The Sydney-Bowen basin in eastern Australia is an elongate back arc-converted foreland basin system situated between the Lachlan Fold Belt in the west and the New England Fold Belt in the east. The Middle Permian Wandrawandian Siltstone at Warden Head near Ulladulla in the southern Sydney Basin is dominated by fossiliferous siltstone and mudstone, with a large amount of dropstones and minor pebbly sandstone beds. Two general types of deposits are recognized from the siltstone unit in view of the timing and mechanism of formation. One is represented by the primary deposits from offshore to subtidal environments with abundant dropstones of glacial marine origin. The second type is distinguished by secondary, soft-sediment deformational deposits and structures, and comprises three layers of mudstone dykes of seismic origin. In the latter type, metre scale, laterally extensive syn-depositional slump deformation structures occur in the middle part of the Wandrawandian Siltstone. The deformation structures vary in morphology and pattern, including large-scale complex-type folds, flexural stratification, concave-up structures, faulting of small displacements accompanied by folding and brecciation. The slumps and associated syn-sedimentary structures are attributed to penecontemporaneous deformations of soft sediments (mostly silty mud) formed as a result of mass movement of unconsolidated and/or semi-consolidated substrate following an earthquake event. The occurrence of the earthquake event deposits supports the current view that the Sydney Basin was located in a back-arc setting near the New England magmatic arc on an active continental margin during the Middle Permian.

Earthquake and its resultant tsunami, as a kind of disaster events in geological history, may be recorded as event deposits of seismite and tsunamite. Typical characteristics of seismite and tsunamite, including seismo-fracture bed, synsedimentary microfracture, micro-corrugated lamination, molar tooth structure, hummocky bedding etc, occurs in Mesoproterozoic Dalongkou Formation in central Yunnan Province. Three types of sedimentary units have been recognized: seismite (unit-A, including limestone with molar tooth structure, seismic shattering rock, seismic corrugated rock, autoclastic breccia and intraclastic parabreccia), tsunamite (unit-B, intraclastic limestone with hummocky bedding or parallel bedding) and background deposits (unit- C). Various stacking of these units constructs three distinct sedimentary sequences::A-B-C、A-C、B-C. The sequence A-B-C represents an event sedimentary sequence of earthquake-tsunami-background deposits. The sequence A-C represents the sequence of earthquake and background deposits (no tsunami occurring). The sequence B-C represents the sequence of tsunami and background deposits (far from the center of earthquake). As the central Yunnan province was located in a tectonic setting of rift basin in Mesoproterozoic era, the earthquake event deposits of Dalongkou Formation are sedimentary response to tectonic activity of the rift basin.

甘肃永靖盐锅峡下白垩统河口群盐锅峡组发现大量恐龙足迹化石。初步凋查发现了1O个化石点293个足印化石。其中在1号点600m2 的发掘面上，保存有7组蜥脚类138个足印、9组兽脚类6O个足印、1组鸟脚类3个脚印和1组翼龙类11个足印。7组蜥脚类足印形成4组保存完好的行迹和3组的足迹组合。最大的蜥脚类足印化石前脚790mm×1120mm。后脚1500mm×1420mm，是目前发现的世界上最大的恐龙足印之一．盐锅峡蜥脚类恐龙足迹可以分为3种类型：第1类足迹前脚为新月形，后脚为椭圆形，前后足印不重合并均向外偏转；第2类足迹前脚为半圆形，后脚为椭圆形，前后足印部分重合，后脚印向外偏转；第3类足迹前脚半圆形，后脚u形，前后足印明显分离并均向外偏转。蜥脚类恐龙足迹向外偏转反映恐龙成“外八字”型行走，这种行进方式可能与其巨大的体重有关。根据计算，盐锅峡蜥脚类恐龙臀高最小为3.04m，最大可达到5.3m。恐龙行走的速度2.3～3.4 km/h。古环境、古地理分析认为白垩纪甘肃兰州—青海民和一带为一内陆淡水湖盆。盐锅峡一带的恐龙足迹化石就发现于最近湖中心的“雾宿山古岛”西侧湖岸上。虽然白垩纪当地气候并不湿润，但湖岸地区草肥水美，是恐龙及其他陆生生物的乐园。

本文在牙形石生物地层对比的基础上，着重讨论吉维特-弗拉斯期的沉积相和沉积古地理。将该期地层红岭山组分为陆棚，开阔台地、局限台地、生物礁和丘、礁前斜坡及泻期六十相及十二十微相。提出西成地区泥盆纪存在—南北两侧均有镶边礁的小型碳酸盐台地，礁间泻期区是该区铅锌矿成矿的有利部位，也是今后寻找铅锌矿的重点靶区。

“三河口群”分布于南秦岭西段、陕甘川交界的勉县—略阳—康县—文县临江—南坪塔藏一带, 其南北均为断裂带限制。过去,“三河口群”的研究在史密斯地层学的理论指导下, 整体时代认为是下、中泥盆统。在非史密斯地层学理论的指导下, 对勉略带“三河口群”进行了解体, 建立了该带的原地和异地地层系统。新的地层系统包括了从太古界到石炭系不同时代的地层, 该地层系统揭示了南秦岭古海洋和大地构造演化过程: 南秦岭晚震旦世—早寒武世为扬子板块的一部分, 奥陶纪—志留纪时期沿南秦岭勉县—略阳—安康—随县(南) 形成裂陷槽盆地, 该盆地于中晚志留世有所萎缩但尚未完全关闭。泥盆纪时期该裂陷槽进一步开裂并形成有限洋盆, 石炭纪洋盆出现向南的俯冲。该洋盆可能在二叠纪仍然存在, 于印支期最终闭合。

北祁连加里东期造山带是在新元古代Rodinia联合大陆(Pangea-850)基础上裂解，经由寒武纪裂谷盆地、奥陶纪初期成熟洋盆、奥陶纪中晚期北祁连活动大陆边缘、志留纪—早、中泥盆世碰撞造山而形成的。奥陶纪中、晚期，北祁连、走廊地区中、上奥陶统发育洋壳-岛弧-弧后火山岩，形成典型的沟-弧-盆体系的沉积。志留纪—早、中泥盆世是北祁连—走廊沉积盆地的转换时期。除天祝、古浪、景泰及肃南等局部地区发育下志留统钙碱性系列火山岩以外，全区志留系均以碎屑岩沉积为主。志留系底部多见—套砾岩层。下—中志留统为典型复理石相的浊流沉积。上志留统变为滨浅海相磨拉石沉积。早、中泥盆世雪山群为典型的陆相粗碎屑磨拉石沉积。从空间分布上看，志留系—泥盆系在走廊—北祁连地区也有自北向南厚度加大、粒度变粗的特征，古流以由南向北、来自造山带的古流为特征。北祁连-河西走廊奥陶纪弧后盆地火山岩—志留系复理石-海相磨拉石—中、下泥盆统陆相磨拉石的充填序列以及空间分布特点，反映为典型的弧后盆地向前陆盆地转化的沉积序列。

海啸(或称津浪，tsunami)是海底地震(海震)火山爆发等因素引发的巨浪。海啸可以在海底形成特殊的事件沉积——海啸岩。海啸岩主要由具丘状层理、平行层理、块状层理及亮错层理的粗碎屑岩或碎屑麦岩组成，它们与触发海啸的地震、火山形成的震积岩、火山岩紧密共生。根据云南滇中地区中元古代昆阳群大龙口组的观测研究，认为大龙口组中存在典型的震积岩(包括震裂岩、震褶岩、自碎屑角砾岩)。与之共生的具丘状层理、平行层理的内碎屑副角砾岩、含砾砂屑灰岩为海啸岩成因，它们组成典型的震积岩一海啸岩序列。

广西北海涠洲岛晚更新世湖光岩组为一套火山碎屑沉积，同期火山岩发育。在靠近火山口的地区，湖光岩组发育一系列地震成因的同沉积变形构造，包括：地震微断裂(张扭性地震微断裂、张性地震微断裂、共扼性地震微断裂和阶梯状地震微断裂)、微褶皱纹理、落石沉陷构造和砂泥岩脉。分析认为这些同沉积一变形构造是由同期火山活动引起的地震作用形成的。

The North Qilian orogenic belt is an elongate tectonic unit that lies between the North China plate to the north and the Middle Qilian microplate to the south, and is formed by a collision of the two plates in the Caledonian. The Shihuigou Section from Yongdeng County, Gansu Province, is in the eastern sector of the North Qilian Mountains, spanning the Ordovician island-arc zones. The Zhongpu Group is distributed in the Shihuigou area and composed of mediumbasic volcanic rocks and volcanic clastic rocks interspersed with cherts, limestones, slates, and metamorphic sandstones.The geochemistry of chert from the Zhongpu Group reveals that all cherts coexisting with island-arc volcanic rocks formed in a continental margin basin environment. Research results of the rare earth elements reveal that these cherts formed in a relatively deep-water basin with no significant terrestrial interference. Therefore, it is inferred that the North Qilian orogenic belt was previously an archipelagic ocean in the Ordovician.

地震是一种灾害性的地质事件。地震及其引发的海啸、重力流可以形成震积岩、海啸岩和震浊积岩。在地震过程中，震积作用可以形成特殊的构造标志（地震断裂层、地裂缝、微同沉积断裂、微褶皱纹理、重力断层等）、沉积和成岩标志（砂岩脉、泥岩脉、泥晶脉、即磨牙(molar tooth)构造、枕状层、砂火山、泥火山、同沉积变形构造、丘状层理等）。地震沉积组合包括原地震积岩（A，包括震裂岩、震褶岩、自碎角砾岩、内碎屑副角砾岩等）、海啸岩（B，由具丘状层理、平行层理的碎屑岩或内碎屑灰岩组成）、震浊积岩（C，由具块状层理、递变层理或玻马序列的粗碎屑岩或碎屑灰岩组成）及背景沉积（D）4个单元，它们组合成A-B-C-D、A-B-D、A-C-D、A-D、B-D、C-D等6种类型的沉积序列。