The Caviahue-Copahue Volcanic Complex (CCVC, 37° 51’ S-71° 05′ W) is located in the central segment of the South Volcanic Zone, ~30 km eastward from the main Andean volcanic arc. Within a complex tectonic setting, it has developed under the influence of the northern transtensional Liquiñe-Ofqui Fault Zone, to the south and the Copahue-Antiñir Fault Zone to the northeast. The onset of volcanic activity within Caviahue volcano-tectonic depression has been dated at Ar/Ar 125 ± 9 ka and it is represented by lava flows and ignimbrites of Las Mellizas Formation. Copahue volcano has a very well documented historical eruptive record, encompassing 13 eruptive cycles in the last 260 years. On the contrary, volcano stratigraphy during Late Pleistocene and pre-historic times is poorly constrained, mainly due to the lack of reliable radiometric data. Based on the peculiar morphology and cooling-fracture systems, lavas that crop out along Dulce, Jara and NE Agrio river valleys have been included in a new stratigraphic unit, here named as Río Dulce Formation. A subglacial emplacement is proposed taking into account the evidence of ice-confinement, provided by the flat-topped and steep-sided lava domes/flows and dammed lava flows. In addition, melt water-magma interaction is supported by conspicuous fine columnar-jointing and closely spaced curved bands with plumose structures, well-developed pseudopillow fracture systems, platy and hackly fractures and cube-jointed entablature-bearing lava flows. The basaltic andesites (SiO₂₌ 55–57%) are porphyritic, with ~30–40% of sieved plagioclase, two pyroxenes and olivine, set in a glassy groundmass. Lava vent distribution and primary anisotropy planes orientation, in coincidence with WNW-ESE and NE-SW trending faults, lineaments and fault scarps, document a first-order structural control on the volcanic emplacement. Although undated, this study can contribute to understanding the timing of glacial fluctuations during Late Pleistocene. Furthermore, it has implications on hazard assessment since it highlights that the evolution of the CCVC has experienced alternating fissure and central eruptive style, likely related to the dynamics of the magma-plumbing system, as suggested by geophysical evidence of unrest.

Caviahue-Copahue火山群（CCVC，37°51'S-71°05'W）位于南火山区的中段，距安第斯主火山弧向东约30公里。在复杂的构造环境中，它在北部伸展的利基涅-奥奇奎断裂带和南部的科帕韦-安蒂尼尔断裂带的影响下发展起来。Caviahue火山-构造depression陷内的火山活动开始于Ar / Ar 125±9 ka，并以熔岩流和Las Mellizas组的火成岩为代表。科帕韦火山具有非常详细的历史喷发记录，在过去260年中涵盖了13个喷发周期。相反，晚更新世和史前时期的火山地层受到的限制很有限，这主要是由于缺乏可靠的辐射数据。基于独特的形态学和冷却破裂系统，沿着杜尔塞河，贾拉河和东北部阿格里奥河谷产生的熔岩被包括在一个新的地层单元中，这里被称为里奥·杜尔塞组。考虑到冰封的证据，提出了一个冰下封存，这是由平顶的和陡峭的熔岩穹顶/水流和受阻的熔岩流所提供的。此外，熔融水-岩浆相互作用得到明显的细柱状节理和紧密间隔的弯曲带的支持，这些弯曲带具有羽状结构，发达的假枕形裂缝系统，板状和凹状裂缝以及立方连接的含铅熔岩流。玄武安山岩（SiO 在这里被称为里奥·杜尔塞队。考虑到冰封的证据，提出了一个冰下封存，这是由平顶的和陡峭的熔岩穹顶/水流和受阻的熔岩流所提供的。此外，熔融水-岩浆相互作用得到明显的细柱状节理和紧密间隔的弯曲带的支持，这些弯曲带具有羽状结构，发达的假枕形裂缝系统，板状和凹状裂缝以及立方连接的含铅熔岩流。玄武安山岩（SiO 在这里被称为里奥·杜尔塞队。考虑到冰封的证据，提出了一个冰下封存，这是由平顶的和陡峭的熔岩穹顶/水流和受阻的熔岩流所提供的。此外，熔融水-岩浆相互作用得到明显的细柱状节理和紧密间隔的弯曲带的支持，这些弯曲带具有羽状结构，发达的假枕形裂缝系统，板状和凹状裂缝以及立方连接的含铅熔岩流。玄武安山岩（SiO 发育良好的伪枕形裂缝系统，板状和凹状裂缝以及立方连接的含钝孔的熔岩流。玄武安山岩（SiO 发育良好的伪枕形裂缝系统，板状和凹状裂缝以及立方连接的含钝孔的熔岩流。玄武安山岩（SiO_{2 =} 55–57％）是斑状的，约有30–40％的筛过斜长石，两种辉石和橄榄石，位于玻璃状地基中。与WNW-ESE和NE-SW趋势断层，线状体和断层陡坡相吻合的熔岩喷口分布和主要各向异性平面取向，证明了对火山作用的一阶结构控制。尽管未注明日期，但这项研究可有助于了解晚更新世期间冰川波动的时间。此外，它还对危险性评估产生了影响，因为它突显出CCVC的演化经历了交替的裂隙和中央喷发型式，这可能与岩浆管道系统的动力学有关，这是动乱的地球物理证据表明的。