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大陆岩石圈伸展最终形成沉积盆地，而它的岩浆活动响应却有很大不同。以岩石围和软流圈无水部分熔融为基础的数值模型表明，于伸展区之下上涌的上地慢的温度对喷发岩浆的化学性质和体积起到了根本控制作用。强大山性断陷活动一般只在软流图势温度比正常情况高100～300℃时才有可能发生，并伴随地设柱活动。这些模型还可以预测大陆岩石围伸展量β与所生成的岩浆体积之间的紧密关系。更为复杂的模型还考虑了富挥发分慢源的部分熔融作用，其固相带温度比正常的要低，可能位于地慢柱中或大陆岩石围地慢的富含岩浆区域。但由于我们对于潜在含挥发分的源区组分的部分熔融作用知之甚少，这种岩浆生成过程的复杂数值模拟还有局限性。对盆地中发育的火成岩进行地球化学和同位素（Sr－Nd-Pb）分析，有助于评价大陆岩石围和软流圈源区组分对岩浆的成岩作用和部分熔融的深度和程度的相对贡献大小。这些数据也可以为估计地壳混染量提供重要的约束条件，尤其是下地壳部分熔融产生的混梁作用。在许多盆地内设源岩浆可能从不真正到达地表，而是底侵入下地壳。若能正确地估计出地壳减薄量，就可以识别出这种底侵岩体。单个盆地内的岩浆喷发位置常受控于已存在的基底结构，盆地内的构造-岩浆活动史对岩浆活动的位置起到了?
The formation of the continental lithosphere eventually formed sedimentary basins, and its magmatic response was quite different. The numerical model based on the partial melting of the rocks and asthenosphere shows that the temperature of the upper and lower updip beneath the extensional zone plays a fundamental role in controlling the chemistry and volume of the erupted magma. Strong mountain faulting activities generally only occur when the temperature of the hydrofoil is 100-300 ° C higher than normal, and the activities of columns are set along with it. These models also predict the close relationship between continental extensibility β and the volume of magma produced. The more complex models also consider the partial melting of the slow-source rich-volatile matter, which has a lower solidus temperature than normal, and may be located in slowly slow magma-rich areas in the slow Earth Columns. However, due to our limited knowledge of the partial melting of the source-component components that are potentially volatile, there are limits to the complex numerical simulation of this magma generation. Geochemical and isotopic (Sr-Nd-Pb) analysis of igneous rocks developed in the basin is helpful to evaluate the relative contributions of the continental lithospheric and asthenospheric source components to the diagenesis and depth and extent of partial melting size. These data may also provide important constraints for estimating the amount of crustal mixing, especially for the role of a mixing beam produced by the partial melting of the lower crust. In many basins, the source magma may never actually reach the surface but instead intrude into the lower crust. If we can correctly estimate the amount of crustal reduction, we can identify such intrusion rock body. The location of magma eruption in a single basin is often controlled by the existing basement structure. The history of tectono-magmatic activity in the basin has played a role in the location of magmatic activity.