The Scandinavian mountain chain: deep processes (TopoScandiaDeep)

山脉大多形成于会聚或走滑边缘，预计不会在板内环境中形成。然而，在始新世早期大陆分裂后，东北大西洋周围的许多地方都出现了隆起。在欧洲北部（挪威北部和南部、苏格兰）、斯匹茨卑尔根岛、格陵兰岛的大陆边缘已经发现了几个圆顶状结构（Japsen和Chalmers, 1999； Japsen等人，2006）。大陆-海洋过渡时期隆起的识别导致了许多早期动力学模型，这些模型将隆起直接与大约60 Ma的北大西洋裂谷事件联系起来（Chery et al., 1992; Clift et al., 1998）。然而，越来越多的证据表明，大部分观测到的隆升是在裂谷期之后发生的，裂谷期大约为10亿年，并且可能分几个阶段发生（Japsen and Chalmers, 1999; Japsen et al., 2006; Rohrmann and van der Beek, 1996）。此外，隆起沿边缘并不均匀（Japsen and Chalmers, 1999; Lundin and Dore, 2002），而是集中在离散的圆顶状结构中，这一事实表明，裂谷和隆起之间并不存在简单的一对一对应关系。所有提出的模型（例如，气候强迫、地幔柱物质在岩石圈下的就位（可能与冰岛热点有关）、岩浆底板、板内压缩或与隆起变薄的裂谷本身的弯曲耦合）都没有得到现有数据的有力支持。为了理解新近纪隆升的机制，我们需要知道地形荷载是如何被支撑的，即均衡、动态或弯曲。如果支撑采用等静力补偿，那么相应的浮力在哪里？（在地壳、岩石圈或亚岩石圈地幔？）在这个方案中，我们将集中分析位于斯堪的纳维亚半岛北部和南部斯堪的纳维亚山脉（Scandes）的两个圆顶。

Mountains form mostly at convergent or strike-slip margins and are not expected to form in intraplate settings. Uplift occurred, however, in various places around the northeast Atlantic after continental break-up took place in the earliest Eocene. Several dome-like structures have been identified along the continental margins in northern Europe (northern and southern Norway, Scotland), Spitzbergen, Greenland (Japsen and Chalmers, 1999; Japsen et al., 2006). Identification of uplift at the continent-ocean transition led to a number of early dynamic models relating the uplift directly to the North Atlantic rifting event at around 60 Ma (Chery et al., 1992; Clift et al., 1998). However, there is a growing body of evidence indicating that much of the observed uplift post-dates rifting by several 10’s of Ma and probably occurred in several stages (Japsen and Chalmers, 1999; Japsen et al., 2006; Rohrmann and van der Beek, 1996). Moreover, the fact that uplift is not uniform along the margins (Japsen and Chalmers, 1999; Lundin and Dore, 2002) but instead is concentrated into discrete dome-like structures suggests that there is no simple 1-to-1 correspondence between rifting and uplift. None of the suggested models (e.g. climatic forcing, emplacement of mantle plume material underneath the lithosphere, possibly in relation to the Icelandic hotspot, magmatic underplating, intraplate compression or flexural coupling to the uplifted, thinned rift itself) has firm support from existing data. In order to understand the mechanisms of Neogene uplift, we need to know how the topographic load is supported, i.e., isostatically, dynamically, or flexurally. If the support is by isostatic compensation, where is the corresponding buoyancy located? (In the crust, lithosphere, or sub-lithospheric mantle?). In this proposal, we will concentrate on analysing the two domes located in Scandinavia, the Northern and Southern Scandinavian mountain ranges (Scandes).