉积期间开始的，并间歇性地持续，直到与上 HYC 单元中的沉积相回归相关的微弱结构不整合。沉积中心位置、沉积相发育、矿化和蚀变带的移动模式归因于区域异常 ENE 趋势、同沉积断层带段的逐渐增长和连接。类似的伸展子盆地发育模式在整个河流超序列中的其他锌矿化子盆地中重复出现，横跨 Carpentaria Zn 省北部，