浅谈日本纹章瓷

西方中世纪时期,王权常常形同虚设,各城邦之间战争不断,既为在战争中辨别敌我以避免伤及战友,也为了树立自身城邦形象,欧洲纹章在这种背景下约于12世纪末兴起。最初只绘制于盾牌上,后来扩展于各类器物和建筑上,其使用范围亦从国家城邦象征向贵族、教会以及其他普通团体和民众扩展,成为体现欧洲文化最典型的象征之一,不过,时至今日,欧洲纹章的主要形式仍然保持盾形。     

中共十一届三中全会研究述评

1978年召开的中共十一届三中全会,结束了粉碎四人帮后的两年徘徊中前进的局面,重新确立了马克思主义的思想路线、政治路线和组织路线,做出了把工作重点转移到社会主义现代化建设上来的战略决策,揭开了改革开放的序幕,以此为起点,中国走上了建设有中国特色社会主义新道路。近30年来,对这一实现伟大历史转折的重要会议的研究成果非常丰富。     

近十余年来魏晋南北朝女性史研究述评

近十余年来,我国史学界对魏晋南北朝女性史的研究已呈现出可喜的态势。这一时期的婚姻具有明显的政治色彩,但婚姻文化也相对开放、自由;同时,女性诸多方面的社会地位也明显提高,但这在中国历史上也仅仅是个相对的概念,在总体上,这一时期的女性依旧处于社会的从属地位。另外,由于魏晋南北朝时期社会的动乱,儒学的衰微,外来文化的影响,也促进了女性生命意识的复苏,人格的觉醒和理性的重新发现。总体而言,学术界对魏晋南北朝女性的研究是范围广,层次多。角度新,但依旧不够全面,宏观胜于微观。     

难以割舍的故乡情

奔波在水泥砖石建成的“森林”中,尤其置身于如鸟笼一般的楼层里,滞涩的空气少了许多大地生发的灵鲜水活,让人有一种压抑的感觉,随着时间的推移,对绿色原野便产生出强烈的思恋,有时甚至到了梦牵魂绕的地步。     

厦门宋元窑址调查及研究

厦门宋元窑址的调查及研究表明,厦门古代陶瓷的生产和发展,不仅得益于优越的自然地理条件,而且同当时的海外市场需求和外贸的发展相辅相承,同时厦门古代陶瓷手工业的发展也带动和促进了厦门及闽南地区社会经济的进步。     

船桥会与清代陕南地方社会

船桥会是清初至民国末年汉江流域普遍存在的民间组织,它依托渡口而存在,并募集资金以建桥造船,利涉汉江.清代陕南船桥会内部实行有章可循的科层制管理,权责明晰.绅粮公议基础上推举的首士和会首在任期内全权负责船桥会事务,会首掌管会产,冬则搭桥,夏则造船,并负责拣选和雇佣水夫、巡河.水夫负责摆渡,巡河负责监督.南郑县案例表明,水...     

抗战时期国民政府的儿童福利政策述评

抗日战争爆发后,国民政府和社会慈善机构采取一系列措施急救难童,重视难童的教养工作。尽管在整个抗战时期,国民政府所推行的儿童福利政策存在着很大的局限性,但其制定的“善种、善生、善养、善保、善教”的儿童福利政策,还是初步显现了现代儿童福利观念的某些特征。应该说,抗战时期国民政府在难童救济与教养方面的努力还是值得肯定的。     

基于扎根理论的共享住宿选择意愿影响因素及机理研究

共享住宿是在共享经济背景下发展起来的一种新兴住宿模式,现已受到众多消费者青睐,但目前针对我国文化和市场条件下的共享住宿选择意愿还缺乏系统研究.基于此,本文对26位国内共享住宿平台用户进行深度访谈,采用扎根理论方法,利用质性分析软件NVivo10对访谈资料进行整理分析,归纳了共享住宿选择意愿的影响因素及影响机理.结果表明...     

游客慢文化感知维度分异与影响因素研究——以高淳国际慢城为例

本文以深入挖掘慢文化内涵为基础,选取高淳国际慢城为案例地,对游客慢文化感知进行调查,构建游客慢文化感知维度分析模型,探讨游客慢文化感知差异及其影响机制。结果表明:(1)慢文化是人类社会在创造物质和精神财富过程中体现回归自然、社会节奏放缓、注重生命意义和生活品质的一种生活状态与文化形态;(2)游客对慢文化的感知存在四个维度,且呈现出慢文化氛围、慢文化产品、慢旅游经济性和慢旅游便捷度的递减关系,表明游客对慢文化的感知相较于显性文化,更注重隐性文化;(3)游客个体因素和旅游感知距离对慢文化产品、慢文化氛围和慢旅游经济性有影响,感知刺激因素对慢文化产品有显著影响,但各影响因素对慢旅游便捷度感知无影响。     

Quantitative estimation of overpressure caused by gas generation and application to the Baiyun Depression in the Pearl River Mouth Basin,South China Sea

Hydrocarbon generation can yield high fluid pressures in sedimentary basins as the conversion of solid kerogen to hydrocarbons can result in an increase in fluid volume. To quantify the relationship between gas generation and overpressure in source rocks, a set of equations for computing the pressure change due to gas generation has been derived. Those equations can be used to quantitatively estimate overpressure generated by type III kerogen in source rocks by considering gas generation and leakage, gas dissolution in formation water and residual oil, thermal cracking of oil to gas, and hydrocarbon episodic expulsion from source rocks. The equations also take consideration of other factors including source rock porosity, transformation ratio, total organic carbon (TOC), hydrogen index, and compressibility of kerogen, oil, and water. As both oil and gas are taken into account in the equations, they can also be used to estimate the evolution of overpressure caused by hydrocarbon generation of type I and type II kerogen source rocks. Sensitivity analyses on the type III kerogen source rock indicate that hydrogen index is the most influential parameter for overpressure generation, while TOC and residual gas coefficient (β: ratio of residual gas over the total gas generated) have a moderate effect. Overpressure can be generated even if the gas leakage/loss in the source rock is up to 80% of the total gas generated. This suggests that the internal pressure seal of the source rock is not a critical factor on the pressure change as long as the source rocks are capable of sealing liquid oil. The equations were applied to evaluate the overpressure in the Eocene–Oligocene Enping Formation source rocks due to hydrocarbon generation in the Baiyun Depression, the Pearl River Mouth Basin by considering the source rock properties, hydrocarbon generation history, and hydrocarbon expulsion timing. Two episodes of overpressure development due to gas generation and release were modeled to have occurred in the Enping Formation source rock since 16 Ma. The overpressure release at 10.2–5.3 Ma via hydrocarbon expulsion was apparently related to the Dongsha phase of tectonic deformation, whereas the pressure release at 2–0 Ma was due to pressure generation that was exceeded the fracture‐sealing pressure in the source rocks.