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Seasonal variation in the three-dimensional structures of coastal thermal front off western Guangdong
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Yan Zhang1, 3, Lili Zeng2, Qiang Wang2, Bingxu Geng2, Changjian Liu1, 3, Rui Shi2, Na Liu2, Weiping Wang1, 3, *, Dongxiao Wang2
Acta Oceanologica Sinica | 2021, 40(7) : 88 - 99
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Acta Oceanologica Sinica | 2021, 40(7): 88-99
• Physical Oceanography, Marine Meteorology and Marine Physics •
Seasonal variation in the three-dimensional structures of coastal thermal front off western Guangdong
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Yan Zhang1, 3, Lili Zeng2, Qiang Wang2, Bingxu Geng2, Changjian Liu1, 3, Rui Shi2, Na Liu2, Weiping Wang1, 3, *, Dongxiao Wang2
Affiliations
  • 1 South China Sea Marine Survey and Technology Center, Ministry of Natural Resources, Guangzhou 510300, China
  • 2 State Key Laboratory of Tropical Oceanography (LTO), South China Sea Institute of Oceanology, Chinese Academy of Sciences, Guangzhou 510301, China
  • 3 Key Laboratory of Marine Environmental Survey Technology and Application, Ministry of Natural Resources, Guangzhou 510300, China
Published: 2021-07-25 doi: 10.1007/s13131-021-1739-9
Outline
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The seasonal structure and dynamic mechanism of oceanic surface thermal fronts (STFs) along the western Guangdong coast over the northern South China Sea shelf were analyzed using in situ observational data, remote sensing data, and numerical simulations. Both in situ and satellite observations show that the coastal thermal front exhibits substantial seasonal variability, being strongest in winter when it has the greatest extent and strongest sea surface temperature gradient. The winter coastal thermal front begins to appear in November and disappears after the following April. Although runoff water is more plentiful in summer, the front is weak in the western part of Guangdong. The frontal intensity has a significant positive correlation with the coastal wind speed, while the change of temperature gradient after September lags somewhat relative to the alongshore wind. The numerical simulation results accurately reflect the seasonal variation and annual cycle characteristics of the frontal structure in the simulated area. Based on vertical cross-section data, the different frontal lifecycles of the two sides of the Zhujiang (Pearl) River Estuary are analyzed.

oceanic thermal fronts  /  South China Sea  /  seasonal dynamics
Yan Zhang, Lili Zeng, Qiang Wang, Bingxu Geng, Changjian Liu, Rui Shi, Na Liu, Weiping Wang, Dongxiao Wang. Seasonal variation in the three-dimensional structures of coastal thermal front off western Guangdong[J]. Acta Oceanologica Sinica, 2021 , 40 (7) : 88 -99 . DOI: 10.1007/s13131-021-1739-9
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1 Introduction
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An oceanic front is a typical mesoscale oceanic phenomenon identified by a discontinuity in, for example, temperature, salinity, or nutrient and chlorophyll a contents (Belkin et al., 2009). According to Yanagi and Koike (1987), oceanic fronts are classified into coastal water fronts, shelf fronts, and open ocean fronts. Numerous studies on the relationship between sea surface temperature (SST) and sea surface wind have been conducted on continental shelf and open ocean fronts in the equatorial and mid-latitude oceans. However, studies on the modification of the effect of sea surface wind on coastal water fronts have rarely been reported.
As an important physical process in the continental shelf, oceanic fronts play a vital role in the regional climate, carbon cycle, primary production, fisheries, coral bleaching, marine birds and mammals, and regional ecosystem (Simpson et al., 1978; D’Croz and Maté, 2004; Pauly and Christensen, 1995; Bost et al., 2009; Cabrera et al., 2011; Omand et al., 2015). The vigorous thermal fronts accompanied by high chlorophyll concentrations stretch several hundreds of kilometers along the shelf (Wang et al., 2001; Hu et al., 2003; Liu et al., 2010). Intense horizontal thermohaline gradients, enhanced turbulence, current shear, and surface convergence are closely linked with persistent fronts (Qiu et al., 2019). These dynamic processes contribute significantly to the high biological productivity in frontal zones (Johannessen et al., 2005; Holt and Umlauf, 2008; D’Asaro et al., 2011; Johnston et al., 2011; Long et al., 2012; Mahadevan et al., 2012; Omand et al., 2015).
The South China Sea (SCS) is an epi-continental marginal sea of the western Pacific Ocean, with a maximum depth of over 3 000 m (Liu et al., 2004). A main feature of its topography is a broad continental shelf shallower than 200 m (Fig. 1), linked to the deep basin by a steep shelf slope in the northern SCS (NSCS), where the isobaths are approximately parallel to the coastline. The climate and upper ocean circulation in the NSCS are dominated by the Asian monsoon, which blows northeasterly from October to April and southwesterly from May to September; spring and autumn are the monsoon transition periods (Xie et al., 2003). In response to monsoon forcing, the basin-scale circulation in the NSCS experiences an energetic seasonal cycle, which is generally cyclonic in winter and anticyclonic in summer (Hu et al., 2000; Liu et al., 2001; Su, 2004). Eddies with a range of horizontal scales are embedded in the circulation and they influence the shelf zone when they shift to continental slope (Su et al., 2020; Hwang and Chen, 2000; Wang et al., 2003; Chow et al., 2008; Nan et al., 2011). Driven by the persistent northeast monsoon in boreal winter, the net onshore Ekman transport over the broad continental shelf favors coastal downwelling and the development of vigorous STFs over the inner shelf (Gan et al., 2013). The winds reverse their direction and blow from the southwest in summer, triggering offshore Ekman transport of surface water over the shelf (Liu et al., 2001; Gan et al., 2009). As a result, persistent surface cooling and STFs are frequently observed in satellite SST during the summer upwelling season (e.g., Hu et al., 2003; Wang et al., 2014).
A wind-driven coastal current with an observed velocity of more than 0.2 m/s travels southwestward along the coast of the NSCS in winter, carrying cold water originating from higher latitudes. Thus, the cold coastal water transported by the coastal current, together with the shoreward accumulation of outer shelf warm water, also favors the development of winter STFs on the inner shelf. Although the position and intensity of these fronts change over time, the fronts tend to be approximately aligned with the shelf topography due to complex shelf dynamic processes that occur throughout the year.
Both the local fronts and coastal upwelling/downwelling have been widely documented in the NSCS by remote sensing measurements, field observations, and model outputs (e.g., Wang et al., 2001; Hu et al., 2003; Chang et al., 2006; Liu et al., 2010; Gan et al., 2013; Zhang et al., 2012). However, as common seasonal features under the influence of the monsoon regime, the shelf STFs in the NSCS and their underlying association with the seasonal wind forcing are not well understood to date, especially from the perspective of in situ observations at a sufficiently high spatial resolution. Results from field campaigns are important for understanding the formation mechanisms and variability of frontal activities in the NSCS.
There is a significant seasonal temporal and spatial variation of frontal activity over the shelf off the Zhujiang (Pearl) River Estuary. The seasonal mean of the temperature gradients calculated from satellite SST is highest in winter (Wang et al., 2001; Jing et al., 2016). During winter, the northeasterly monsoon causes strong cooling and stirring in the coastal sea and induces a southward intrusion of northern cold water along the coast (Shi et al., 2015). The results of comparison studies have shown that the STFs off the Zhujiang River Estuary are produced by the combined effect of the diluted fresh water from the Zhujiang River and the prevailing northeast monsoon, and are seen as an extension of the Fujian-Guangdong coastal front in the winter satellite SST gradient (Wang et al., 2012; Chang et al., 2006; Shi et al., 2015; Jing et al., 2016; Zhang et al., 2011). The variability of sea-surface thermal fronts is well studied use satellite data (Wang et al., 2001, 2004). But the three-dimensional structures, the detailed characteristics of these STFs and their underlying associations with the seasonal wind forcing have not been well understood in this region.
This study focuses on the three-dimensional structures and seasonal variations of the STFs over the shelf off the Zhujiang River Estuary using four repeat field surveys, satellite measurements, and model simulations. Section 2 describes the in situ observations, the satellite-derived datasets, SST gradient calculation, and model simulations. The three-dimensional structures of seasonal STFs are investigated by in situ observations in Section 3. Section 4 discusses the relation between the thermal front and wind, and Section 5 presents the simulated seasonal variation and lifecycle of STFs. Finally, a summary is presented in Section 6.
2 Data and methods
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2.1 Shipboard hydrographic measurements
A total of 4 repeat surveys, in summer and winter 2006 and spring and autumn 2007 (Table 1), were conducted over the shelf off the Zhujiang River Estuary in the NSCS (Fig. 1). The cruise tracks and positions of the CTD casts were designed to be the same in each survey, to obtain a better understanding of survey data by comparing these hydrographic structures in different seasons. On each cruise, there were 18 cross-shelf hydrographic transects covering the major front-development zones in the shelf off the Zhujiang River Estuary. The temperature, conductivity, and pressure were measured using a SeaBird 911 Plus CTD instrument.
Strict quality control was applied to the in situ data. In summer and autumn, the investigation was divided into several surveys because of typhoons and the onset of the winter monsoon, if the survey time slot was longer than 10 d in order to avoid calculation errors. The total number of CTDs and the selected CTDs used in this paper from the 4 surveys are listed in Table 1.
2.2 Satellite remote sensing data
The satellite remote sensing data used in this study include SST and sea surface wind from several satellite sensors. The SST data are derived from the operational SST and sea ice analysis (OSTIA) data provided by the Group for High Resolution SST (GHRSST) Pilot Project. This project was initiated by the Global Ocean Data Assimilation Experiment in 2000. OSTIA SST with a daily resolution of 0.05°×0.05° uses several types of satellite data from the GHRSST project, as well as in situ observations, to determine the SST for the global ocean. The OSTIA dataset provides robust data and acceptable near-shore accuracy, which enables it to identify coastal fronts in the NSCS. Among five sea surface temperature products based on satellite remote sensing observations, the OSTIA SST is considerable closer to the in situ observations. The OSTIA SST yields the smallest root mean square difference (RMSD) compared with independent buoy and ship observations in the coastal and shelf seas around China (Xie et al., 2008).
The sea surface wind data are from the quick scatterometer (QuikSCAT) and advanced scatterometer (ASCAT). QuikSCAT wind velocity is high-pass filtered using a 13-d running mean to examine the sea surface wind response at the synoptic time scale, which provides a more extensive geographical and temporal coverage and higher spatial resolution of ocean vector winds than those obtained by other space-borne sensors (Liu et al., 2002; Chelton and Wentz, 2005). Since QuikSCAT finished its mission in October 2009, ASCAT continues to provide global sea surface wind data.
The QuikSCAT data are distributed by Remote Sensing Systems (RSS) with a daily resolution of 0.25°×0.25°, and the ASCAT data from 2009 to 2016 are available from the Asia-Pacific Data Research Center. The existing data covering the NSCS frontal area are sufficient to support the present study despite the lack of near-shore data. The monthly climatological mean vector and scalar winds are calculated based on daily observations in this study and the wind data are based on 10-m equivalent neutral winds. Equivalent neutral wind is the wind that would exist under idealized conditions at a given height for a neutrally stratified atmospheric boundary layer.
2.3 SST gradient calculation
In this study, a gradient-based algorithm is utilized for each of the daily mean SST fields (Letelier et al., 2009). The intensity of the surface thermal front (STF) is quantitatively estimated by the SST gradient in each geo-referenced grid cell. The zonal and meridional components of the SST gradient (GSSTX, GSSTY) are calculated via centered difference. The gradient magnitude (GM) is estimated by the following formula:
$ {\rm{GM}} = \sqrt {{{({\rm{GSS}}{{\rm{T}}_X})}^2} + {{({\rm{GSS}}{{\rm{T}}_Y})}^2}}. $
2.4 Model simulation
We use the Regional Ocean Modeling System (ROMS) model, which covers the whole shelf and slope region of the NSCS (Fig. 1). This model uses a curvilinear horizontal orthogonal grid with an average spatial resolution of approximately 3 km, where the coordinate directions (x, y) are nearly aligned alongshore and cross-shore, respectively. There are 31 levels in the vertical.
The model uses SRTM30 topographic data (with a horizontal resolution of (1/30)°) (Farr and Kobrick, 2000) from the National Geophysical Data Center (NGDC, USA). The model was initialized using climatological temperature and salinity from the World Ocean Atlas 2013 and forced by 6-h CCMP wind (Atlas et al., 1996) and meteorological parameters from the National Centers for Environmental Prediction and National Center for Atmospheric Research (NCEP/NCAR). Hybrid Coordinate Ocean Model (HYCOM) reanalysis data (Bleck, 2002) for daily surface elevation, temperature, salinity, and currents are applied at the lateral open boundaries in the model. Eight tidal constituents (M2, S2, N2, K2, K1, O1, P1 and Q1) were used to calculate the hourly tidal elevation and currents using the results from the Oregon State University global tidal inverse model (Egbert and Erofeeva, 2002; Egbert et al., 1994). The daily river discharge of the Zhujiang River was obtained from the Zhujiang River Resources Commission. After a spin-up period of 5 years with climatological winter-mean forcing, the model was run in hindcasting mode from 1 January 2000 to 1 December 2010. Daily output from 2000 to 2010 was used for analysis.
3 Observed thermal fronts
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3.1 Thermal fronts observed by the 4 in situ surveys
Figure 2 presents the STFs observed from the 4 field campaigns in winter, spring, summer, and autumn of 2006–2007, respectively. Surface thermal front is obvious in winter and spring, and the maximum thermal gradients from in situ observation exceed 0.20°C/km.
Previous studies analyzed the thermal fronts outside the Zhujiang River Estuary as a single entity in winter (Wang et al., 2001; Shi et al., 2015; Jing et al., 2016), but the in situ results show that the front located around the Zhujiang River Estuary is not a simple response to a single mechanism as previously studied (SCSB/SOA, 1990), but should be separated into two parts for analysis (Fig. 2).
The in situ SST gradient in Fig. 2 shows that in winter the STFs on the west side of the Zhujiang River Estuary are clearly induced by the colder fresher water from the Zhujiang River. The strong northeast wind drives the runoff water southwest along the coast and the front forms at the head of the estuary, although the runoff from the Zhujiang River reaches a minimum during winter. On the east side of the Zhujiang River Estuary the STFs merge with the front to the northeast but are located farther offshore; the front to the northeast is formed where southward-moving Fujian coastal cold water from northwestern Fujian meets the warm water ahead.
Spring is the transition season of the monsoon regime, when the northeast winds weaken gradually and are eventually replaced by the reverse summer monsoon winds at the end of spring (Wang et al., 2012). The wind direction is nearly east during the spring survey and the intensity clearly decreases. The STFs off the western part of the Zhujiang River Estuary persist although their extent is reduced slightly, but the STFs off the eastern part of the Zhujiang River Estuary almost disappear. In winter and spring, the patterns of the salinity front on the west side of the Zhujiang River Estuary are almost the same as those of the thermal front, so the thermal front in this region is mainly formed by the influence of Zhujiang River water in these two seasons.
In summer, the front around the Zhujiang River Estuary disappears as a result of the prevailing southwest monsoon, and the cross-shelf thermohaline structures in the vertical profiles are dominated by coastal upwelling and topographic effects (Gan et al., 2009; Su and Pohlmann, 2009). The in situ measured SST gradient in summer does not show a notable Zhujiang River plume front. In the summer survey the STFs were located mostly at the boundary of Guangdong Province where upwelling frequently occurs; STFs are found where cold water from the deep layers upwells, as is seen more clearly in the vertical profiles (Fig. 3).
In autumn the opposite transition occurs, from southwest to northeast prevailing wind. Most stations of the autumn survey were sampled in November after the onset of the winter monsoon, when the front on the west side of the Zhujiang River Estuary had not yet formed. On the east side of the Zhujiang River Estuary the thermal front had started to appear with a similar pattern to that in winter. These results show that wind forcing plays an important role in the seasonal cycle of thermal front activity.
3.2 Cross-shelf vertical structures of seasonal thermal fronts
To identify the differences in thermal fronts between the western and eastern parts of the Zhujiang River Estuary, we select three sections that cover the two sides (L03 in the east; L14 and L17 in the west) of the estuary.
In winter, water in the upper layer is well mixed with a mixed layer depth of 70 m (L03); at depths less than 70 m in the profile the vertical thermal (Fig. 3) and salinity structures have nearly the same pattern. The L03 profile shows an obvious thermohaline front with sharp thermal and salinity gradients from the sea surface to the bottom (Yanagi and Koike, 1987). On the cross-shelf transect the main body of the thermohaline front occurs between 20 m and 50 m depth, and corresponds to the strong band-shaped thermal fronts on the shelf over the eastern side of the Zhujiang River Estuary in winter. In spring, as the mixed layer depth is reduced, the thermohaline front weakens and nearly disappears. In summer, the thermohaline front disappears in the L03 section and there is evident upwelling. In autumn, as the northeast prevailing wind strengthens, the upper layer is well mixed and the thermohaline front appears, although the intensity is weaker than in winter.
The L14 and L17 sections are both on the western side of the Zhujiang River Estuary. Temperature and salinity profiles show a thermohaline front in winter and autumn. The offshore gradient of sea temperature in L17 is stronger than in L14 during winter and spring, although L17 is farther from the Zhujiang River Estuary. This phenomenon can be found more clearly in the salinity profiles, and may be due to the strong northeasterly winter monsoon wind forcing. In summer, the gradient of temperature in the x direction disappears, and the L14 salinity gradient strengthens greatly, becoming stronger than that in L17 under the influence of plentiful diluted Zhujiang River water and the southwest wind that traps the diluted water. In autumn the situation is similar to that in winter, but the gradients of temperature and salinity are slightly weaker.
3.3 Probability of occurrence of surface thermal fronts, as inferred from satellite data
The probabilities of occurrence of STFs in each month are calculated from the daily SST dataset from 2006 to 2015. In the calculation, only STFs with local temperature gradients greater than 0.03°C/km were retained. Areas with a probability of developing STFs greater than 30% are consistent with the spatial patterns of frontal intensities at the sea surface observed from satellite data (Fig. 4). The monthly climatological winds are shown in Fig. 5. In November, forcing by the strong northeast winter monsoon results in sea water that is being brought onto the shelf by Ekman drift piling up in the northwestern part of the SCS and the thermal front appears as a strong band-shaped area with a high probability of front occurrence that persists throughout the winter.
The probability of thermal front occurrence reaches its maximum in January, over the 100 km nearest the coast on both sides of the Zhujiang River Estuary. Off the western side of the estuary the thermal front is present from November to the following February, decays from February to May, and disappears from June to October. The STFs have a high probability of occurrence in the winter half year (November–April) but nearly disappear in the summer half year (May–October).
4 Relation between thermal front and wind
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As the occurrence of STFs in each month generally has some connection with the wind forcing (see Section 2.2), we choose a box region (shown in Fig. 4) to study the relation between them using a regional-mean time series (Fig. 6).
The regional-mean front index over the western shelf of the Zhujiang River Estuary reaches its maximum value in January and minimum in September. Except in summer when the offshore wind is weak, the variation of the front index is consistent with the seasonal cycle of alongshore wind, but lags a little after September. The direction of_the wind perpendicular to the coast determines the variation of the thermal gradient; offshore wind velocity has a positive correlation with thermal gradient, and onshore wind velocity has a negative correlation with thermal gradient. This suggests that the frontal activity is closely related to the seasonal wind forcing in this region.
5 Simulated seasonal variation and lifecycle of STFs
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In situ surveys are limited because they are time-consuming and expensive. Satellite data measurements can only reflect the characteristics of the sea surface, although the spatial patterns of STFs are almost same to the in situ results, but the values are weakened by quality control methods, such as interpolation and assimilation (Fig. 7). Here, the ROMS model is used to further examine the thermodynamic mechanisms of the coastal front. The numerical simulation results accurately reflect the seasonal variation and annual cycle of the front structures in the simulated area. Vertical cross-sections are used to analyze the different frontal lifecycles on the two sides of the Zhujiang River Estuary.
The results of the numerical simulation (Fig. 7) show that the seasonal variation in the simulated area is consistent with that seen from satellite observations, and the distribution of the fronts across the four seasons is simulated well, especially the reappearance of the thermal front pattern in winter. The strength of the front is stronger than in satellite observations, and is close to the value of in situ observations. We analyze the annual cycle of the Zhujiang River Estuary coastal STFs with the simulated results for the L03 and L17 profiles.
The L03 profile is on the east of the Zhujiang River Estuary, an area strongly influenced by the winter monsoon and the southward movement of the Fujian coastal cold water in winter. The modeled temperature distribution along the L03 profile (Fig. 8) shows that along the coast where the depth is about 30 m the thermal front is significant with a sharp temperature gradient in winter (December, January, February); the front extends across the whole vertical profile from the surface to the bottom, which is consistent with the in situ observations (Fig. 3), and then weakens in March and disappears in April and May. In June, under the influence of upwelling the thermal front appears off the coast at depths of 10–50 m; its strength and range are greater than the thermal front in winter, and it develops and strengthens in July and August, before weakening and disappearing in September. However, this is not seen in the satellite observations because the front occurs below the sea surface. In October, the temperature gradient seems to strengthen in the region of the winter front, and the winter thermal front is formed in November.
The modelled thermal front lifecycle of the L17 profile (Fig. 9) is similar to that of L03. The coastal thermal front is significant in winter, and the thermal front induced by upwelling develops in summer, but with weaker intensity than the thermal front of L03.
6 Summary
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In this study, seasonal variation in the three-dimensional structures and the lifecycle of the shelf STFs on the coast of the NSCS are investigated, with satellite data and 4 repeat fine-resolution in situ surveys in four seasons of 2006–2007. A model is used to further examine the lifecycle and thermodynamic mechanisms of the coastal front and their underlying associations with wind forcing.
Both in situ and satellite observations show that the coastal thermal front exhibits substantial seasonal variability. The front is strongest and has its greatest extent and strongest sea surface temperature gradient in winter. The in situ data show that the front located around the Zhujiang River Estuary is not a simple response to a single mechanism as previously studied, but that it should be considered as two separate parts. In winter, the STFs on the west side of the Zhujiang River Estuary are induced by the colder diluted freshwater from the Zhujiang River, and on the east side of the Zhujiang River Estuary the STFs merge with the front to the northeast but are located farther offshore; the front to the northeast is formed where southward-moving Fujian coastal cold water from northwestern Fujian meets the warm water ahead. In spring, there are still STFs over the western part of the Zhujiang River Estuary, although they cover a smaller area, but the STFs over the eastern part of the Zhujiang River Estuary almost disappear. In summer, the front around the Zhujiang River Estuary disappears, and the SST gradient of in situ observations, driven by the prevailing southwest monsoon, does not show a notable Zhujiang River plume front. In autumn, there is still no front in the western part of the Zhujiang River Estuary, but in the eastern part of the estuary the thermal front begins to reappear with a similar pattern to that in winter.
The results from both field campaigns and satellite measurements suggest that the seasonal wind forcing plays an important role in determining the frontal activity over the shelf. The ROMS model is used to further examine the thermodynamic mechanisms driving the coastal front. The numerical simulation results accurately reflect the seasonal variation and annual cycle characteristics of the front structure in the L03 and L17 profiles, and show the differences in frontal lifecycle between the two sides of the Zhujiang River Estuary.
Funding
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  • The National Natural Science Foundation of China under contract Nos 41776025, 41576003, 41776026, 41676018 and 41806035; the Pearl River S&T Nova Program of Guangzhou under contract No. 201906010051; the Rising Star Foundation of the South China Sea Institute of Oceanology under contract No. NHXX2019WL0101; the Science and Technology Program of Guangzhou under contract No. 202002030490.
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Appendix
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Article Info
doi: 10.1007/s13131-021-1739-9
  • Receive Date：2020-07-17
  • Online Date：2026-03-03
  • Published：2021-07-25
Article Data
Affiliations
History
  • Received：2020-07-17
  • Accepted：2020-09-17
Funding
The National Natural Science Foundation of China under contract Nos 41776025, 41576003, 41776026, 41676018 and 41806035; the Pearl River S&T Nova Program of Guangzhou under contract No. 201906010051; the Rising Star Foundation of the South China Sea Institute of Oceanology under contract No. NHXX2019WL0101; the Science and Technology Program of Guangzhou under contract No. 202002030490.
Affiliations
    1 South China Sea Marine Survey and Technology Center, Ministry of Natural Resources, Guangzhou 510300, China
    2 State Key Laboratory of Tropical Oceanography (LTO), South China Sea Institute of Oceanology, Chinese Academy of Sciences, Guangzhou 510301, China
    3 Key Laboratory of Marine Environmental Survey Technology and Application, Ministry of Natural Resources, Guangzhou 510300, China

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表12种不同金属材料的力学参数
科
Family		 属数
Number of
genus		 种数
Number of
species		 占总种数比例
Percentage of
total species (%)		 属
Genus		 种数
Number of
species		 占总种数比例
Percentage of total
species (%)
鹅膏菌科Amanitaceae 2 11 5.26 鹅膏菌属 Amanita 10 4.78
小菇科 Mycenaceae 2 12 5.74 丝盖伞属 Inocybe 5 2.39
多孔菌科 Polyporaceae 8 14 6.70 蜡蘑属 Laccaria 5 2.39
红菇科 Russulaceae 3 23 11.00 小皮伞属 Marasmius 6 2.87
小菇属 Mycena 11 5.26
光柄菇属 Pluteus 5 2.39
红菇属 Russula 17 8.13
栓菌属 Trametes 5 2.39
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