Upwelling Irradiance below Sea Ice—PAR Intensities and Spectral Distributions

Abstract

Upwelling and downwelling spectral (320–920 nm) distributions and photosynthetic active radiation (PAR) intensities were measured below a first-year land-fast sea ice in a western Greenland fjord with and without a snow cover. Time-series of surface upwelling PAR, downwelling PAR, and under-ice PAR were also obtained. Spectral distributions of upwelling and downwelling irradiances were similar except for reduced intensities in the UV, the red, and NIR parts of the spectrum when the ice was snow-covered. Upwelling PAR amounted to about 10% of downwelling intensities, giving 5.1 µmol photons m⁻² s⁻¹ at the bottom of the ice with a snow cover and 8.2 µmol photons m⁻² s⁻¹ without. PAR partitioning analyses showed that the upwelling was related to scattering by suspended particles in the water column. A snow melt increased under-ice daily maximum downwelling PAR from 50 to 180 µmol photons m⁻² s⁻¹ and overall under-ice PAR of 55 and 198 µmol photons m⁻² s⁻¹ with 10% upwelling. It is concluded that upwelling PAR below sea ice might be an important factor regarding sea ice algae photophysiology and performance with a 10% higher PAR; specifically when PAR > E_k the light saturation point of the sea ice algae.

1. Introduction

Nearly 10% of the surface of the earth is covered by sea ice, at its maximum extent in both the Arctic and Antarctic [1,2], and sea ice has a significant role in the Earth’s climate due to its high albedo, whereby 50%–80% of upcoming radiation is reflected [3]. Sea ice is an ecosystem with defined pathways of matter and energy [4], and several organisms, from bacteria to polar bears, rely and depend on sea ice for maintaining their life cycles [5]. Ice algae residing at the bottom of the sea ice and in the brine channels contribute about 10% of the total marine-produced carbon [6]. They bloom in the early spring when light reaches the bottom of the sea ice, often passing a snow pack of variable thickness. Most of these microalgae are acclimated to low light conditions [7,8,9]. For instance, active sea ice algae photosynthesis has been observed at just 0.17 µmol photons m⁻² s⁻¹ at the bottom of a 1 m thick sea ice cover with 0.9 m snow [10]. Light is the main limiting factor for sea ice algae in early spring, as nutrient concentrations are still relatively high in the water column [11]. Irradiance at the sea ice–water interface is in-part regulated by the downwelling irradiance from the atmosphere, albedo of the snow and ice, and snow and ice thickness. The absorption and scattering in the snow and ice packs are related to snow age, temperature, water content [12], and, especially, brine and gas volumes in the sea ice [13]. There are further solid and dissolved substances in the snow and sea ice pack that either scatter or absorb the irradiance, including CDOM, chlorophyll a (Chl a), self-shading by algae, particulate matter, and diverse impurities [14]. In open and ice-free waters, some of the irradiance that reaches the oceans is reflected back to the water–air interface, as a result of scattering, and enters the atmosphere as water-leaving radiance [15]. This signal and its spectral composition are applied, for example, in multiple remote sensing applications for measuring Chl a and suspended particulate matter concentrations in the oceans [16]. The water-leaving radiance signal has been applied in sea ice-covered areas for Chl a and optical properties of the water column [17]. The intensity and spectral composition of the water-leaving radiance depends on the optical properties of the water column constituents, such as its dissolved and solid substances [18]. Under-ice light intensities are several times lower than in an ice-free water column, but there is still an upwards-directed irradiance, termed upwelling irradiance [19]. There are, to the authors knowledge, not many specific studies of the upwelling irradiances below sea ice. We here report the results of a study where we measured vertically and spectrally resolved upwelling and downwelling irradiance and photosynthetic active radiation (PAR) below a first-year land-fast sea ice.

We raise the following questions: (1) What is the intensity of the upwelling irradiance below the sea ice; (2) are there any differences in spectral composition of the upwelling and downwelling irradiances; (3) which optical properties in the water column regulate the intensity of the upwelling irradiance and discuss the potential effects that upwelling irradiance might have on low-light adapted ice algae [20].

2. Materials and Methods

2.1. Study Area and Sampling

Measurements and sampling were carried out at 66°56.370′ N, 50°59.280′ W in early March 2013 on first-year land-fast sea ice in the Kangerlussuaq estuary (Figure 1a). The estuary is only affected by inflowing, highly turbid meltwater from the Greenland inland ice (GrIS) between May and September [21]. The estuary, its optical conditions, the snow and ice, and its primary production are described previously [22,23,24]. The present study was part of a larger research program carried out on the ice between 11 and 20 March 2013, which had a focus on the effects of loss of snow cover on biological and photobiological conditions of the sea ice algae as reported elsewhere in this Special Issue [25]. In the present work we report upwelling and downwelling irradiances below the sea ice, both with and without a snow cover, along with measurements of sea ice and snow thickness, sea ice properties including bulk salinity, brine and gas volumes, temperature, and Chl a content in the ice. Physical and optical properties of the water column below the ice were measured as depth profiles of salinity, temperature, Chl a, and suspended particulate matter (SPM) concentrations.

2.2. Optical Measurements

Time series were obtained at the site for surface downwelling PAR and upwelling PAR measured at 0.5 m above the surface for albedo with two Li-Cor sensors (LI-COR LI-190R Quantum Sensor) marked Up + Down PAR (Figure 1b). A third Li-Cor sensor (LI-COR LI-192 Underwater Quantum Sensor) was mounted at 3 cm below the ice to measure downwelling PAR (marked as under ice PAR), with all sensors connected to a datalogger (Figure 1b). The under-ice sensor was mounted on a stick and kept in place by a frame until the stick was frozen into the ice. Sensors were placed at the site with an even and uniform snow cover, and great care was taken to keep disturbance of the snow cover to a minimum. Transmittance was given by the ratio between under-ice downwelling PAR and surface downwelling PAR. Under-ice spectral irradiance was measured with a recently (0.5 yr) purchased and calibrated TriOS Ramses ACC VIS cosine-corrected hyperspectral radiometer (Radiometer—TriOS Mess- und Datentechnik). The measuring range of the TriOS sensor was 320–920 nm with a spectral resolution of 1.3 nm, and connected to a PC with a cable running the TriOS standard software. The sensor was mounted on an articulated L-arm and deployed through a hole with a diameter of 9.0 cm drilled with a Mark II Kovacs ice corer. Distance between hole and measuring point was 1 m. Triplicate measurements of downwelling irradiances were obtained from 3 cm below the bottom of the sea ice and down to a depth of 8.0–9.0 m with a vertical resolution of 0.5 m. The TriOS optical sensor was subsequently mounted to measure upwelling irradiances, also in triplicate, with a 0.5 m depth resolution down to 3.5–4.0 m depth. Sensor measuring depths were given to an accuracy of 1 cm by a calibrated pressure sensor system mounted on the L-arm and connected with a cable to a PC on the surface of the ice. Spectral measurements were carried out in two stages: (1) upwelling and downwelling with an intact snow cover and (2) upwelling and downwelling with no snow cover where it was removed manually, forming a snow free rectangle 15 by 15 m with the deployment hole in the middle (Figure 1b). All TriOS spectral measurements were carried out on 14 March 2013 between 1:20 and 2:20 PM with a clear and sunny sky. The PAR site with the three PAR sensors was established at 11:10 AM on 12 March with continous recordings every five minutes until 00:30 PM 19 March. Air temperature was recored every 5 min at 1 m above snow surface at the experimental site (Figure 1b).

2.3. Ice Cores, Bulk Salinity, and Temperatures

Snow cover thickness at the experimental site was measured to the nearest 0.1 cm with a ruler, and ice cores were collected using a Mark II Kovacs corer with an inner diameter of 9.0 cm. Sea ice temperatures were measured by drilling a 3 mm thick hole to the center of the ice core and measured to the nearest 0.1 °C with a digital thermometer Testo Thermometers (Temperature measuring instruments with connectable probes | DK-Site). Total length of the ice core was measured to nearest 0.1 cm. The cores were cut into 5 cm thick slices with a stainless steel saw and placed in sealed polyethylene bags and brought back to the laboratory at Kangerlussuaq International Science Support (KISS). Here, samples were thawed in the dark overnight in a refrigerator at 4 °C and, once thawed, salinity was measured to nearest 0.01 using a salinometer YSI Pro Plus (YSI ProQuatro | Portable Multiparameter Water Quality Meter). Bulk salinity and temperatures were applied for calculating brine and gas volumes of the ice following [26]. More details on sampling procedures are found in [4,25].

2.4. CTD, Chlorophyll a, Suspended Particulate Matter

Water samples for Chl a and SPM were sampled using a bilge pump with an intake immersed through a 9.0 cm drilled hole in the ice to a depth of 1.5 m below bottom of the sea ice. Chl a in water samples and thawed ice were determined by filtering 200 mL of the sample through glass fibre filters (GF75, Advantec). Filters with phytoplankton were extracted in 10 mL 95% ethanol for about 16 h, and the extract was centrifuged and the supernatant was analysed on a Turner Trilogy fluorometer (Trilogy Laboratory Fluorometer | Turner Designs | United States). SPM concentrations were determined by filtration of an exact volume (0.5–1.l) of water through pre-combusted (400 °C, 6 h) glass fiber filters (GF/F, Whatman). Distilled water was used to remove any salt residues, and filters were kept dark and cold until returned to Denmark where they were dried (60 °C, 16 h) and weighed. More details on laboratory procedures are given in [23]. CDOM absorption coefficients in the sea ice sampled near the present site in 2011 were low and absorption signal was close to detection limit of the spectrophotometer method and not included here (Lund-Hansen, unpublished data). On 10 March in 2008, a Seabird CTD SBE 19plus (SBE 19plus V2 SeaCAT Profiler CTD | Sea-Bird Scientific—Overview | Sea-Bird) mounted with a Seapoint fluorometer and a Wetlabs C-Star transmissometer (C-Star Transmissometer | Sea-Bird Scientific—Overview | Sea-Bird) was applied to measure phytoplankton and SPM concentrations and distributions with depths in the water column below the ice. Water samples for Chl a and SPM were collected with a Niskin 5 L water sampler from 1.5 m below the sea ice, and Chl a and SPM samples were analysed as described above. The March 2008 calibrations of fluorometer signal against Chl a concentrations and transmissometer signal against SPM concentrations were verified with the March 2013 samples of Chl a and SPM.

2.5. Data Treatment

The vertically resolved spectrally upwelling and downwelling data (mW m⁻² nm⁻¹) were all integrated into PAR (µmol photons m⁻² s⁻¹) following standard methods [19]. Diffuse attenuation coefficient K_d(PAR) was determined by linear regression between natural logarithm (ln) transformed PAR readings and depth using the Lambert–Beer law where irradiance at the depth z (I_z) equals: I_z = I_o × e^{−Kd(PAR)×z}. I_o is irradiance at the ice-water surface and K_d(PAR) is the diffuse attenuation coefficient for downwelling PAR, as outlined [23]. The equations of the regression lines (r² > 0.99) between depth and ln(PAR) were all statistically significant (p < 0.01) and applied to derive PAR irradiances at the bottom of the ice (I_o), as described by [23]. Spectral measurements were accomplished within an hour around noon on 14 March. Integrated PAR data at depths based on the spectrally resolved upwelling and downwelling measurements, were corrected for any changes in downwelling PAR at the surface which was measured continiuosly between 12 and 19 March at the nearby upwelling and downwelling PAR site (Figure 1b).

2.6. PAR Partitioning

Diffuse attenuation coefficient K_d(PAR) is expressed as the sum of partial attenuation coefficients related to water, chromophoric dissolved organic matter (CDOM), phytoplankton, and SPM as [19]:

K_d(PAR) = K_w + K_CDOM + K_Phyto + K_SPM

(1)

or as:

K_d(PAR) = 0.027 + K*_CDOM(CDOM₄₄₀) + K*_Phyto (Chl a) + K*_SPM (SPM)

(2)

where 0.027 m⁻¹ is PAR attenuation in pure water [27], K*_CDOM is the CDOM specific attenuation coefficient of 0.22 m² g⁻¹ CDOM [28], K*_Phyto (Chl a), and K*_SPM (SPM) are specific attenuation coefficients of phytoplankton equal to 0.029 m² mg⁻¹ and 0.13 m² g⁻¹ for SPM obtained from a comparable study [23]. CDOM absorption coefficient at 440 nm was derived as described [23] based on water samples collected at the site in March 2008 (Lund-Hansen, unpublished data).

3. Results

3.1. Physical and Optical Properties of the Snow, Ice, and Water Column

The average ice thickness was 74.8 ± 0.8 cm and average snow depth was 1.2 cm ± 0.2 cm. The ice was relatively cold at the surface, as low as −8.9 °C, but temperature increased gradually to −2.0 °C at the sea ice–water interface, with only small variations in bulk salinity (Figure 2a). Gas and brine volumes (%) increased towards the bottom of the ice with the increase in ice temperature [26] (Figure 2b), and Chl a increased similarly towards the sea-ice water interface (Figure 2c).

Below ice water temperatures varied between −1 °C and −0.5 °C and salinity between 21.7 and 23, with peaks in salinity likely related to double diffusion [29], but there was no stratification of the water column (Figure 3a). Similarly for the optical constituents Chl a and SPM, there were likewise no variations with depth, with a Chl a of about 0.65 µg L⁻¹ in the entire water column and SPM concentrations between 1.2 and 1.5 mg L⁻¹ (Figure 3b).

3.2. Upwelling and Downwelling PAR

Extension of the ln(PAR) regression lines towards the sea-ice water interface gave a downwelling irradiance of 46.8 µmol photons m⁻² s⁻¹ with snow and 105.9 µmol photons m⁻² s⁻¹ without snow. Upwelling PAR at the interface reached 5.1 µmol photons m⁻² s⁻¹ with snow and 8.2 µmol photons m⁻² s⁻¹ without snow (Figure 4) This equals PAR irradiance reflectances of 11% and 8% as the ratio between upwelling and downwelling PAR [19] with and without snow. Results showed that both K_d(PAR) and K_u(PAR) were slightly higher without any snow, but also that K_d(PAR) was higher than K_u(PAR) independent of snow cover as summarized in

Table 1. Diffuse attenuation coefficients for downwelling PAR—K_d(PAR) and upwelling PAR K_u(PAR), under-ice downwelling PAR (I_0d), and under-ice upwelling PAR (I_0u), irradiance reflectances with (+Snow) and without snow (−Snow). Average downwelling surface PAR during sampling period was 546.4 µmol photons m⁻² s⁻¹.

	+Snow	−Snow
Kd(PAR) m−1	0.25	0.32
Ku(PAR) m−1	0.21	0.27
I0d (Down) µmol photons m−2 s−1	46.8	105.9
I0u (Up) µmol photons m−2 s−1	5.1	8.2
Irradiance reflectance (%)	11	8

.

3.3. Partitioning

Partitioning results clearly demonstrated that PAR attenuation (72%) was related to SPM as summarized in

Table 2. Partitioning (%) of K_d(PAR) relative to the optical constituents-water, CDOM, phytoplankton, and suspended particulate matter.

	Water	CDOM	Phyto	SPM
Kd(PAR) (%)	10	7	11	72

, and much less to phytoplankton (11%) and water (10%).

3.4. Spectral Distribution

Spectral distributions of both upwelling and downwelling irradiances with and without a snow cover were different and irradiances around 500 nm the least attenuated wavelengths in both cases (Figure 5a). A comparison of spectral distributions of ratios between upwelling and downwelling with no snow (E_u −/E_d −) and with snow (E_u +/E_d +) showed, that UV-A and blue (320–480 nm), and especially red (600–700 nm) and near infrared (750–820 nm) wavelengths were relatively stronger attenuated with a snow cover (Figure 5b). Integration of irradiances between 320 and 400 nm to derive UV-A irradiance (W m⁻²) showed that E_d(UV-A) increased from 1.5 to 3.4 W m⁻² without snow and that E_u(UV-A) increased from 0.08 to 0.24 W m⁻² giving ratios of 2.3 and 3.0, respectively.

3.5. Time-Series of Downwelling, Under-Ice, and Upwelling PAR

The daily maximum of under-ice PAR varied between 40 and 60 µmol photons m⁻² s⁻¹ with the initial snow cover of 1 cm, which melted and disappeared during 15–16 March where air temperatures at the site increased from−12 °C to +0 °C during 1.5 day, after which under-ice PAR reached a daily maximum of 180 µmol photons m⁻² s⁻¹ during 17–19 March (Figure 6b). The nearly threefold higher under-ice PAR was clearly related to the melting of the snow cover and strongly reduced PAR albedo from 0.75 between 12 and 15 March to 0.27 between 17 and 19 March, and a parallel increase in transmittance from 0.08 to 0.23. Upwelling PAR for the experimental period 12–19 March was calculated by adding 10% to measured under-ice PAR, where maximum daily upwelling under-ice PAR reached about 4 µmol photons m⁻² s⁻¹ with snow cover, which increased to about 16 µmol photons m⁻² s⁻¹ after melting of the snow (Figure 6b).

4. Discussion

4.1. Spectral Distribution and K_d(PAR)

The present spectral distribution data for under-ice irradiances were comparable to previous under-ice observations also with comparatively higher absorption in the red part of the spectrum with a snow cover, and minimum attenuation at about 500 nm [8]. Spectral composition of downwelling irradiance could be changed by algae absorption in the ice [30], but the present Chl a concentrations are low with an average of 0.75 mg Chl a m⁻² for the whole ice core, which is unlikely to affect the composition, as observed in other studies with bottom ice Chl a of 20–60 mg Chl a m⁻² [31]. Such low Chl a concentration in the ice or at the bottom of the ice aligns with previous studies in Kangerlussuaq [8,24]. The present higher absorption of red light emphasizes the optical effects of even a 1 cm thick snow cover, accentuated by a doubling from 67.4 mW m⁻² nm⁻¹ to 133.2 mW m⁻² nm⁻¹ at 500 nm with no snow cover. A relatively higher attenuation in the red part of the spectrum without a snow cover was also observed in a previous study in Kangerlussuaq [8]. The attenuation of upwelling irradiances were relatively higher in the blue and red parts of the spectrum compared to the with snow situation, and UV-A intensities further increased with no snow. The K_d(PAR) for downwelling PAR was 0.25 m⁻¹ with snow and 0.32 m⁻¹ without snow, were also comparable to previous below-ice coefficients in Kangerlussuaq [24]. However, the present coefficients were nearly two times higher than values of 0.15 m⁻¹ in the high Arctic Young Sound [32] and 0.17 m⁻¹ in the central Arctic Ocean [33]. The twofold higher K_d(PAR) in Kangerlussuaq is likely related to higher SPM concentrations in Kangerlussuaq where partitioning analyses showed that 72% of PAR attenuation was related to SPM. The Kangerlussuaq summer study in turbid meltwater showed a significant (p < 0.01) and positive linear and high (r² = 0.92) correlation between SPM and K_d(PAR), and that reflectance was governed by SPM [28]. The inflow of glacial freshwater to Kangerlussuaq ends from beginning September with no other inflow during winter, so the higher K_d(PAR) observed here could be related to resuspension of sediment by the strong tidal currents with tidal ranges up to 2 to 3 m in Kangerlussuaq [22].

4.2. Under-Ice Light Field and Reflectances

The downwelling attenuation coefficient K_d(PAR) = 0.25 m⁻¹ with snow was slightly higher without snow K_d(PAR) = 0.32 m⁻¹, which might be attributed to a changed angular field of downwelling irradiance in the absence of a snow cover [34,35]. However, brine and gas volumes of the present ice were quite high, which strongly enhance the scattering whereby light leaving the ice at the bottom is highly diffused [36]. Spectral measurements were obtained within about 1 h, but it cannot be ruled out that conditions in the water column changed during measurements considering the high tidal ranges of 2 to 3 m in Kangerlussuaq [22]. A change in condition is substantiated by the fact that K_d(PAR) actually increased from 0.25 to 0.32 m⁻¹ during the experiment. There was further a small difference of 0.04 m⁻¹ between K_d(PAR) and K_u(PAR) with higher K_d(PAR) for reasons which are not clear, and calls for further investigation. The PAR upwelling irradiances at the bottom of the sea ice of 5.1 and 8.2 µmol photons m⁻² s⁻¹ for downwelling irradiances of 46.8 and 105.9 µmol photons m⁻² s⁻¹ with and without snow equaled irradiance reflectances of 11% and 8%. The under-ice PAR was determined by extension of the regression line ln(PAR) at depth versus depth to the bottom of the ice, which assumes that PAR attenuation is exponential in the entire water column and the very high (r² = 0.99) correlation coefficients of the regression lines confirmed this. Under-ice PAR data points were corrected for any changes in surface downwelling PAR measured with the continuous PAR sensor so the difference of 3% point in irradiance reflectance might also relate to changed conditions.

4.3. Low Light Adaptation

Active photosynthesis at a PAR level of 0.17 µmol photons m⁻² s⁻¹ has recently been observed below a combined pack of 1 m snow and 0.9 m thick sea ice [10], and demonstrates that even extremely low PAR irradiance can drive photosynthesis of the highly shade-adapted sea ice algal community. In the present study upwelling irradiances reached 5.1 and 8.2 µmol photons m⁻² s⁻¹ for snow-covered and snow-free conditions which added 11% and 8% to the under-ice PAR. Total under-ice PAR then reached 51.9 µmol photons m⁻² s⁻¹ as 5.1 plus a downwelling of 46.8 µmol photons m⁻² s⁻¹ for a situation with a snow cover and a total of 105.9 µmol photons m⁻² s⁻¹ with no snow (Table 1). Ice algae primary production is generally assumed to be light limited [37,38] where this higher—downwelling PAR plus upwelling—could potentially increase the primary production, but this is out of the scope of the present study.

4.4. Acclimation to Low Light, Snow Melt, and Removal

Light passes through a pack of snow and ice where albedo, high scattering and absorption coefficients in the pack ensure very low light intensities at the bottom of the sea ice. Light attenuation is much stronger in snow [14] compared to ice, giving typical attenuation coefficients of 11.9 m⁻¹ in snow and 0.84 m⁻¹ in ice [14]. Furthermore, snow is a much more dynamic entity compared to the thickness of even land-fast ice and occurrences with periods of melt, snowfall and snowdrift [39,40] and is accordingly the dominant factor in governing the under-ice light intensities [14]. For instance, under-ice light intensities increased in the present study from about 40 to 180 µmol photons m⁻² s⁻¹ within 1.5 days related to a melt of the snow cover. The photobiological and photophysiological effects of the PAR increase and the consequences have been documented in a parallel study from this campaign [25] and are just summarized in brief here. A comparison of conditions before and after the melt and increase in under-ice PAR showed that algae biomass (Chl a) decreased 3.6 times, DOC 1.9 times, the photobiological parameters rETR_max and Φ_{PSII_max} were both reduced, and species composition changed from being dominated by flagellates (55%) to diatoms (67%) after the melt [25]. In a follow-up study in Kangerlussuaq in 2016 under-ice PAR increased from 60 to 150 µmol photons m⁻² s⁻¹ by artificial removal of the snow cover, whereby rETR_max and Φ_{PSII_max} were also reduced, along with development of photoprotective pigments and mycosporine-like amino acids (MAAs) for UV-protection [38]. Potential effects on the photobiology of the ice algae are assumed low at low downwelling irradiances, but clearly adds to the total irradiance experienced by the algae at high downwelling irradiances.

4.5. Light Saturation Point E_k

E_k is the light intensity at which photosynthesis begins to shift from light limitation to limitation by carboxylation. Above this light intensity, photoinhibition can potentially commence for any given assemblage of microalgae due to excess photons that cannot be used for carbon fixation [37]. E_k reached 45 µmol photons m⁻² s⁻¹ in the parallel study [25], which aligns with the under-ice PAR before the snow melt of 40–50 µmol photons m⁻² s⁻¹. This E_k value was greatly exceeded for a maximum downwelling under-ice PAR of 180 µmol photons m⁻² s⁻¹ after the melt, though irradiance actually encountered by the ice algae reached 198 µmol photons m⁻² s⁻¹ with the added 10% upwelling. This 4 times higher irradiance, relative to an E_K of 45 µmol photons m⁻² s⁻¹, caused strong photoinhibition, damaging photobiological effects, and changes in biomass and species composition before and after the melt as shown in the study [25]. It should be emphasized that E_k is not constant but varies depending on the light history of the algae, nutrients, and their species composition. For instance, an E_k around 120 µmol photons m⁻² s⁻¹ was obtained in another Kangerlussuaq study where artificial removal of the snow cover increased under-ice PAR to near 150 µmol photons m⁻² s⁻¹, which also had some adverse and damaging effects [38]. A laboratory study with a low E_k of 25 µmol photons m⁻² s⁻¹ also showed clear photoinhibition once irradiances > E_k [40]. When ice algae are adapted to a certain level of irradiance, as characterized by E_k, photoinhibition can commence and photodamaging effects can occur at irradiances higher than E_k, where a 10% added PAR upwelling might add to these effects.

5. Conclusions

Spectral distributions, PAR intensities, and optical properties of upwelling and downwelling irradiances below sea ice have been explored in a study on first-year land-fast sea ice. The study showed that upwelling PAR reached about 10% of downwelling intensities. The upwelling was related to scattering in the water column, where partitioning analyses showed high SPM related scattering coefficients. Data from a parallel and similar studies carried out at the site in Kangerlussuaq, showed that removal of a snow cover by melt or artificially removed strongly affected photobiology of the ice algae by a significant increase in under-ice PAR. When under-ice irradiances > E_k it was assumed that the 10% upwelling irradiances added to the photoinhibition and adverse effects of the increased PAR.