共查询到17条相似文献，搜索用时 62 毫秒
1.
禄丰古猿化石地点偶蹄目化石初步研究 总被引：3，自引：0，他引：3
云南,禄丰古猿化石地点经9次发掘,偶蹄目化石与哺乳类其他目一样,不仅材料增多,而且发现了新的属、种。经初步研究,由已记述的12种增加到22个种类,其中一部分是与华北时代相当于保德期的动物群有密切关系的属、种,另一部分是与南亚印、巴次大陆中西瓦立克动物群有亲缘关系的类型,其地质时代为中新世晚期,相当于欧洲陆相地层哺乳动物分期的土洛里。 相似文献
2.
3.
描述了产自云南禄丰古猿化石地点的犀科化石禄丰无鼻角犀新种(Acerorhinus lufengensis sp. nov.)和林氏山西犀相似种(Shansirhinus cf.S.ringstroemi)。A.lufengensis的个体较大;原尖不收缩或微弱收缩,次尖几乎不收缩,反前刺缺失或非常微弱;前臼齿前尖肋强壮;臼齿前刺短小,无内齿带,除M3外无小刺;下前臼齿的下内脊呈横向;下门齿呈特别粗壮的獠牙状。从A.lufengensis的一系列进步性状判断,它的时代至少不会早于M3外脊和后脊分界明显的A.palaeosinensis,应相当于晚中新世的NMU10或MN12,年龄约7 Ma。S.cf.S.ringstroemi具有丰富的釉质褶皱、微弱的前尖肋、非常强大的前刺、强烈收缩的原尖、发达的齿桥和中窝、角状的U形内谷、连续的内齿带、膨大成方形的次尖等。在这个种内,体型有增大的趋势,釉质褶皱向增强的方向发展,中窝数量增多,而禄丰标本在尺寸上略小于甘肃临夏的上新世最早期材料,釉质褶皱也相对更弱,中窝仅有一个。因此,禄丰S.cf.S.ringstroemi的时代应该略早,出现于晚中新世的7 Ma左右是比较合理的解释。 相似文献
4.
5.
本文记述了近年来经过多次发掘和采用筛洗方法从禄丰古猿化石产地获得的一批竹鼠化石标本,共有一属3种: Brachyrhizomys nagrii;Brachyrhizomys cf.pilgrimi和Brachyrhizomystetracharax以及2枚单个牙齿属于暂不宜订种属的类型。 相似文献
6.
7.
8.
描述了产自云南禄丰古猿化石地点的豪猪化石禄丰豪猪 (新种 ) (Hystrixlufengensissp .nov.)。这是一种较原始的豪猪。它的个体中等 ;两上颊齿列往前靠近 ;下颌骨骨体较低 ,齿隙稍凹 ,其前端高于下颊齿冠面 ;颊齿齿冠较低 ;上颊齿舌侧沟横向较短 ;P4大 ,前尖通常孤立 ,中附尖很发达 ,不与中脊连 ;M3较少退化 ;上颊齿具 3齿根 ,大的内侧齿根具明显纵沟 ;下颊齿通常具 4齿根等。形态结构分析表明 ,H .lufengensis仅比H .parvae进步 ,比H .primigenia和H .sivalensis及其他种都原始。它可能代表亚洲目前已知最早、最原始的豪猪。其产出时代为晚中新世保德期 (狭义 )的较早期 (距今约 8Ma)。 相似文献
9.
禄丰古猿化石地点的鱼化石 总被引：2，自引：0，他引：2
在禄丰古猿化石产地采获许多鲤的咽喉齿化石,由形态特征看,相近于现代广泛分布的鲤(Cyprinus carpio Linn.)的咽喉齿,当代表其早期记录。现今云南一带生存有多种鲤,可能为其繁衍的后代,且相当繁盛。这一发现为鲤属(Cyprinus)起源于亚洲提供了化石依据。 相似文献
10.
述了采自云南禄丰晚中新世石灰坝组的仓鼠类化石—新种──Kowalskiahanaesp.nov.。后脊Ⅱ和三齿根在M1中所占的比例、第一臼齿前边尖的宽度以及第三臼齿的退化程度表明,新种的演化水平与欧洲瓦里士晚期或土洛里早、中期的K.schaubi,K.fahlbuschi和K.skofleki接近,它是我国现知科氏仓鼠属中构造最原始的一种。 相似文献
11.
It is more and more clear that the fossil materials from the Ramapithecus locality of Lufeng respresent a very complete association of Vertebrates and the most rich assemblage in the Pontian mammalian faunas of South China. Seven forms of Carnivora were reported by the author in 1979. Up to now, twenty seven forms of the order have been found. The taxonomic unit, distribution in the different layers of the Seetion D and the specimen count of each form can be seen in Table 1. This paper only reports the preliminary results of the Carnivora fossils of the Lufeng mammalian fauna. A detailed study of these specimen will be published in future article.<br>Most of the new forms added to the list of Carnivora are bears, civets and mustelids. Four, ten and three forms have been referred to Ursidae, Mustelidae and Viverridae respectively.<br>Among the fossils, only a few specimens of two forms (Sivaonyx bathygnathus and Ictitherium gaudryi) were collected from the first layer and the rest came from the second layer and below. This fact indicates that possibly the required living conditions for most of the forms had changed and they no longer existed in the first layer. It tallies with the situation shown in the deposits such as a clear erosin surface between the first and second layers and difference of the upper and lower layers in composition.<br>Ictitherium gaudryi is the most abundant one of twenty seven forms (67 specimens) . Secondly, Sivaonyx bathygnathus (29 specimens) , Epimachairodus fires (19 specimens) and Pseudaelurus sp. (14 specimens) are also common. In addition, Ursavus depereti, Indarctos sp. and Ursinae indet. are represented by more than 12 specimens. The rest are quite rare.<br>In the Carnivora of Lufeng, sixteen forms can be identified to the genus level. At least two genera (Sivaonyx and Ursavus) were not reported from chinese Neogene deposits before and it is possible that certain forms of mustelids and civets are also new for the fossil record of Baodean (or Pontian) in China. Miocene linsang and binturrong may exist in the Viverridae and another form, previsionally attributed to Mustelidae indet. (2) is also a problematical one.<br>Compared to the late Miocene faunas of Europe and North America, Lufeng fauna shows close relations to them. Considering the Carnivora, at. least ten genera (Indarctos, Ursavus, Martes, Eomellivora, Lutra, Sivaonyx, Ictitherium, Epimachairodus, Pseudae-lnrus and lelis) can be found in Europe and six genera (Indarctos, Martes, Eomellivora, Lutra, Pseudaelurus and Felis) exist also in North America. Some affinities to Africa were indicated by a few genera (Ictitherium and Felis) .<br>In comparison with the \"Hipparion fauna\" of North China and middle Siwalik fauna of India-Pakistan subcontinent, Lufeng fauna has its own distinguishing features. As shown in Table 2, five families (Ursidae, Mustelidae, Viverridae, Hyaenidae and Felidae) all appear in the three faunas. Seven genera (Indarctos, Martes, Eomellivora, Ictitherium, Epimachairodus, Pseudaelurus and Felis) are common for all faunas. Proputorius and Lutra are present at Lufeng and other localities of North China. Sivaonyx is common to that of Lufeng and Siwalik.<br>Of eight forms identified to species level, two (Proputorius lufengensis and Epimachairodus fires) are new species. Ursavus depereti can only be found in the Torolian fauna of Europe. Four (Indarctos sinensis, Eomellivora wimani, Martes palaeosinensis and Ictitherium gaudryi) of the forms are limited to the Baodean of North China. Sivaonyx bathygnathus not only lived in Dhok Pathan fauna (corresponding to Turo lian of Europe) , but also occured as early as Nagri (corresponding to Vallesian of Europe) of South Asia.<br>Judging from the comparisons of the micromammalian fauna and the other orders of Lufeng fauna, it is possible that the geological age of Lufeng fauna corresponds to Dhok Pathan of the middle Siwalik of South Asia (or Selenoportax lydekkeri IntervalZone offered by Barry J. C. et al. in 1982) and Turolian of Europe.<br>The composition of Lufeng Carnivora lacks canids and amphicyonids as in the Baodean of North China and some forms of civets fossils are relatively rather common. In general, the living forms of many civets are typical beasts inhabiting tropic or subtropic forests. The otters and some mustelids reflect restricted palaeoecological enviroments generally associated with aquatic conditions. The large cats and bears are said to be \"forest-dwelling\"usually.<br>Further research with the Lufeng fauna and associated conditions may be resolved in the near future. 相似文献
12.
Lufeng rhizomyid fossils collected by exeavation and underwater sieving of fossili-ferous sediments, are studied in this paper.<br>The specimen referable to Brachyrhizomys nagrii is a left lower dentition with M1—M3(V. 8126) . Length of M1-M3, is 11. 75 mm. Both size and characters (such as short M3 and an elongated mesolophid on M3 ) agree well with Siwalik specimens (Fig. 4).<br>The specimens identifiable to Brachyrhizomys ef. B. pilgrimi are a left dentary with M1—M3 (V8127. 1) , a right M3 (V8127. 2) and an I1 (V8127. 3) . This is a large species with heavy deep dentary (depth below M=15. 4 mm) and massive incisors. It also is the biggest one of three species of Lufeng Brachyrhizomys. An apparent trait is suppression of mure on Mo-3. The narrow connection may not be present in early wear. Length of M-Ms is 15. 6 mm and more closer to B. ef. pilgrimi than to B. pilg- rimi of Siwaliks in size (Fig. 5, A, B and C).<br>The third species is B. tetracharax to which the most of the rhizomyine fossils from Lufeng Ramapithecus locality belong. The materials include an incomplete skull and associated lower jaw (V8128. 1) , five maxilla fragments (V8128. 2—6) . fourteen lower jaws (V8128. 7-20) . Fifty five isolated upper and lower ehack teeth (V8128. 21-75) , eleven isolated upper and lower incisors (V8128. 76—86) . Unfortunately, the skull and assoeiated lower jaw are crushed and fiattened laterally (Fig. 6, A) . The portions of it preserved are the ear region of two sides, partial right palate and left zygoma、partial maxilla, premaxilla, temporal bone and nasal. The infraorbital foramina were damaged and the shape of their ventral slit ean not be observed. The dentary is deep. In general, the upper dentition is longer than the lower one. Average length of them is 12. 28 mm and 14. 30 mm respectively. It is undoubtedly to refer the specimens from Lufeng to B. tetracharar, although there is discrepaney between the dimensions of the cheek teeth of Lufeng and Siwalik. M' has four roots. Ma elongates transversely. There is a strong mesolophid on M2 and an evident mure on worn M2-3. M, extends longitudinally. These traits distinguish the specimens from the other speeies easily. The yariations of upper and lower eheek teeth manifested by differences of wear stage in size and pattern of occlusal surface are shown in Fig. 6.<br>In addition, two isolated cheek teeth are referred to Rhizomyidae indet. A right M' with four roots (V8129) possesses an antero-lingual flexus (Fig. 7) . Another right M5 with a root (V8130) has been well worn and only retained lingual reentrant and three enamel lakes on oeclusal surface (Fig. 8).<br>The best known record of rhizomyid evolution is doeumented in Siwaliks of Pakistan. It is considered to be a standard for comparison of fossil rhizomyids through. out the world especially Asia. Three species of Brachyrhizomys mentioned above have known temporal ranges in Pakistan and eoexisted for a short time at 8 Ma. So Lufeng hominoid fauna can be placed about 8 Ma or perhaps a bit later. 相似文献
13.
Ursavus在中国的首次发现——并记禄丰古猿化石产地的其他熊类标本 总被引：2，自引：0，他引：2
本文记述的是1981年在禄丰古猿化石产地发掘中发现的熊类标本,共有二属二种和一种暂不能确定属、种的类型。其中祖熊(Ursavus)过去只见于欧洲、北美和西亚的中新世地层,在我国还是首次发现。禄丰的标本,就其大小和特征可归于Ursavus depereti;印度熊(Indarctos)过去在我国发现过两个种:中国印度熊(I.sinensis)和拉氏印度熊(I.lagrelli),禄丰的标本为前一个种;第三类型与Protursus和Ursus都有相似之处,但又有区别,鉴于材料不足,暂不订属和种。 相似文献
14.
15.
Lufeng is a county of Yunnan Province, about 60 km. to the west of Kunming city (Fig. 1) . Shihuiba locality (No. 75033 IVPP) (102°4' E, 25°1'N) is situated on the southern slope of Miaoshanpo Hill, about 9 km. north of Lufeng county.<br>Geomorphologically, Lufeng area is a small block basin, located in the east of the middle Plateau of Yunnan. Average height of it is about 1560 m. above sea level. The basin extends about 12 km. from south to north and about 2-3 km. from east to west. In its northern end, the most narrow part is only 0. 3-0. 5 km.<br>There are three rivers (the West River, the East River and the South River) in the basin. They join near Lufeng county and then is called Xingsu River (Fig. 2) .<br>The form and development of Lufeng basin were controled by a series of faults of south-north direction. The base and margin of the basin consist of strata of Presinian period mainly, in addition, Jurassic and Cretacious periods. The distribution of Cenozoic beds is only restricted to the piedmont or the center of the basin.<br>The strata of Presinian period called Kunyang Group, is a suite of thick metamorphic limestone and mudstone, topographically expressed as well-round, lowlying mountains and hills. The Mesozoic deposits are so called\"Red Beds\". They are identified as Fengjiahe (Early Jurassic) , Zhanghe (Middle Jurassic) and Jiongdihe (Late Cretacious) , Matoushan (Early Cretacious) formations respectively. In the Cenozoic strata, the Neogene beds are fluvial-laeustrine swamp deposits, consisting of sand, gravel, sandy clay, clay and lignite, about 30 m. or more in thickness, and exposed in Shihuiba, Tuguaneun, Taizicun, Lufeng and Xiabanqiao-Yangjiahuayuan. The Quarternary beds are fluvial gravels and terrace deposits, directly overlying on the old bedrock and the terraces of several rivers.<br>Miaoshanpo Hill on which Ramapithecus fossil locality lies consists of Kunyang Group, greyish white, greyish blue and in part pink microlitic dolomitic limestone and purplislh grey sericite slate intercalated with secondary belts of quartz. The Section A, B and C were exposed at different locations of a artificial road trough going to the back of the Miaoshanpo Hill for excavating limestone. In addition, the lignite deposits of lacustrine swamp face surrounding the Section D were exposed when Chengkun RaiIroad was built, the earthy crust of Miaoshanpo Hill was eradicated and pushed to the roadbed of the Railroad. The deposits have been excavated for 9 times since 1975 andthe location of the excavated section has been moved much westward.<br>The sequences of the Sections A and D are summarized from top to bottom in turn as following, mainly according to the observations of 1983, also refering to the sections over the years (Fig. 4 and 5) .<br>Section A:<br>1. Dark purple, purple, orange red weathering crust. Earthy deposits with porousities and plant roots. There are sands and gravels in the bottom. Average diameter of the gravels is 1-2 cm. The layer is 1. 5-3. 5 m. in thickness.<br>2. Yellow, yellowish drab calcareous clay and sandy clay with clear horizontal bedding. Deposits coarsen gradually from lower to upper. The clay is pure and hard, nearly without root casts and holes. It is demareated from the lower layer by a eleor erosin surface. The space occupied by the layer shows initial landform. Thickness is 2-6 m.<br>3. Grey, greyish yellow, greyish brown clay with intercalations of sand and gravel. Deposits coarsen gradually from upper to lower. There are 2-3 belts of blackish brown carbonaceous clay. The thickness of each belt is 15-20 cm. About 1. 5-3m. in thickness.<br>4. Purple sandy clay with sands and gravels and clear bedding. Deposits coarsen downward. The diamater of gravels is 5-25 cm. The elements of them are quartz, sandstone, slate and limestone and so on. There are usually pollution motley and casts of root in the layer. The surface of the deposit was washed and wearthered, it looks like columnar. Exposed thickness is 5 m.<br>The sequences of the Sections B. and C are similar to that of the Section A. Any fossil of vertebrate has not been found from sections mentioned above yet.<br>Section D:<br>1. Yellow sandy clay with sand and gravel lenses. The color of the clay is brown contaminated by ferro-magnesium. The element of the gravel is mainly quartz with mediate roundness and diameter 1-—2 cm. The layer is demarcated by a clear erosin surface from the lower layer and lost at the northeast of the Section. About 0. 5-2m. in thickness. Dip SW 210°-220°, dip angle 5°.<br>2. Interbedding of blackish brown carbonaceous clay and greyish white fine sand. In general, there are four continued belts of carbonaceous clay and five small sand layers. Each elay belt and small sand layer is about 10-15 cm. in thickness. Their thickness and continued degree are various with the difference of section position. The sand contains abundant shell fragments of mullosc. Dip SW 210°, dip angle 5°-10°. Thickness 0. 7-3 m.<br>3. Blackish brown massive lignite with compact and solid texture. Partialy intercalating with blackish grey laminated sand and sandy clay. There are some burrows in the lignite occasinally. White spots and greyish green epiphytes are common in the bed. Dip Sw 210°-220°, dip angle 5°—12°. Thickness 0. 3-1. 4 m.<br>4. Interbedding of black carbonaceous clay and grey fine sand with clear texture of microstratifications. There are small and irregular lenses of lignite. About 0. 21. 8 m. in thickness. Dip SW 210°, dip angle 5°—10°.<br>5. Grey, uniform and pure fine sand with intercalations or lenses. of black carbonaceous clay and lignite. The color of the sand is more and more dark from upper tolower. There are a lot of shell fragments of molluse and quartz pebbles of diamater about 1-2 cm. Dip SW 210°, dip angle 5°-10°. Thickness 1. 5-2. 5 m.<br>6. Lignite consisting of two or three laminated layers. There are grey fine sand and blackish grey carbonaceous clay between the lignites. Containing plant fossil and woody fragments in the lignite. White and greyish blue epiphytes are common. Dip SW 210°—220°, dip angle 10°. Thickness 0. 5 m.<br>7. Greyish white, blackish grey clay with white small pebbles of quartz and nodules of pyrite. Exposed thickness in test pit of 1981 is 1. 6 m. No any vertebrate fossil has been found from the layer.<br>8. Purplish red, orange red, yellowish brown sandy elay. The layer has not been excavated during the excavations over the years. The thickness exposed in test pit of 1981 is 0. 8 m. Any vertebrate fossil has not been found from the layer.<br>These sections and their correlativities are shown in Fig. 4. Approximate 110 forms of vertebrate fossil have been found from the layers 1-6 of the Section D. The list of the fauna is shown in the chinese text.<br>Except Shihuiba, the Neogene strata have been also found in many places of the basin such as: Lufeng, Tuguancun, Taizicun and Xiabanqiao-Yangjiahuayuan and so on. The deposits can be divided into main two parts: the upper sand with gravel lenses and lower sandy clay with carbonaceous clay or lignite It is considered that the upper sand layer can correspond to the layer 1 of the Section D and the lower sandy clay layer can correspond to the layers 2-7 of the Section D. 相似文献
16.