Liu Zaihua Jiang Zhongcheng He Shiyi
(Karst Dynamics Laboratory, Ministry of Land and Resources, Guilin, 541004)

2 Excursion routes
ROUTE 1: September 10, Monday, 7:30 - 10:00: The Institute of Karst GeologyàYaoshan Mt.
(1)Yaoshan Mt.: Locating in the eastern suburb of Guilin, it got the name from the Yao Emperor Temple built in the Tang Dynasty on the mountain. It extends in N-S trend and has the hightest point in Guilin, which is 909.3 m a. s. l. The mountain is underlain by sandstone, shale of the lower part of Middle Devonian Series, covered by weathering product with remarkable thickness. To the east, south and west, it confronts the karst landforms. Standing on the top of the mountain, one can have a spectacular bird's eye view of the beautiful Guilin and the tower karst. So here is a good spot to understand the macro karst form in Guilin and its environment of formation.

Fig. 1 Schematic map of karst landform around Guilin area
1. peak cluster depression 2.peak forest plain 3.karst hill 4.non-soluble rock area 5.blind valley 6.underground stream 7.polje 8.gorge 9.resident point 10.river 11.highway 12.rail-way 13.stop or discussion point l4.cave (1)Yaoshan Mt. (2) Picturesque Guilin (3) Non-karst landform (4) Peak cluster depression (5) Peak forest plain (6) Cuesta peak (7) Karst Hydrogeologiecal Experimental Site (8)Reed Flute Cave (9)Shuinan Cave (10) Rentou Peak Red bed outcrop (11) Zhenpi Cave

The Yaoshan Mt. is also a good tourism place for its green trees and historical sites. In spring, many people come to enjoy the blossoming azalea. Besides the historical sites of the Bailu(white deer) Temple of the Tang Dynasty, the Baiyun(white cloud) Taoist Temple and the Mao Buddhist Convent of the Ming Dynasty, in the southwest foot of the mountain, there is a great and complete Jing Jiang King (brother of the first Emperor of Ming Dynasty) Mausoleum. On the both sides of the road in front of it, there are lifelike stone statues of man, tiger, lion, sheep, elephant and Chinese unicorn, and etc.
(2) The Picturesque Guilin: Looking westward from the top of the Yaoshan Mt., Gullin is located in a karst basin, extending N-S along the Lijiang River, and decorates with tower karst. The limpid Lijiang River has many tributaries around Guilin Town, such as the Taohua River, Xiaodong River, Nanxi River, and etc. So Guilin is a city surrounded by stone peaks and rivers, which looks very beautiful. Many of the isolated peaks have become scenic spots, in which the Folded Brocade Hill, the Fu Bo Hill, the Solitary Beauty Peak, the Seven Star Hill, the West Hill, the Through Hill, the Pagoda Hill, the Elephant Trunk Hill, the Reed Flute Cave, and so on are the most favoured by tourists.
(3) Non-karst Landform: Looking far away around Yaoshan Mt., if the weather is fine enough providing good visibility, you can see the non-kart areas distributed in the surroundings of the Guilin karst basin(Fig.9). The source of Lijiang River, Yuechengling Mt. at north is 2,142m a.s.l, about 2,000 m higher than Guilin karst plain. There are series of mountains and hills lowering down gradually towards the plain. The strata are lower Proterozoic slightly metamorphosed sandstone, slaty shales, phyllite, and lower Paleozoic non-soluble strata (Cambrian, Ordovician) overlain unconformably by quartz sandstone of lower Devonian Series, with some igneous intrusions. Contrasting to karst landform, the non-karst area is characterized by high relief, continuous mountain ridge, gentle hillslope and complete surface drainage system. The macroscopic higher relief in non- soluble rock area is probably a result of more intensive chemical weathering process than the physical one in humid and warm conitions.
The feature of distribution of the non-karst area around Guilin plays an important role in the karst development of the area, since they form a special hydrological pattern to let the karst area get a lot of allogenic water with very aggressive capacity. The recharge of the allogenic water brings about the differences between the peak- cluster depression and the peak-forest plain in both their distribution and landforms.
(4) Peak-cluster Depression: Looking southwards from Yaoshan Mt. there is a patch of peak-cluster depression. The framework of the landform shows certain regularity. It is composed of many pentagonal or hexagonal depressions distributed uniformly. A polygonal depression usually has an area of 0.06 to 1.00 km2 and a depth of 90 to more than 300 m, funnel-like or cylindrical in shape. The stone peaks are mainly cone shape, with slope over 50o. There are usually some sinkholes and shafts on the bottom of the depressions which drain surface water.
The peak-cluster depression usually distributes near the surface divide, with peak surface 400 to 700 m in elevation, which is 200 to 400 m higher than the nearby plain. It has a thick vadose zone but poor surface flow, so the infiltration of the precipitation is the main power of the geomorphic process. The distribution of the peak cluster depression is far from the area of surface river, which, from another side, indicates the great influence of surface river, especally allogenic river, on the formation of the peak-forest plain.
(5) Peak-forest Plain: From the top of Yaoshan Mt., it can be recognized that this subtype of tower karst is distributed along the Lijiang River and its tributaries, with the Guilin downtown area as its typical site. A lot of peaks stand separately on a plain, with relative elevation from 30 to 80 m, and a shape of tower and a density of 1.23 individual/ km2. The plain surface is even, more or less undulating, generally 150 m a.s.l, on the same level as the terrace of the Lijiang River. There are lots of waters, such as streams, ponds, wells and springs on the plain. It is, therefore, thought that the distribution of the peak- forest plain was closely related to the surface water flow, especially allogenic water flow. In fact, the larger the catchment area of the allogenic water, the broader the relevant peak-forest plain. Therefore, climate, geology and its resulted hydrological setting should all be considered as the main factors on the formation of the peak-forest plain.
(6) Cuesta Peak: It is generally considered that the tower karst was developed under humid and warm conditions. But various peak shapes in a small area are mainly controlled by geological factors, and not necessarily determined by climatic difference. For example, in the eastern part of Guilin downtown area, where the dip angle of the upper Devonian massive limestone is generally gentle or nearly horizontal, the peaks usually show tower or cone shape. However, in western part of Guilin, from the West Hill to the Dafeng Hill, limestone bed is generally dipping 20-30o eastward, so stone peaks are characterized by cuesta shape with asymmetrical profile, which shows a gentle slope on its eastern side and a steep slope on its west side(Fig.2). Near Ertang, 15 km to the west of Guilin, well-rounded isolated low knobs are developed on the lower Carboniferous medium to coarse grain dolomite.

Fig.2, Sketch map of cuesta peak near the Dafeng Hill

ROUTE 2: September 10, 10:00 - 12:30, Yaoshan Mt.-> the Guilin Karst Experimental Site
(7) Guilin Karst Experimental Site
The Guilin Karst Experimental Site was setup in 1986 in a former Sino-French cooperative project between the Institute of Karst Geology, CAGS, China, and the Laboratoire d'Hydrogeologie, USTL, France, which started from 1986, and finished in 1990. Now, the site is as a correlation site for IGCP 448 "World Correlation on Karst Ecosystem"(2000-2004).
The aim of the former project is to investigate the behavior of a karst hydrogeological system in the peak cluster (Fengcong in Chinese) region, which is a subtype of tower karst, characterized by many dolines scattered among group of stones peaks sharing the same basement. The peak cluster totals about half million km2 in southwest China, where more than 100 million people live. In the past decades, water resources estimation in region with topography of this kind has been carried out on different scale and for different purposes, i.e., for irrigation, hydropower construction, railway tunneling, mine dewatering, municipal water supply, as well as regional economical planning. However, the results of such water resources estimation are always questionable because little is known about the hydrological behaviors of karst systems in the peak cluster regions.
The 15-year operation of this experimental site has provided many new data from the works such as satellite and aerophoto interpretation, geological mapping, bore hole logging, meteorological and groundwater monitoring, tracing, karst geochemistry and isotope investigation, and storm response observation, which throws new light into the relationship between precipitation and outflow, and between karst processes and the global carbon cycle; the infiltration rate; the interior structure; and the hydrological and geochemical regulation function of the peak cluster karst ecosystem, especially of its epikarst zone. A comprehensive mathematical model for the karst hydrologic system has been set up.
The experimental site is near Yaji Village in the eastern suburb of Guilin, about 8 km to the southeast of Guilin downtown area. Geomorphologically, it is on the boundary between peak cluster land and peak forest land (Fig.1).
The history of Guilin tower karst could be dated back to Late Cretaceous, as is evidenced by the red calcareous breccia with Atopochara flora of Late Cretaceous which remain on the top of some isolated limestone peaks. Whether there is an evolution sequence from peak cluster to peak forest is controversial, but it is clear that the two subtypes are mixed to each other on the plane, and the peak forest is usually distributed in those area where fluvial process of allogenic water from non-karst area is strong, whereas peak cluster prefers those area beyond the influence of strong allogenic water.
The Experimental Site comprises a karst hydrological system which totals about 2 km2. Its recharge area is in peak cluster region with 11 dolines, whereas its output is composed of one perennial spring (S31) and three intermittent springs (S29, S291, and S32) at the eatern border of the Guilin peak forest plain (Fig.3). The altitude of the plain surface is about 150m, whereas that of the highest peak in the recharge area is 652m, and those of doline bottoms are ranging between 250m and 400m. The whole system is developed in Upper Devonian massive pure limestone. The dipping of the limestone strata is about 5-10o toward the southeast. There is a major fault striking NNE on the western boundary of the peak cluster region. According to surface survey and aerophoto interpretation, the major joints and fractures are NEE, NWW, and NNE oriented, and cast strong influence on the development of dolines and the flow directions of karst groundwater, e.g., the doline No.1, No.3, and No.4 are distributed along a major fracture zone with large calcite veins in NEE direction (Fig.3).
Minor karst features such as karrens, grikes, kamenitza are well developed on doline slope, and they are concentrated in surface zone (the epikarst) 3-10m thick. The biggest cave found in the Site is on the mountain slope, east of the spring S291, the altitude of its entrance is 197.5m. The accessible part of the cave is 100m long, 1m to 20m in width, and 5m to 20m high. During storm rainfall, a slope runoff about 30 l/s recharges into the cave, and from the hydrochemical data, it is supposed to be related to the outflow of S291. There are also some fossil caves, e.g., a cave filled up by breccia of violet red siltstone and siliceous grain was encountered in bore hole No.9 at a depth of 100.7m to 158m.

Fig. 3 Monitoring network of the Experimental Site
1: doline; 2: road; 3: motor way; 4: boundary between peak forest and peak cluster; 5: spring; 6: bore hole; 7: fault

The karst hydrological system of the site is characterized by very thick aeration zone, heterogeneous interior structure, and uneven input and output (Fig. 4). The thickness of the aeration zone is 110m to 400m. The heterogeneity of the system's structure is featured by the existence of the epikarst zone, and the co-existence of big conduits and micro-fissures beneath the epikarst, e.g., two (CF6 and CF9) of the four bore holes in the recharge area hitted the conduit, and showed great water table fluctuation during storms (about 30m in CF6, as recorded by a water level auto-recorder), but the other two (CF7 and CF8) didn't. In addition, five bore holes around spring S31 show similar feature. The input of the system is solely rainfall, and the multiyear mean annual precipitation around Guilin is 1914.3mm, however, 75.42% of which is concentrated in the rainy season from April to August. Moreover, according to the data from five precipitation auto-recorders setup at different parts of the Site, both the monthly rainfall and that of a storm event are varied remarkably from the plain to the dolines, and from the lower doline to the high doline. The discharge from four springs at the output of the system are shown in Table 1. Their great fluctuation is not only the reflection of the uneven input, but also the heterogeneity of the system's structure.

Fig 4 Schematic profile of Yaji karst hydrological system
1: soil cover; 2: epikarst spring; 3: phreatic spring; 4: karst conduit

In the recharge area, there are quite a few epikarst springs flowing out from the doline slope or its bottom, some of them are perennial (e.g., S25, S55), others are intermittent (e.g., S54, S56).
By multiyear monitoring, some interesting findings have been found from the Experimental Site as follows:
1) The hydrological regulation function of the epikarst zone
During the storm, the regulation function of epikarst zone to the hydrological system could be clearly seen. Although the doline slope can absorb most of the rainfall and slope runoff, water do not drop down through the vadose zone to the phreatic zone straightly but rather form a flow running in the lower part of epikarst zone at a depth of a few meters below ground surface. Many epikarst springs flow out on the lower part of doline slope, some even with the appearance of "artesian spring", e.g., the S56 spring, with a discharge of maximum 30 l/s, flowing out at an altitude of 110m higher than the general output S31, nevertheless there is no impermeable bed whatever beneath it. The confluence of epikarst springs flow into swallet near bore hole CF6 in doline No.1, and recharge the spring S31. Evidently, all these processes prolong the flow time of water in the karst system, and thus smooth the hydrograph.
The Yaji karst hydrologic system is conceptualized as having three regulation reservoirs, namely, the first regulation reservoir-the epikarst zone, the second regulation reservoir-the vadose zone below the doline bottom, and the third regulation reservoir-the phreatic zone. Based on this conceptual model, a hydrological mathematical model is set up, which takes into account different types of parameters for different regulation reservoirs. The result of discharge simulation by this model for spring S31 and other sub-karst systems is satisfactory. Employing this model, the percentage of water regulated in different reservoirs of the system and the percentage of rapid flow and slow flow in the system at different time could all be identified. This will improve greatly the water resources estimation in karst region of peak cluster landform.
2) Sensitivity of karst processes to soil CO2 change or the change of land use
Fig. 5 shows seasonal change in [Ca2+] and [HCO3-] in water, and soil CO2 partial pressure at the Guilin Karst Experimental Site.
It can be seen that soil CO2 partial pressure changes remarkably during a year, with maximum in the summer growing season, and minimum in cold winter. Related to this, the [Ca2+], [HCO3-] in water also show remarkable coincident change. That means that karst processes are very sensitive to the soil CO2 change. In addition to the seasonal change, Figure.5 also shows the increase in soil Pco2 in a multi-year scale. The latter is related to the reforestation at the site since 1993, and/or the increase in the atmospheric CO2 content (Harrison and others 1993). The increase in soil Pco2 drives the dissolution of carbonate rock, resulting in the increase in [Ca2+], [HCO3-] of karst water. This is also evidenced by the fact that the corrosion flux of limestone tablets in the Guilin Exp. Site increased from 1993 to 1995 (Table 2).

Fig. 5 Seasonal and multi-year change of hydrochemistry and its sensitivity to the change in soil CO2 partial pressure

(3) Water-rock interaction theory is difficult to explain the feature of hydrochemical variation at the Site
Fig.6 shows physico-chemical records of water in bore hole No.1, which was drilled in fissured karst media at the Site. It can be seen that the system has unusual physico-chemical variation during a storm, that is, conductivity of water was lower, and pH was higher under base level; whereas the conductivity of water was higher, and pH was lower during the storm. Obviously, this can not be explained by conventional water-rock interaction theory, because according to the theory, conductivity of water should decrease during the storm, as the time of water-rock interaction is shorter at this time. In addition, the monitoring results in bore hole No. 5, which was drilled in fissured-conduit karst media, show that the conductivity of water was even higher than that in the bore hole No.1 of 5 meters away under base level (Fig.7). Moreover, the physico-chemical variation of water in bore hole No.5 was more stable. This is also in the opposite direction by the conventional water-rock interaction theory. We think that it is necessary to consider water, rock and CO2 gas as a whole in explaining the physico-chemical variation of water in karst system, because we have found higher partial pressure of CO2 in the system during a storm-event (e.g. 12000ppm, compared to 8000ppm at normal time in Autumn season), which dissolved more limestone, and thus increase the conductivity of water.

Fig.6 Physico-chemical variations of water in bore hole No.1 at the Site
Note: The bore hole No.1 was drilled in fissured karst media.

Fig.7 Physico-chemical variations of water in bore hole No.5 at the Site
Note: The bore hole No.5 was drilled in conduit-fissured karst media.

4) Karst ecology of the Site and their environmental effects
It's investigated by using the methods of standard sample square statistics (4m′4m in bush area and 1m′1m in grass area) and sample belt survey that there are 128 species of vascular plant distributed among 32 families and 70 genera in the main part of the Site (about 2km2), including 124 species of spermatophyte among 29 families and 67 genera, and 4 species of fern among 3 families and 3 genera. Statistically, investigated result shows that Vitex negundo (PhotoⅤ-1), Loropetalum chinnensis (PhotoⅤ-2), Phyllostachys sulphurea and Rosa cymosa have the highest density. They consist of the fundamental pattern of the secondary bush vegetation in the Site and also present the colony constructing species of recent evolution stage. The present flora structure reflect that the existing vegetation belongs to secondary grass-bush plant, which is now in the early stage of positive evolvement in such a bare karst area. At the same time, the fact that a few kinds of survival species, such as Sapium rotundifolium and Ficas microparpa etc., of subtropical primitive karst forest was found at the steep slope of doline indicates that the natural vegetation in the Site has not been thoroughly destroyed. Therefore, the seed pool in soil cover does not lose a lot. Unfortunately, the most part of the Site, especially the bottom of doline and the gentle slopes, was destroyed by fire once a year before 1993. This has led to the great lose of almost all the seeds of primitive karst forest species. As a result, Vitex negundo and Loropetalum chinnensis, the pioneer plant of secondary bush cluster, are growing very well in the Site. The appearance of these two species also indicates that the soil is acidic.
Moreover, we also found a great deal of predominant species or colony constructing species of natural subtropical karst plants at Putuo Mt. in Seven Star Park, 10 km west from the Site, where the vegetation is well protected. Therefore, it is deduced that the karst forest situation before being destroyed in Guilin region is very similar to the existing natural karst forest in the southern of Guizhou Province (Zhu Shouqian et al). The results have further verfied that the most stable karst forest plant in subtropical region is controlled by edaphic and topographic conditions.
Some environmental effects have been observed in this Site in comparison with karst forest area of southern Guizhou separately（He Shyi）. The result shows that in the Experimental Site the meteorological factors vary in accordance with the regional climate change. The maximum annual temperature difference is 33℃ and the maximum annual variation of air relative humidity is over 80%. However, in the Guizhou karst forest area the situation is very different, the correspondent parameters are 18.3℃ and 40% respectively. Meteorologically, there is no frigidity in winter season and no extreme hot in summer season within the dense forest, with daily air temperature and humidity change of no more than 8℃ and 35% respectively. Compared with the forest ecosystem, the regulation effect of vegetation to micro-climate in the bush ecosystem of the Site is much weaker, and the change of local meteorological factors is controlled by geomorphological condition, i.e. the air temperature is high at the bottom of doline where the air flows slowly, on the contrary, the air flows quicker at the puerto place and the heat accumulation effect is not so distinct. Moreover, owing to the lack of vegetation coverage on the ground surface, the bare carbonate rock absorbs the heat from sunshine greatly and makes the temperature of rock surface very high (the highest observed is 58℃ in summer season). This is very harmful to the positive evolvement of ecosystem itself.
ROUTE 3: September 10, Monday. 14:30 - 18:00, The Institute of Karst Geology--> Reed Flute Cave à The Institute of Karst Geology
(8)Reed Flute Cave : 176 m a.s.1. in altitude, it is situated on the southern side of the Guangming (Bright) Hill, and 8 km to the northwest of Guilin city. Its plane is in a shoe shape, 240m long in E-W and 50 - 90 m wide in S.N direction (Fig.8). The major cave consists of a big hall, with a floor space of 14,900m2 and height of 10 -18 m. There are some small branches in the cave, where sinkholes can be found.
Speleothems are well decorated, especially near the entrance. The dripping water is rich and the dripstone are not only in various types but also in big size, displaying a wonderful cave world. This cave was called" The Art Gallery of Mother Nature ". It is worth notice that there are more speleothem near the entrance than other part of the cave. This is because there is a minor fault and consequently dripping water is more abundant. Moreover, the stalagmites are generally longer than the corresponding stalactites, and can reach more than 10 m, which suggests quicker speed of dripping water . Besides the dripstone, shield and flowstones such as rimstone, bacon are also developed. Moreover, one can see a kind of circular roof mosquito net, that is, a bacon hanging under a shield. In the middle part of the cave, the rock on the cave ceiling is more complete, so the speleothems are few. But on the cave floor there is a pile of collapsed stone blocks of 15 m thick , with some stalagmites grew up on it.
It is considered that the complicated cave structure, big hall with abundant speleothem of considerable size reflect the subsurface karst features under the humid and warm conditions.
(9) Shuinan Cave: situated near the Reed Flute Cave, with the elevation of 175m at the cave entrance，250m in length，20m in width and 40m in height. A stalagmite (No.1, 2.45m high) from the cave was cut and moved back to the laboratory for paleoclimate reconstruction study. The modern temperature at the place where the stalagmite was selected is 19.2～19.9oC. From the cutting profile, 8 deposition cycles could be found. This probably indicates some periodic changes in geology, climate and environment.. For instance，more clay could be found near deposition hiatus, with abundance of organic carbon, manganese and copper，and heavier oxygen and carbon isotopes, which indicate the forming conditions of dry and cold climate. According to Uranium-series dating, the age of the stalagmite is from 190ka B.P. to 80ka B.P..


Fig.8 The plane and section map of the Reed Flute Cave (modified from Zhu Xuewen et al,1988)
1. stalactite 2.stalagmite 3.flowstone 4.soil 5.collapse

Sept. 11, Tuesday: Boat Cruise on Lijiang River
The Cruise will start from Yangti or Daxu depending on the water level of the river, through Xingping to Yangshuo, with total length of about 35km (Fig.9). On boat, one can enjoy beautiful peak cluster scenery on both sides of the Lijiang River, such as peculiar tower karst, green hills and peaks, and the clear river water. On limestone cliffs, natural paintings made by the blue-green algae, and heliotropic stalactites can be observed. Lunch will be served on boat.

Fig.9 Guilin Karst along Lijiang River
ROUTE.4: September 12, Wed. 8:00 - 12:00: The Institute of Karst Geology à Rentou (Man head) Red Bed à Zhenpi Caveà The Institute of Karst Geology
(10) Rentou Peak Red Bed outcrop: There is a patch of Red Bed in the plain between towns of Qifeng and Yanshan. It has an area of about 1 km2. According to the borehole data, the Red Bed is more than 100 m thick, and composed of red mudstone, siltstone and limestone breccia, with greenish grey mottles. So it was suggested to be a lacustrine deposit. Abundant fossils of Atopochara flora were found, mainly Atopochara sp., Charites sp. and etc., indicating the Red Bed is formed in Late Cretaceous, which is also verified by the Rb-Sr isotopic age of illite in the Red Bed. This finding is important to studying the evolution history of tower karst in Guilin. The red bed is found scattered and widespread on the top of quite a few peaks, such as on Houshan Hill (580 m as l.) and Old Man Hill (320 m asl.), or in the karst depressions of high altitude. Therefore, it is reasonable to imagine that the region was once covered by Late Cretaceous Red Bed in an area much greater than what is seen today. Owing to the differential uplift during Tertiary, the Red Bed was denudated and removed gradually, and the tower karst began to occur in the exposed limestone area. From such consideration, a simplified model for the development of the tower karst in Guilin has been summarized as in Fig. 10.
(11) Zhenpi Cave: It is in the southwestern foot of the Dushan Hill, 10 km to the south of downtown Guilin. The cave has a small chamber-like hall in the front part and a subterranean stream at the back. The chamber part is 12 m wide and 3-5 m high, extending 15m inwardly. Its floor space is about 200m2, having a cultural layer about 3 m thick. In 1973, more than thirty skeleton of Neolithic Man were unearthed along with a number of stone artifacts, earthenwares, bone implements and clamshell object, as well as many fossil remains such as Lijiang Deer, Asian Elephant, Coconut Cat, Antelope and other tropical and subtropical animals. The cultural layer is covered by flowstone 10-80 cm thick. Results of dating of some specimens are as follows: flowstone 6600-3370years(C-14method), clam-shell 11,3104±180years ( C-14 method), animal bone 7,580±410years (C-14 method ), and ceramic fragments 10,550 years (thermoluminescent dating). According to these data, the times of the prehistoric man could be traced back to 7,500-10,000 years B.P. All these historical relics are displayed in a museum in front of the cave. Fossils of spore and pollen from the cave show that 6000 years B.P. the vegetation around Guilin was much more flourishing than today with more species of plant.

Fig.10 A simplified model for the evolution history of Guilin karst (After Yuan Daoxian, 1986)
1. Middle and upper Devonian limestone 2.Cretaceous red breccia 3.Cretaceous red siltstone 4.Cretaceous red mudstone 5.surface stream and swallet

References 1. Liu Zaihua (ed.), 1991. IGCP 299 "Geology, Climate, Hydrology and Karst Formation" Guidebook for Field Excursions of International Symposium and Field Seminar on Karst of Inner Plate Region with Monsoon Climate. P1-18. The Institute of Karst Geology 2. Liu, Zaihua, Yuan, Daoxian, Zhao, Jingbo. 1997. Carbon dioxide in soil and its drive to karst processes: A case study in transitional zone between North and South China. In: Proceedings of 12th Congress of Speleology, Switzerland. Vol.1, p300 3. Liu Zaihua, Zhao Jinbo, 2000. Contribution of carbonate rock weathering to the atmospheric CO2 sink. Environmental Geology , vol.39, no.9, pp1053-1058 4. Yuan Daoxian (ed.), 1988. Glossary of Karstology. The Geological Publishing House, Beijing, China 5. Yuan Daoxian et al., 1991. Karst of China. The Geological Publishing House, Beijing, China 6. Zhang Meiliang et al., 2000. Determination of age and stable isotope components of stalagmite No.1 in Shuinan Cave, Guilin, and their significances in paleoclimate.. Geological Geochemistry, 2000, 28(1):41-47 7. Zhu Xuewen et al., 1988. Study on Karst Geomorphology and Caves in Guilin. The Geological Publishing House, Beijing,China 8. A.C Waltham (Editor), China Cave 1985, First Sino-British Cave Project, published by The Royal Geographical Society, 1986, London,60 pages. 9. Yuan Daoxian. New Observation on Tower Karst. International Geomorphology, 1986 part II(Edited by V. Gardiner). John Wiley & Sons LTD, 1987:1109-1123

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