区域地质构造12碰撞造山带2

Chapter 17: Continental Arc Magmatism
Figure 17-5. MORB-normalized spider diagram (Pearce, 1983) for selected Andean volcanics. NVZ (6 samples, average SiO2 = 60.7, K2O = 0.66, data from Thorpe et al. 1984; Geist, pers. comm.). CVZ (10 samples, ave. SiO2 = 54.8, K2O = 2.77, data from Deruelle, 1982; Davidson, pers. comm.; Thorpe et al., 1984). SVZ (49 samples, average SiO2 = 52.1, K2O = 1.07, data from Hickey et al. 1986; Deruelle, 1982; López-Escobar et al. 1981). Winter (2001) An Introduction to Igneous and Metamorphic Petrology. Prentice Hall.
层成
纳 木 那 尼 穹 隆
贝提克穹隆带
贝提克穹隆带的构造
蒙特罗萨的位置
蒙特罗萨穹状褶皱
前陆磨拉石盆地相
Fig2. Schematic cross-section of a foreland system shown at approximately true scale, modified after DeCelles and
造山带的前缘弧
克希斯坦剖面
蛛网图
残留弧相
西 太 平 洋 的 残 留 弧
残留弧定义
• Remnant arcs are the submarine ridges which lie behind active island-arc systems. In simple cases, these ridges are bounded by scarp systems on both flanks, have volcaniclastic aprons on the rear flank, and are similar in composition to frontal arcs.－Karig，1972
赫尔威特的盖层推覆体
莫克尔推覆体
前陆褶皱冲断带构造样式
前陆褶皱冲断带构造样式
阿巴拉契亚谷岭带
阿巴拉契亚谷岭带源自文库
J. Bret Bennington and Charles Merguerian Thomson Custom Pub (September 01, 2006)
前陆褶皱带
侏罗山构造剖面
新赫布里底 帕劳－本州 西菲律宾脊
残 留 弧 的 地 震 波 速
COMPLEX REMNANT ARCS
残 留 弧 成 因 模 式
阿巴拉契亚的残留弧
墨 西 演哥 化残 留 弧
班戈－江错
纳木错弧后蛇绿岩
增生弧相
阿根廷古生代增生弧
阿 根 廷 增 生 弧 岩 浆 模 式
南美元古－古生代增生弧
DIFFERENTIATION TRENDS FOR IAV
Early Fe-Ti Ox FX in Calc-Alk
CaPl NaPl
Pl+Cpx FX
Figure 16-6. From Winter (2001) An Introduction to Igneous and Metamorphic Petrology. Prentice Hall.
Chapter 17: Continental Arc
Magmatism
Figure 17.2. Schematic diagram to illustrate how a shallow dip of the subducting slab can pinch out the asthenosphere from the overlying mantle wedge. Winter (2001) An Introduction to Igneous and Metamorphic Petrology. Prentice Hall.
Nb(Ta) Anomalies
HFS Elements
Figure 16-11a. MORB-normalized spider diagrams for selected island arc basalts. Using the normalization and ordering scheme of Pearce (1983) with LIL on the left and HFS on the right and compatibility increasing outward from Ba-Th. Data from BVTP. Composite OIB from Fig 14-3 in yellow.
造山带2
大地构造相
弧构造相类
前缘弧相
Structure of an Island Arc
Figure 16-2. Schematic cross section through a typical island arc after Gill (1981), Orogenic Andesites and Plate Tectonics. Springer-Verlag. HFU= heat flow unit (4.2 x 10-6 joules/cm2/sec)
Earth 238-27
Fold-thrust belt
Earth 238-27
Fold-thrust belt
Vercors balanced and restored cross-section (french Alps)
http://earth.leeds.ac.uk/tectonics/alpine_tectonics/index.htm
Appalachian Mountains of the US---overhead view
活化盖层相
活化盖层相
芒布朗的位置
芒布朗地质图
A.地质构造图 彭宁 飞来峰；赫尔威特中 生代沉积；红针地块 花岗岩和变质岩；芒 布朗剪切带；芒布朗 地块花岗岩和变质岩； 赫尔威特底滑脱带； 赫尔威特底冲断层； 彭宁底冲断层。
岩石化学特征
TRACE ELEMENT CHARACTERISTICS HYDROUS MORB SOURCE,
SELECTIVELY ENRICHED MORB SOURCE, OR OIB SOURCE W/
HFS-COMPATIBLE RESIDUAL MINERAL?
Hydrophilic LIL Elements
简单残留弧的成因
• The Palau-Kyushu, Lau-Colville, and West Mariana ridges have been identified as the rear edges of frontal arcs, left behind as rifting in the inter-arc basin separates the remnant feature from the active arc (Karig, 1970, 1971a).
B.综合剖面
芒布朗构造剖面
剖面位置见上图
外阿尔卑斯构造演化
前陆褶皱冲断带相
扎格罗斯造山带
扎格罗斯前陆褶皱冲断带
扎格罗斯前陆褶皱冲断带
Earth 238-27
Fold-thrust belt
Seaward edge of passive-margin sedimentary basins
VOLCANIC ROCKS OF ISLAND ARCS
• Complex tectonic situation and broad spectrum of volcanic products • High proportion of basaltic andesite and andesite • Basalts common and an important part of the story
增 生 弧 演 化 模 式
东 准 增 生 弧
东 准 花 岗 岩 地 球 化 学
西 南 天 山 增 生 弧
西昆仑增生弧
前陆褶皱带相
前陆褶皱带相
Fig. 5. Sections from the paleodoline of La Corde and their schematic correlation. Note the siderolithic sediments at the base, the lensshaped “Cerithium Beds” inside the Diablerets Member as well as the coral (section 6) and oyster reefs (section 7).
SIMPLE REMNANT ARCS
• Simple remnant arcs consist of linear, commonly arcuate basement ridges bounded on both flanks by scarp systems. A sediment apron occurs on the rear flank and commonly buries that scarp system, but there is a characteristic lack of coeval sediment deposition on the forward flank (Fig. 2). Both scarp systems represent the rifted edges of extensional marginal basins.
主线性剪切带相
辛 普 隆 剪 切 带
辛普隆剪切带的鞘褶皱
喀斯考湾剪切带
斜向冲断与短轴背斜
剪切穹隆带相
主剪切穹隆带相
康马地区区域地质简图
K2zn-宗桌组；(J3-K1)j-加 丕拉组；J3w-维美组；J12tm-田巴群；T3ny-涅如群； T1-2ln-吕村群；P1k-b-康 马组、白定浦组；C2p-b. 破林浦组、比聋组；C1sp少岗组。1-构造片岩带；2花岗岩及花岗片麻岩；3-断
Giles (1996). Wedge top basin fill consists of coarse-grained fluvial deposits when it develops in subaerial settings, while mass flows and fine-grained shelf sediments can characterise this zone in a subaqueous setting conditions. The wedge top depozone becomes part of the mountain belt while it deforms and it is usefull for studying the kinematic history of the wedge, unconformities occur as a frequent feature. Foredeep depozone is the well developed part of the system. It is generally characterized by a transition from deep-marine (flysch phase) to shallow-marine or continental sedimentation (molasse phase). A rejuvenation of the load or changes in effective elastic thickness can produce a complex sedimentary infill geometry. Unconformities are rare in the innermost part of the basin and more frequent close to the outermost edge. The forebulge is a zone of scarce deposition or erosion in case of subaerial conditions. It is generally characterised by several unconformities which help to reconstruct the bulge migration through time. In the retro-foreland system this depozone can be missing. Back-bulge sediments derive from the mountain belt, though contributions from the craton and development of carbonate platforms can occur in subaerial conditions. Unlike the foredeep depozone, isopac maps show a closure around a central thick zone.
Chapter 17: Continental Arc Magmatism
Figure 17.4. Chondrite-normalized REE diagram for selected Andean volcanics. NVZ (6 samples, average SiO2 = 60.7, K2O = 0.66, data from Thorpe et al. 1984; Geist, pers. comm.). CVZ (10 samples, ave. SiO2 = 54.8, K2O = 2.77, data from Deruelle, 1982; Davidson, pers. comm.; Thorpe et al., 1984). SVZ (49 samples, average SiO2 = 52.1, K2O = 1.07, data from Hickey et al. 1986; Deruelle, 1982; LópezEscobar et al. 1981). Winter (2001) An Introduction to Igneous and Metamorphic Petrology. Prentice Hall.